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Maurice E. Cooley

Publications and source records attributed to Maurice E. Cooley.

10 recordsLinked to original sources
USGS1991

Geohydrology of the High Plains aquifer system, Cheyenne urban area, Wyoming

The Cheyenne area is on broad tablelands that form part of the High Plains aquifer. Surficial deposits, along with the Ogallala Formation and the White River Group, are included in the High Plains aquifer in the study area, and both unconfined and confined ground-water conditions exist within 100 feet of land surface. During wet years, shallow ground-water problems affect urban development. The High Plains aquifer is considered an aquifer system in the Cheyenne area. Water-yielding sandstone and conglomerate units are surrounded by sequences of clay and silt; although the water-yielding units under confined conditions may be areally extensive, they are not easily identified. Urban development has modified the High Plains aquifer system locally as indicated by the mapped potentiometric surfaces, the perched water zones, and the surface-drainage patterns. That part of the system in the shallow zones is affected by excavations and by structures that penetrate the saturated zones.

Wyoming↗
USGS1986

Divisions of potential fracture permeability, based on distribution of structures and lineaments, in sedimentary rocks of the Rocky Mountains-High Plains region, Western United States

The principal map show geologic structures and lineaments that indicate fracture traces in sedimentary rocks in all or parts of Arizona, Colorado, Kansas, Nebraska, New Mexico, Oklahoma, South Dakota, Texas, Utah, and Wyoming. Fractures associated with geologic structures and lineaments may affect the potential fracture permeability of consolidated rocks. Divisions indicating differences in the potential fracture permeability are delineated on the map.

Arizona, Colorado, Kansas, Nebraska, New Mexico, O↗
USGS1986

Artesian pressures and water quality in Paleozoic aquifers in the Ten Sleep area of the Bighorn Basin, north-central Wyoming

The major Paleozoic artesian aquifers, the aquifers most favorable for continued development, in the Ten Sleep area of the Bighorn Basin of Wyoming are the Tensleep Sandstone, the Madison Limestone and Bighorn Dolomite (Madison-Bighorn aquifer), and the Flathead Sandstone. The minor aquifers include the Goose Egg and Park City Formations (considered in the Ten Sleep area to be the lateral equivalent of the Phosphoria Formation) and the Amsden Formation. Most wells completed in the major and minor aquifers flow at the land surface. Wellhead pressures generally are less than 50 pounds per square inch for the Tensleep Sandstone, 150-250 pounds per square inch for the Madison-Bighorn aquifer, and more than 400 pounds per square inch for the Flathead Sandstone. Flowing wells completed in the Madison-Bighorn aquifer and the Flathead Sandstone yield more than 1,000 gallons per minute. The initial test of one well completed in the Madison-Bighorn aquifer indicated a flow rate of 14,000 gallons per minute. Transmissivities range from 500 to 1,900 feet squared per day for the Madison-Bighorn aquifer and from about 90 to 325 feet squared per day for the Tensleep and Flathead Sandstones. Significant secondary permeability from fracturing in the Paleozoic aquifers allows local upward interformational movement of water, and this affects the altitude of the potentiometric surfaces of the Tensleep Sandstone and the Madison-Bighorn aquifer. Water moves upward from the Tensleep and other formations, through the Goose Egg Formation, to discharge at the land surface as springs. Much of the spring flow is diverted for irrigation or is used for rearing fish. Decreases from original well pressures were not apparent in wells completed in the Tensleep Sandstone or in the Madison-Bighorn aquifer in the study area except for a few wells in or near the town of Ten Sleep. Most wells completed in the Flathead Sandstone, which also are open to the Madison-Bighorn aquifer, show a decrease of pressure from the time of completion to 1978. The decrease of pressure is partly the result of water moving from the Flathead Sandstone into the Madison-Bighorn aquifer, which has a lower potentiometric surface than does the Flathead Sandstone, even during the time the wells are not in operation. Pressure in some small-capacity wells completed in the Goose Egg Formation also has decreased near Ten Sleep. Most of the wells, particularly the irrigation wells, show a progressive decrease in pressure during the irrigation season but recover during periods of nonuse. Measurements of the pressure were made principally in 1953, 1962, 1970, and 1975-78. Well water from the Paleozoic aquifers generally contains minimal concentrations of dissolved solids and individual constituents but excessive hardness. Dissolved-solids concentrations of water are less than 300 milligrams per liter in the Tensleep Sandstone and the Madison-Bighorn aquifer, less than 200 milligrams per liter in the Flathead Sandstone, and as much as 450 milligrams per liter in the Goose Egg Formation. Bicarbonate is the major constituent, followed by calcium and magnesium. Relatively large concentrations of sulfate, as much as 490 milligrams per liter, were found, mainly in water from the Goose Egg Formation. The water has low sodium (alkali) and medium salinity; therefore, the water is satisfactory for irrigation and most other uses, if excessive hardness is not a detrimental factor. Wellhead temperatures range from 11 ? to 27.5 ? Celsius (51 ? to 81.5 ? Fahrenheit) within a range in depth of approximately 250 to 4,000 feet. This gives a geothermal gradient of about 0.44 ? Celsius per 100 feet (0.79 ? Fahrenheit per 100 feet).

Water Supply Paper↗
USGS1979

Effects of uranium development on erosion and associated sedimentation in southern San Juan Basin, New Mexico

A reconnaissance was made of some of the effects of uranium development on erosion and associated sedimentation in the southern San Juan Basin, where uranium development is concentrated. In general, the effects of exploration on erosion are minor, although erosion may be accelerated by the building of access roads, by activities at the drilling sites, and by close concentration of drilling sites. Areas where the greatest effects on erosion and sedimentation from mining and milling operations have occurred are: (1) in the immediate vicinity of mines and mills, (2) near waste piles, and (3) in stream channels where modifications, such as changes in depth have been caused by discharge of excess mine and mill water. Collapse of tailings piles could result in localized but excessive erosion and sedimentation.

Open-File Report↗
USGS1979

Regional geohydrology of the San Juan hydrologic basin of New Mexico, Colorado, Arizona, and Utah

The San Juan Basin in the southeastern part of the Colorado Plateau, southwest of the San Juan Mountains, broadly includes the Acoma and Gallup Sags in its southern part and the small Chama Basin in its northeastern part. Regionally, the water-yielding strata (aquifers) dip inward toward the center of San Juan Basin or toward the axes of the adjoining structural sags. Aquifers exposed or at shallow depths along the margin of the basin are deeply buried in the center of the basin. The occurrence and movement of ground water is strongly influenced by the structural configuration of the basin; fractures along joints and faults, particularly the Puerco fault belt; distribution and lithology of the rock strata, and the relationship of the uplands recharge areas of the aquifers to the lowland areas where the most ground-water discharges. The aggregate thickness of sedimentary rocks is more than 10,000 feet in the deepest part of the basin. In order of decreasing abundance, these rocks consist of mudstone, claystone, siltstone, sandstone, silty sandstone, coal, limestone, conglomerate, and gypsum. The main aquifers consist of sandstone or sandstone containing lenses of conglomerate except for the San Andres Limestone. The principal aquifers, listed in descending stratigraphic order, are the Tertiary Cuba Mesa and Llaves Members of the San Jose Formation and the Ojo Alamo Sandstone; the Pictured Cliffs, Cliff House, Point Lookout, Gallup, and Dakota Sandstones; the Westwater Canyon and Salt Wash Sandstone Members of the Morrison Formation, the Cow Springs Sandstone, the Zuni Sandstone, and the Entrada Sandstone; and the San Andres Limestone, Glorieta Sandstone, and De Chelly Sandstone. These aquifer are separated by formations, that do not readily transmit water between the aquifers. Regional movement of ground water is mainly to the San Juan and Chaco s Rivers, the Puerco River, the Rio Puerco, and their main tributaries. Ground water from aquifers overlying the Dakota Sandstone discharge within the confines of the San Juan hydrologic basin. Part of the ground water in the Dakota Sandstone, Morrison Formation, and underlying formations moves across the interbasin divide into the Black Mesa, the Blanding Basin, or to the Rio Grande Trough.

Arizona, Colorado, New Mexico, Utah↗
USGS1979

Depths of channels in the area of the San Juan Basin Regional Uranium Study, New Mexico, Colorado, Arizona, and Utah

During December 1977 and January 1978 about 280 measurements were made of the depths of channels (arroyos) more than 6 feet deep in the San Juan Basin area. More than half of the measurements were made at sites where channel depths had been previously measured Between 1964 and 1969. Some channels in the western part of the basin had Been re-measured in 1969 and in 1971. The principal areas Being dissected by arroyos are near highlands along the margins of the Basin and in uplands in the northeastern part of the Basin. The most severe dissection by arroyos and the deepest arroyos--commonly Between 40 and 60 feet deep--are in the southeastern part of the Basin. Dissection By arroyos is least in the central part of the Basin near the Chaco River where most arroyos are less than 10 feet deep. Elsewhere, moderate dissection predominates with most arroyos Between 12 and 40 feet deep. Comparison of measurements made from 1964-71 with those made in 1977-78 shows that more channels in the western San Juan Basin were filling than were downcutting. Downcutting or filling was generally less than 2 feet. About two-fifths of the sites measured showed less than half a foot of downcutting or filling. Maximum downcutting was 4 feet along the Rio San Jose in the southeastern part of the basin. Maximum filling of 7 feet was along the Chaco River at the Chaco Canyon National Monument. Along ii other streams elsewhere in the western part of the basin, channels were filled 3 to 4.5 feet. The few measurements made in the southeastern San Juan Basin indicate that since 1964 downcutting has predominated over filling. Large floods during the summer of 1977 caused some change in channel depths in the southwestern part of the San Juan Basin. Some of the channels appeared to have been filled during the years prior to the cutting that occurred from the 1977 floods. At other places, flood flows aggraded (filled) channels. The rate of erosion and arroyo formation in the entire San Juan Basin is effected by man. The southeastern part of the basin--having been occupied by man for several centuries--shows the greatest effects of man on the rate of arroyo formation. Recent urban developments, particularly near Gallup, also appear to have affected the rate of erosion and arroyo formation. In contrast, arroyos appear to be aggrading below many earth-fill dams. In general, the effects of the petroleum, coal, and uranium exploration and development on arroyo formation have been minimal because the main trenching of the arroyos predates oil and mining operations. Some modification--degradation or aggradation--of the arroyos and local trenching of new arroyos have taken place in the area of some of the mines. Most of the observed effects from the mining operations on erosion and aggradation relate to the discharge of mine and mill water into the nearby streams.

Open-File Report↗
USGS1978

Floods of September 1970 in Arizona, Utah, Colorado, and New Mexico

During September 5-7, 1970, unusually large floods occurred in the mountains of central Arizona and in the Four Corners area of Arizona, Utah, Colorado, and New Mexico. Flooding also occurred in southern and northeastern Arizona. The record-high rainfall of September 5 occurred when a mass of moist tropical air from Pacific storm Norma collided with a cold front from the northwest. A new 24-hour precipitation record of 11.40 inches (290 millimeters) was established for Arizona, and new 12- and 24-hour precipitation records of 6.0 inches (152 millimeters) were established for Utah. The flood took the lives of 23 persons and was reported to have caused about $8.4 million in damage in Arizona. The main area of flooding was in the mountains in central Arizona. The flood generally was less destructive with increasing distance downstream; in the Salt and Verde River basins the reservoirs were capable of storing all the floodwater. Flooding in the Dolores and San Juan River basins in the Four Corners area was mostly in rural areas, and two people were drowned in McElmo Creek in Utah. The flood was not as large as that of October 1911, which is the largest known flood in the area. A second storm occurred in the Four Corners area September 12-14; however, the amount of flooding generally was less than that from the previous storm. Flood damage as a result of the two storms was reported to be about $2.9 million.

Arizona, Colorado, New Mexico, Utah↗
USGS1977

Effects of the catastrophic flood of December 1966, north rim area, eastern Grand Canyon, Arizona

Precipitation from the unusual storm of December 1966 was concentrated on highlands in northern Arizona, southwestern Utah , southern Nevada, and south-central California and caused widely scattered major floods in the four States. In Arizona the largest amount of precipitation was in the north rim area of eastern Grand Canyon, where about 14 inches was measured. The largest flows occurred along Bright Angel Creek and the MilK Creek-Dragon Creek part of the Crystal Creek drainage basin. The maximum effects of the flood were along Milk Creek-Dragon Creek, where a mudflow caused extensive channel modification. Floods that occurred in the Bright Angel and Crystal Creek basins have a recurrence interval of only once in several centuries. The streamflow that resulted from the storm on the Kaibab Plateau caused considerable local scouring and deepening of channels, including some renewed arroyo cutting. The most catastrophic effects of the 1966 floods were caused by two mudflows that extended from the edge of the Kaibab Plateau along Dragon Creek in the Crystal Creek basin and Lava Creek in the Chuar Creek basin to the Colorado River. More than 10 other large mudflows occurred in Nankoweap, Kwagunt, Crystal, and Shinumo Creek basins. About 80 large debris slides left conspicuous scars in the amphitheaters at the heads of the side gorges, and at least 10 small slides occurred on the Kaibab Plateau. (Woodard-USGS)

Professional Paper↗
USGS1973

Salt deposits in Los Medanos area, Eddy and Lea Counties, New Mexico

The salt deposits of Los Medanos area, in Eddy and Lea Counties, southeastern New Mexico, are being considered for possible use as a receptacle for radioactive wastes in a pilot-plant repository. The salt deposits of the area. are in three evaporite formations: the Castile, Salado, and Rustler Formations, in ascending order. The three formations are dominantly anhydrite and rock salt, but some gypsum, potassium ores, carbonate rock, and fine-grained clastic rocks are present. They have combined thicknesses of slightly more than 4,000 feet, of which roughly one-half belongs to the Salado. Both the Castile and the Rustler are-richer in anhydrite-and poorer in rock salt-than the Salado, and they provide this salt-rich formation with considerable Protection from any fluids which might be present in underlying or overlying rocks. The Salado Formation contains many thick seams of rock salt at moderate depths below the surface. The rock salt has a substantial cover of well-consolidated rocks, and it is very little deformed structurally. Certain geological details essential for Waste-storage purposes are unknown or poorly known, and additional study involving drilling is required to identify seams of rock salt suitable for storage purposes and to establish critical details of their chemistry, stratigraphy, and structure.

New Mexico↗