Geology topics

Joe B. Gillespie

Publications and source records attributed to Joe B. Gillespie.

5 recordsLinked to original sources

USGS1996

Hydrologic and chemical interaction of the Arkansas River and the Equus Beds aquifer between Hutchinson and Wichita, south-central Kansas

Large chloride concentrations in Arkansas River water have the potential to degrade water quality in the adjacent Equus beds aquifer between Hutchinson and Wichita, Kansas. The aquifer is an important source of water for municipal, industrial, agricultural, and domestic uses. A three-dimensional, finite-difference, ground-water flow-model program (MODFLOW) was used with data from past studies and data collected during 1988-91 to simulate aquifer and stream conditions during the late 1930's, during 1940-89, and during 1990-2019. Results of ground-water flow-model simulations indicated that declining water levels in the Equus beds aquifer since the 1940's have caused base flow in the Arkansas and Little Arkansas Rivers to decrease. In 1940, the Arkansas and Little Arkansas Rivers had simulated net base-flow gains within the model area of about 21 and about 67 ft 3 /s (cubic feet per second), respectively. By the end of 1989, the Arkansas River had a simulated net base-flow loss of about 52 ft 3 /s, and the Little Arkansas River had a net base-flow gain of about 27 ft 3 /s. Simulations for 1990-2019 showed that the water-level changes in a selected model cell located in the central part of the Wichita well field could range from -0.2 to -78 feet. Waterlevel changes in a selected model cell located near the Arkansas River could range from +1.3 to -1.2 feet. In model simulations where only pumpage varied, net base-flow loss from the Arkansas River to the aquifer ranged from about 59 ft 3 /s (no increase in pumpage since 1989) to 117 ft 3 /s (a 3-percent per year increase in pumpage since 1989) by 2019. Assuming a chloride concentration of 630 milligrams per liter, the median concentration in Arkansas River water collected during 1988-91, the quantity of chloride discharged from the Arkansas River to the aquifer was estimated to have increased from about 21 tons per day in 1940 to about 100 tons per day in 1989. By 2019, chloride discharge was indicated to range from about 110 tons per day (associated with no increase in pumpage since 1989) to 200 tons per day (associated with a 3-percent per year increase in pumpage since 1989). A particle-tracking program (MODPATH), which used the results from the flow model, was used to simulate the distribution in the aquifer of chloride from the river during the same time periods. Particle-tracking simulations show that, during 1940-89, the simulated distribution of particles representing chloride from the Arkansas River expanded from relatively narrow bands near the river to a wider distribution within the aquifer and the Wichita well field. Particle-tracking simulations indicate that chloride discharge from the Arkansas River may have reached the edge of the Wichita well field as early as 1963.

Kansas↗

USGS1994

Geohydrology and saline ground-water discharge to the South Fork Ninnescah River in Pratt and Kingman Counties, south-central Kansas

Saline ground water discharges to the South Fork Ninnescah River in Pratt and Kingman Counties from the adjacent alluvial aquifer. Electromagnetic terrain surveys in this area indicated that the saline ground water is entering the river in intermittent reaches along the channel. The chloride concentration in the river near Murdock exceeds 250 milligrams per liter 75 percent of the time. During base flow in November 1988, stream discharge increased 67 cubic feet per second, and the chloride concentration increased 360 milligrams per liter from Pratt to the Pratt-Kingman County line. The chloride load to the river along this reach was 82 tons per day. The source of saline water probably is dissolution of salt in the Permian rocks, about 600 feet below land surface. Subsequent subsidence and collapse of Permian rocks into salt-dissolution cavities probably has caused fracturing in overlying Permian rocks. Brine moves upward through the Permian rocks and discharges into the alluvial aquifer. The brine discharge to the alluvium is about 0.7 cubic foot per second. In the area of major saline-water discharge to the river, the fluid-potential levels in the Permian rocks are higher than fluid-potential levels in the alluvial aquifer. Several methods for reducing the saline ground-water discharge to the South Fork Ninnescah River have been considered. The most effective of these methods appears to be interception of brine flow in the Permian rocks by pumping of relief wells. Brine could be disposed by injection into deeper formations, by storage in evaporation reservoirs, or by desalinization.

Water-Resources Investigations Report↗

USGS1986

Geohydrology of the Wellington-alluvial aquifer system and evaluation of possible locations of relief wells to decrease saline ground-water discharge to the Smoky Hill and Solomon rivers, central Kansas

Saline water discharges from the alluvial aquifer into the Smoky Hill and Solomon Rivers between New Cambria and Solomon in central Kansas. Chloride concentrations in the Smoky Hill River sometimes exceed 1,000 mg/L during low flow conditions. The source of saline water is the underlying Wellington aquifer, a zone of halite and gypsum dissolution, subsidence, and collapse along the eastern margin of the Permian Hutchinson Salt Member of the Wellington Formation. Locally, brine from the Wellington aquifer flows upward through collapse structures in the confining layer into the overlying alluvium. Estimated brine discharge averages about 0.8 cu ft/sec. Control of the saline groundwater discharge to the Smoky Hill and Solomon Rivers is desirable to improve the quality of water in the rivers. The upward discharge of natural brine into the alluvium could be partly controlled by relief wells installed in the Wellington aquifer. The wells need to be located in the area of greatest saline groundwater discharge to the rivers and near the eastern end of the Wellington aquifer between New Cambria and Solomon. The relief wells could be pumped just enough to reverse the hydraulic gradient between the Wellington and alluvial aquifers, decreasing the upward flow of brine into the alluvium and, into the rivers. The brine could be disposed into brine aquifers underlying the area at depth or pumped into surface evaporation-storage reservoirs. (Author 's abstract)

Water-Resources Investigations Report↗

USGS1981

Saline ground-water discharge to the Smoky Hill River between Salina and Abilene, central Kansas

Saline water discharges from the alluvial aquifer into the Smoky Hill and Solomon Rivers between New Cambria and Sand Springs, Kansas. During relatively stable base flow in 1976-77, the discharge was about 32 cubic feet per second. Chloride concentrations at base flow increased about 800 milligrams per liter in the Smoky Hill River and 550 milligrams per liter in the Solomon River. The source of the saline water is the underlying Wellington aquifer, a zone of dissolution, subsidence, and collapse along the eastern margin of the Wellington Formation. Locally, brine from the aquifer moves upward through collapse structures in the confining layer at the base of the alluvium. The brine discharge ranges from 0.3 to 0.8 cubic foot per second, and the chloride load ranges from 150 to 370 tons per day. Results from a mathematical model of the fl ow system indicated that recharge from periodic flooding, as in 1973, was sufficient to reverse the normal (197677) hydraulic gradient between aquifers. Although brine discharge was temporarily reduced, saline-water discharge to the rivers increased. The discharge of brine could be intercepted by pumping wells completed in the Wellington aquifer to lower the potentiometric head and reduce upward flow. The intercepted brine could be discharged into formations underlying the area at depth or piped to a storage reservoir from which the brine would be evaporated or released to the rivers during peak flows. Also, the freshwater in upstream base flow could be diverted by canal, and the saline-water discharge could be retained by low-head dams in the river channel for release during peak flows.

Kansas↗

USGS1976

Results of infiltration tests near Scott City, western Kansas

Several types of ring infiltrometers were used to determine infiltration rates in loessial soil near Scott City, Kansas. Test results were evaluated for consistency, and were compared with infiltration rates in the underlying loess and with hydraulic conductivities in the unsaturated zone. Average daily infiltration rates in the Richfield soil ranged from 3 to 5 feet or 0.9 to 1.5 m (metres) after 16 days using 22-inch or 560mm (millimetre) ring infiltrometers; 2.3 feet (0.7 m) after 68 days using a 10-inch (250-mm) ring infiltrometer; and from 1.3 to 2.2 feet (0.4 to 0.7 m) after 38 days using double-ring infiltrometers. By comparison, the average daily infiltration rate in the underlying Peoria Loess using a 10-inch (250-mm) ring infiltrometer was about 13 feet (4.0 m) after 7 days. Tests using the double-ring infiltrometer, a paraffin seal in the 22-inch (560-mm) infiltrometer, and the measurement of flow through concentric areas of the soil core indicated that leakage of water between the infiltrometer wall and the soil was not significant. Lateral movement of the wetting front extended radially 4.7 feet (1.4 m) from the infiltrometer wall. Laboratory tests of a soil core indicated that the lowest hydraulic conductivity was in the depth interval from 3.9 to 8.6 inches (99 to 218 mm). Soil in this interval, which coincides with the depth of cultivation, evidently limits the rate of infiltration. Air-permeability tests in the unsaturated deposits gave a hydraulic conductivity of 0.2 foot per day (0.1 m/day) for the depth interval from 57 to 75 feet (17.0 to 23.0 m) as compared to a hydraulic conductivity of 1.9 feet per day (0.6 m/day) for the depth interval from 0 to 5 feet (0 to 1.5 m). A perched water table probably would occur above this interval during prolonged infiltration. Infiltration rates determined from the different types of ring infiltrometers were not consistent, but the tests showed that substantial quantities of water could infiltrate the Richfield soil.

Kansas↗