Search USGS⌕ Search

Geology topics

Barry S. Smith

Publications and source records attributed to Barry S. Smith.

8 recordsLinked to original sources
USGS2005

Simulated changes in water levels caused by potential changes in pumping from shallow aquifers of Virginia Beach, Virginia

A steady-state ground-water flow model of the southern watersheds of Virginia Beach, Virginia, was refined and used to simulate changes in aquifer water levels caused by potential changes in pumping in the Transition Area of Virginia Beach, Va., a 20-square mile planning zone that runs through the middle of the city. Cessation of dewatering at borrow pits, pumping to irrigate a golf course, pumping to irrigate lawns of a hypothetical neighborhood, and pumping to irrigate both the golf course and lawns of the hypothetical neighborhood were simulated. Simulated recoveries from cessation of dewatering of borrow pits were generally restricted to the immediate area of the pits. The simulated recoveries averaged about 20 feet (ft) near the center of the cells representing the active areas of the pits and 2 ft at the cells representing the extent of the pits. At a golf course, 4 hypothetical wells pumping 300,000 gallons per day (gal/d) from the Yorktown sand aquifer resulted in drawdowns averaging 10 ft in the pumping cells and 1 ft at a distance of 1.2 miles (mi) from the center of the pumping cells. The extent of the 1-ft drawdown was virtually the same as that simulated previously and reported in a permit application for the golf course. Simulated pumping of 150,000 gal/d from 4 cells in the confined sand aquifer representing a 40-acre neighborhood resulted in drawdowns averaging 7 ft in the pumping cells and 1 ft at a distance of 0.8 mi from the center of the cells. Simulated pumping of 300,000 gal/d from the same 4 cells resulted in drawdowns averaging 15 ft in the pumping cells and 1 ft at a distance of 1.4 mi from the center of the cells. Simulated pumping of 150,000 gal/d at the golf course and another 150,000 gal/d in the hypothetical neighborhood resulted in drawdowns that averaged 5 ft around the cells representing the golf course wells spaced 1,300 ft apart and 7 ft around the contiguous cells representing the 40-acre neighborhood. A drawdown of 1 ft encompassed most of the eastern half of the Transition Area.

Virginia↗
USGS2003

Ground-water flow and saline water in the shallow aquifer system of the southern watersheds of Virginia Beach, Virginia

Population and tourism continues to grow in Virginia Beach, Virginia, but the supply of freshwater is limited. A pipeline from Lake Gaston supplies water for northern Virginia Beach, but ground water is widely used to water lawns in the north, and most southern areas of the city rely solely on ground water. Water from depths greater than 60 meters generally is too saline to drink. Concentrations of chloride, iron, and manganese exceed drinking-water standards in some areas. The U.S. Geological Survey, in cooperation with the city of Virginia Beach, Department of Public Utilities, investigated the shallow aquifer system of the southern watersheds to determine the distribution of fresh ground water, its potential uses, and its susceptibility to contamination. Aquifers and confining units of the southern watersheds were delineated and chloride concentrations in the aquifers and confining units were contoured. A ground-water-flow and solute-transport model of the shallow aquifer system reached steady state with regard to measured chloride concentrations after 31,550 years of freshwater recharge. Model simulations indicate that if freshwater is found in permeable sediments of the Yorktown-Eastover aquifer, such a well field could supply freshwater, possibly for decades, but eventually the water would become more saline. The rate of saline-water intrusion toward the well field would depend on the rate of pumping, aquifer properties, and on the proximity of the well field to saline water sources. The steady-state, ground-water-flow model also was used to simulate drawdowns around two hypothetical well fields and drawdowns around two hypothetical open-pit mines. The chloride concentrations simulated in the model did not approximate the measured concentrations for some wells, indicating sites where local hydrogeologic units or unit properties do not conform to the simple hydrogeology of the model. The Columbia aquifer, the Yorktown confining unit, and the Yorktown-Eastover aquifer compose the hydrogeologic units of the shallow aquifer system of Virginia Beach. The Columbia and Yorktown-Eastover aquifers are poorly confined throughout most of the southern watersheds of Virginia Beach. The freshwater-to-saline-water distribution probably is in a dynamic equilibrium throughout most of the shallow aquifer system. Freshwater flows continually down and away from the center of the higher altitudes to mix with saline water from the tidal rivers, bays, salt marshes, and the Atlantic Ocean. Fresh ground water from the Columbia aquifer also leaks down through the Yorktown confining unit into the upper half of the Yorktown-Eastover aquifer and flows within the Yorktown-Eastover above saline water in the lower half of the aquifer. Ground-water recharge is minimal in much of the southern watersheds because the land surface generally is low and flat.

Water-Resources Investigations Report↗
USGS2002

Conceptual hydrogeologic framework of the shallow aquifer system at Virginia Beach, Virginia

The hydrogeologic framework of the shallow aquifer system at Virginia Beach was revised to provide a better understanding of the distribution of fresh ground water, its potential use, and its susceptibility to contamination. The revised conceptual framework is based primarily on analyses of continuous cores and downhole geophysical logs collected at 7 sites to depths of approximately 200 ft. The shallow aquifer system at Virginia Beach is composed of the Columbia aquifer, the Yorktown confining unit, and the Yorktown-East-over aquifer. The shallow aquifer system is separated from deeper units by the continuous St. Marys confining unit. The Columbia aquifer is defined as the predominantly sandy surficial deposits above the Yorktown confining unit. The Yorktown confining unit is composed of a series of very fine sandy to silty clay units of various colors at or near the top of the Yorktown Formation. The Yorktown confining unit varies in thickness and in composition, but on a regional scale is a leaky confining unit. The Yorktown-Eastover aquifer is defined as the predominantly sandy deposits of the Yorktown Formation and the upper part of the Eastover Formation above the confining clays of the St. Marys Formation. The limited areal extent of highly permeable deposits containing freshwater in the Yorktown-Eastover aquifer precludes the installation of highly productive freshwater wells over most of the city. Some deposits of biofragmental sand or shell hashes in the Yorktown-Eastover aquifer can support high-capacity wells. A water sample was collected from each of 10 wells installed at 5 of the 7 core sites to determine the basic chemistry of the aquifer system. One shallow well and one deep well was installed at each site. Concentrations of chloride were higher in the water from the deeper well at each site. Concentrations of dissolved iron in all of the water samples were higher than the U.S. Environmental Protection Agency Secondary Drinking Water Regulations. Concentrations of manganese and chloride were higher than the Secondary Drinking Water Regulations in samples from some wells. In the humid climate of Virginia Beach, the periodic recharge of freshwater through the sand units of the shallow aquifer system occurs often enough to create a dynamic equilibrium whereby freshwater flows continually down and away from the center of the ridges to mix with and sweep brackish water and saltwater back toward the tidal rivers, bays, salt marshes, and the Atlantic Ocean. The aquifers and confining units of the shallow aquifer system at Virginia Beach are heterogeneous, discontinuous, and without exact marker beds, which makes correlations in the study area difficult. Investigations using well cuttings, spot cores, or split-spoon samples with geophysical logs are not as definitive as continuous cores for determining or correlating hydrogeologic units. Future investigations of the shallow aquifer system would benefit by collecting continuous cores.

Water-Resources Investigations Report↗
USGS2001

Ground-water flow in the shallow aquifer system at the Naval Weapons Station Yorktown, Virginia

The Environmental Directorate of the Naval Weapons Station Yorktown, Virginia, is concerned about possible contamination of ground water at the Station. Ground water at the Station flows through a shallow system of layered aquifers and leaky confining units. The units of the shallow aquifer system are the Columbia aquifer, the Cornwallis Cave confining unit, the Cornwallis Cave aquifer, the Yorktown confining unit, and the Yorktown-Eastover aquifer. The Eastover-Calvert confining unit separates the shallow aquifer system from deeper confined aquifers beneath the Station. A three-dimensional, finite-difference, ground-water flow model was used to simulate steady-state ground-water flow of the shallow aquifer system in and around the Station. The model simulated ground-water flow from the peninsular drainage divide that runs across the Lackey Plain near the southern end of the Station north to King Creek and the York River and south to Skiffes Creek and the James River. The model was calibrated by minimizing the root mean square error between 4 7 measured and corresponding simulated water levels. The calibrated model was used to determine the ground-water budget and general directions of ground-water flow. A particle-tracking routine was used with the calibrated model to estimate groundwater flow paths, flow rates, and traveltimes from selected sites at the Station. Simulated ground-water flow velocities of the Station-area model were small beneath the interstream areas of the Lackey Plain and Croaker Flat, but increased outward toward the streams and rivers where the hydraulic gradients are larger. If contaminants from the land surface entered the water table at or near the interstream areas of the Station, where hydraulic gradients are smaller, they would migrate more slowly than if they entered closer to the streams or the shores of the rivers where gradients commonly are larger. The ground-water flow simulations indicate that some ground water leaks downward from the water table to the Yorktown confining unit and, where the confining unit is absent, to the Yorktown-Eastover aquifer. The velocities of advective-driven contaminants would decrease considerably when entering the Yorktown confining unit because the hydraulic conductivity of the confining unit is small compared to that of the aquifers. Any contaminants that moved with advective ground-water flow near the groundwater divide of the Lackey Plain would move relatively slowly because the hydraulic gradients are small there. The direction in which the contaminants would move, however, would be determined by precisely where the contaminants entered the water table. The model was not designed to accurately simulate ground-water flow paths through local karst features. Beneath Croaker Flat, ground water flows downward through the Columbia aquifer and the Yorktown confining unit into the Yorktown-Eastover aquifer. Analyses of the movement of simulated particles from two adjacent sites at Croaker Flat indicated that ground-water flow paths were similar at first but diverged and discharged to different tributaries of Indian Field Creek or to the York River. These simulations indicate that complex and possibly divergent flow paths and traveltimes are possible at the Station. Although the Station-area model is not detailed enough to simulate ground-water flow at the scales commonly used to track and remediate contaminants at specific sites, general concepts about possible contaminant migration at the Station can be inferred from the simulations.

Virginia↗
USGS1999

The potential for saltwater intrusion in the Potomac aquifers of the York-James Peninsula, Virginia

The most productive aquifers of the Virginia Coastal Plain are in the Potomac Formation. Water supplies in the Potomac aquifers are impaired, however, by saltwater in some areas. A two-dimensional, densitydependent, solute-transport model was used to investigate saltwater movement in the Potomac aquifers and the potential for saltwater intrusion or upward migration of saltwater. The model was designed to represent a simplified section of the Potomac aquifers and associated confining units near Lee Hall, Va. Solute-transport simulations show that the direction of ground-water flow and the hydrogeologic properties, particularly the permeability of aquifers and the distribution of confining sediments in the Potomac Formation, control the system hydrodynamics and saltwater movement in the Potomac aquifers. The simulations indicate lateral intrusion for the Lower Potomac aquifer near Lee Hall, Va. Velocity vectors of the simulations indicate that a hypothetical, but typical, production well in the Middle Potomac aquifer could induce upconing only within the immediate vicinity of the well. Migration of saltwater from the Middle and Lower Potomac aquifers east of the hypothetical well also was indicated by the simulations.

Virginia↗
USGS1996

Hydrogeologic setting, hydraulic properties, and ground-water flow at the O-Field area of Aberdeen Proving Ground, Maryland

The U.S. Army disposed chemical agents, laboratory materials, and unexploded ordnance at O-Field in the Edgewood Area of Aberdeen Proving Ground, Maryland, from before World War II until at least the 1950's. Soil, ground water, surface water, and wetland sediments in the O-Field area were contaminated from the disposal activity. A ground-water-flow model of the O-Field area was constructed by the U.S. Geological Survey (USGS) in 1989 to simulate flow in the central and southern part of Gunpowder Neck. The USGS began an additional study of the contamination in the O-Field area in cooperation with the U.S. Army in 1990 to (1) further define the hydrogeologic framework of the O-Field area, (2) characterize the hydraulic properties of the aquifers and confining unit, and (3) define ground-water flow paths at O-Field on the basis of the current data and simulations of ground-water flow. A water-table aquifer, an upper confining unit, and an upper confined aquifer comprise the shallow ground-water system of the O-Field area. A lower confining unit, through which ground-water movement is negligible, is considered a lower boundary to the shallow system. These units are all part of the Pleistocene Talbot Formation. The model developed in the previous study was redesigned using the data collected during this study and emphasized New O-Field. The current steady-state model was calibrated to water levels of June 1993. The rate of ground-water flow calculated by the model was approximately 0.48 feet per day and the rate determined from chlorofluorocarbon dates was approximately 0.39 feet per day.

Maryland↗