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At least 1,351 records · Page 75Linked to original sources
USGS1964

Chemical quality of surface water in the West Branch Susquehanna River basin, Pennsylvania

The West Branch Susquehanna River is 228 miles long and drains 6,913 square miles of mountainous area in central Pennsylvania. Much of this area is forestcovered wilderness, part of which is reserved as State game land. Wild animals, such as deer, bear, turkey and grouse, are sheltered there, and many streams contain trout and other game fish. This helps to make the region one of the best hunting and fishing areas in Pennsylvania. The Congress has approved Federal funds for the construction of several reservoirs to prevent flooding of the main river and several of its tributaries. Water stored behind the dams will not be withdrawn below a minimum level designated as conservation pools. These pools will be available for recreation. Several headwater streams, such as Clearfield, Moshannon, and at times Sinnemahoning Creek, that carry drainage from coal mines are acid and contain high concentrations of dissolved solids, especially sulfates. These streams acidify the West Branch Susquehanna River downstream as far as Jersey Shore. One of the most influential tributaries affecting the quality of the West Branch Susquehanna River after they merge is Bald Eagle Creek. Bald Eagle Creek enters the main river downstream from Lock Haven which is approximately 100 river miles from the river's source. Because of its alkaline properties, water of Bald Eagle Creek can neutralize acidic water. Many streams draining small areas and several draining large areas such as Pine Creek, Lycoming Creek, and Loyalsock Creek are clear nearly neutral water low in dissolved solids whose pH is about 7.0 most of the time. These streams have a diluting and neutralizing effect on the quality of the West Branch Susquehanna River, so that from Williamsport downstream the river water is rarely acid, and for most of the time it is of good chemical quality.

Pennsylvania↗
USGS1964

Hydrologic studies of small watersheds, Honey Creek basin, Collin and Grayson Counties, Texas, 1953-1959

This report presents the results of an investigation into the effects of floodwaterretarding structures in the 39 square miles of the Honey Creek basin above the stream-gaging station near McKinney, during the period October 1952 to September 1959. The number of such structures in the study area was increased from 2 to 12 during the investigation. Data were collected which permit computation of basin and watershed precipitation, inflow to and outflow from each floodwater-retarding structure, evaporation and seepage from each pool, and a continuous record of discharge from the entire study area. Transpiration was not evaluated, but in the water-budget summary it is included in the item "pool consumption", together with evaporation and seepage. During the 7-year study period, the annual inflow to the gaged pools ranged from 1.34 to 26.50 inches and averaged 7.39 inches, of which 0.73 inch was direct rainfall on the pool surface. The annual pool consumption ranged only from 1.33 to 1.85 inches, and averaged 1.62 inches. These results indicate that in a year of substantial runoff the floodwater-retarding structures would have only a minor effect on downstream water yield, but in a year of low runoff the structures would have a marked effect on downstream water yield. The effect on the flood regimen at a downstream point because of floodwaterretarding structures in the headwaters will vary with the amount and intensity of the precipitation and with antecedent conditions. The beneficial effects of the structures on Honey Creek during the floods of April and May 1957 is illustrative. During the period April 19 to May 31, 1957, the total volume of inflow to the floodwater-retarding structures was equivalent to 4.3 times the combined capacities of the pools from an average basin rainfall of 30.31 inches. The retarding effects of the structures limited the flooding on Honey Creek at the gage to minor flooding on only five occasions during that period.

Texas↗
USGS1964

Chemical quality of surface waters in the Brazos River basin in Texas

The Brazos River basin, which makes up 15 percent of the land area of Texas, extends from the High Plains, where altitudes reach 4,200 feet and the average precipitation ranges from 15 to 20 inches a year, to the Gulf of Mexico where the annual rainfall is 45-^50 inches. Large reservoirs have been built in the Brazos River basin, but the use of the stored water has been limited because the salinity often makes the water undesirable for municipal and industrial use. However, the water is generally satisfactory for irrigation. Records for the Brazos River show that the salinity of the water was a problem even as early as 1906 and that the water more often than not failed to meet today's chemical-quality standards for a municipal supply. The salt load of the Brazos River comes from the entire basin and is the result of solution, accretion of undetermined amounts of oil-field brine, and accretion of brine from springs and seeps such as those in Salt Croton Creek which contribute about 400 tons of chloride a day. Much of the salinity of the Brazos River is due to inflow of brines above Possum Kingdom Dam. The area above Possum Kingdom Dam is about 52 percent of the total area in the Brazos River basin but contributes only about 17 percent of the total runoff; however, about 50 percent of the annual salt load comes from this part of the basin. Quality-of-water records show a wide difference in the salinity of the steams in different parts of the basin, Dissolved-solids concentrations ranged from about 100 ppm (parts per million) for flood water to 300,000 ppm for saturated brines from springs. The quality of the surface water in the Brazos River basin is discussed by areas and by stream reaches. This study indicates that the water of the Salt Fork Brazos River is too saline for most uses. The water of the Double Mountain Fork Brazos River is less saline and might be used for irrigation; however, it probably could not be used as a municipal supply or as a supply for most industries. The water of the dear Fork Brazos River is generally good but is adversely affected by brine pollution. Chemical-quality records for the Lampasas, Leon, and Navasota Rivers indicate that the water of these streams is of excellent quality; however, more data are needed to determine variations. The quality of the water in other tributaries could only be inferred from the results of miscellaneous sampling and from the probable effect of the underlying rocks. The weighted-average concentration of constituents in the Brazos River at Richmond indicated that inflow below Whitney Reservoir has a dilution effect on the river. For 12 of the 14 years of record, the weighted-average dissolved-solids concentration of the Brazos River at Richmond was lessi than, the 500 ppm maximum limit recommended by the U.S. Public Health Service (1961). This study indicates that water stored in Possum Kingdom and Whitney Reservoirs tends to become stratified, with the more saline water being at the greater depths. Samples collected in 1956 at Whitney Reservoir showed that the chloride concentration at the bottom was almost twice that at the surface. After a flood in June 1957, the dissolved-solids concentrations of bottom releases at Possum Kingdom were almost double those of surface releases through the spillway even though the flood volume had been more than twice the capacity of the reservoir. The quality of water in the lower main stem can be improved by control and disposal of brines in the upper basin. Also, the maximum concentrations in the water of the lower main stem can be lowered by dilution with water stored in reservoirs on tributaries that yield water of good quality.

Water Supply Paper↗
USGS1964

Hydrology of aquifer systems in the Memphis area, Tennessee

The Memphis area as described in .this report comprises about 1,300 square miles of the Mississippi embayment part of the Gulf Coastal Plain. The area is underlain by as much as 3,000 feet of sediments ranging in age from Cretaceous through Quaternary. In 1960, 150 mgd (million gallons per day) of water was pumped from the principal aquifers. Municipal pumpage accounted for almost half of this amount, and industrial pumpage a little more than half. About 90 percent of the water used in the area is derived from the '500-foot' sand, and most of the remainder is from the ?400-foot' sand; both sands are of Eocene age. A small amount of water for domestic use is pumped from the terrace deposits of Pliocene and Pleistocene age. Both the '500-foot' and the '1,400-foot' sands are artesian aquifers except in the southeastern part of the area; there the water level in wells in the '500-foot' sand is now below the overlying confining clay. Water levels in both aquifers have declined almost continuously since pumping began, but the rate of decline has increased rapidly since 1940. Water-level decline in the '1,400-foot' sand has been less pronounced since 1956. The cones of depression in both aquifers have expanded and deepened as a result of the annual increases in pumping, and an increase in hydraulic gradients has induced a greater flow of water into the area. Approximately 135 mgd entered the Memphis area through the '500-foot' sand aquifer in 1960, and, of this amount, 60 mgd originated as inflow from the east and about 75 mgd was derived from leakage from the terrace deposits, from the north, south, and west and from other sources. Of the water entering the '1,400-foot' sand, about 5 mgd was inflow from the east, and about half that amount was from each of the north, south, and west directions. The average rate of movement of water outside the area of heavy withdrawals is about 70 feet per year in the '500-foot' sand and about 40 feet per year in the '1,400-foot' sand. The average rate of depletion of storage in each aquifer since pumping began is about 1 mgd. Most of the recharge to the '500-foot' and '1,400-foot' sands occurs in outcrop areas about 30-80 miles east of Memphis. Also, water leaks from the terrace deposits to the '500-foot' sand in some places, and there may be some leakage from streams where the confining clay is thin or is breached by faults or streams. The quality of water from both the principal aquifers is very good. Iron, carbon dioxide, and hydrogen sulfide are the only constituents found in undesirable quantities. Water from the terrace deposits is hard but generally contains less iron and carbon dioxide than water from either of the principal aquifers. The hydraulic characteristics of both aquifers were determined by pumping tests and by applying the knowledge of the geology o# the area; these characteristics indicate that the aquifers are capable of producing more water than is currently being pumped from them. The '500-foot' sand will produce more water per unit decline of water level than will the '1,400-foot' sand. There appears to be no reason why the development of water supplies from both aquifers should not continue, but well spacing will remain a factor which could affect future development. Greater well spacing will tend to prolong the useful life of a well and the aquifers.

Water Supply Paper↗
USGS1964

Geology and ground water of the Luke area, Maricopa County, Arizona

Luke Air Force Base, in the Salt River Valley in central Arizona. is within an intermontane basin--the Phoenix basin--in the Basin and Range lowlands province. The Luke area, the subject of this study, extends beyond the limits of the base. Ground-water resources of the Luke area were studied to determine the possibility of developing a water supply of optimum quantity and quality to supplement the base supply. Several wells drilled for this purpose, prior to the study, either produced an inadequate supply of water or produced ware-that had a high dissolved-solids content. The Phoenix basin is filled with unconsolidated to semiconsolidated Tertiary and Quaternary sedimentary rocks that are referred to as valley fill. Although its total thickness is unknown, 2,784 feet of valley fill--primarily consisting of clay, silt, sand, and gravel--has been penetrated. Percentage-distribution maps of fine-grained materials indicate a gross-facies pattern and a selective depositional area of the valley-fill materials. The maps also indicate that the areal distribution of fine-grained materials increases with depth. In general, the better producing wells, regardless of depth, are in areas where tee valley fill is composed of less than 60 percent fine-grained materials. The water table in the area is declining because large quantities of water are withdrawn and recharge is negligible. The decline near Luke Air Force Base during the period 1941-61 was about 150 feet. Ground water was moving generally southwest in the spring of 1961. Locally, changes in the direction of movement indicate diversion toward two major depressions. The dissolved-solids content of the ground water ranged from about 190 to 6,300 ppm. The highest concentration of dissolved solids is in water from the southern part of the area and seems to come from relatively shallow depths; wells in the northern part generally yield water of good quality. After a reconnaissance of the area, the U.S. Geological Survey located and supervised the drilling of two test wells--wells (B-2-1) 9bcb and (B-2-1) 5abc?on Luke Air Force Base. The quantity of water produced by the wells was adequate. The dissolved-solids content of water from the wells was low, and the overall quality of water from well (B-2-1) 5abc was good. When well (B-2-1) 9bcb was perforated between 907 and 977 feet, the water had a fluoride concentration of 4.4 ppm; however, the fluoride concentration decreased to 2.8 ppm when new perforations were cut at a shallower depth, and it was decided that dilution with other base water supplies probably would alleviate any possible fluoride problem.

Water Supply Paper↗
USGS1964

Evaluation of hydrogeology and hydrogeochemistry of Truckee Meadows area, Washoe County, Nevada

Practically all the ground water of economic importance in the Truckee Meadows area, an alluviated intermontane basin in western Nevada is in the valley fill, which consists of unconsolidated and partially consolidated sedimentary deposits. The Mesozoic and Cenozoic consolidated rocks of the mountains bordering the valley contain some water in fractures and other openings, but they have virtually no interstitial permeability. The permeability of the valley fill is extremely variable. The Truckee Formation, which is the oldest deposit of the valley fill, yields very little water to wells. Permeable lenses of sand and gravel in the valley fill that are younger than the Truckee Formation yield moderate to large amounts of water to wells. The estimated average annual recharge to and discharge from the groundwater reservoir is 35,000 acre-feet. About 25,000 acre-feet of the recharge is from the infiltration of irrigation water diverted from the Truckee River. Most of the discharge is by evapotranspiration and by seepage to ditches and streams. Some water in the area is unsuitable for many uses because of its poor chemical quality. Water in the Steamboat Springs area is hot and has high concentrations of chloride and dissolved solids. Both water draining areas of bleached rock and ground water downgradient from areas of leached rock have high concentrations of sulfate and dissolved solids. Surface water of low dissolved-solids content mixes with and dilutes some highly mineralized ground water. Increased pumping in discharge areas will help to alleviate waterlogged conditions and will decrease ground-water losses by evapotranspiration. Increased pumping near the Truckee River may induce recharge from the river to the ground-water system.

Water Supply Paper↗
USGS1964

The effect of artesian-pressure decline on confined aquifer systems and its relation to land subsidence

Ground water in the Southwestern United States is derived chiefly from unconsolidated to semiconsolidated alluvial deposits. Where these deposits contain confined water, they may be susceptible to compaction and related land- surface subsidence, if artesian pressures are reduced. Compaction of artesian-aquifer systems can be estimated from core tests if the artesian-pressure decline is known. Compaction occurs chiefly in the finer grained deposits ; porosity decrease is greater near the top of the confined aquifer than near the bottom. Because most of the compaction of these aquifer systems is permanent, the storage coefficient during the initial decline of artesian pressure greatly exceeds the storage coefficient during a subsequent pressure decline through the same depth range, after an intervening period of pressure recovery.

Water Supply Paper↗