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Search indexed USGS publications on groundwater, aquifers, geologic maps, mineral resources and earthquakes. Explore source records by subject and place.

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At least 1,009 records · Page 56Linked to original sources
USGS1976

Hydrogeology of a drift-filled bedrock valley near Lino Lakes, Anoka County, Minnesota

The bedrock surface of east-central Minnesota is dissected by an intricate network of valleys. Outside the bedrock valley at site B, 3 mi (4. 8 km) from site A, 100 ft (30 m) of drift overlies the bedrock surface. Observation wells were installed at the two sites to determine the vertical ground-water movement between the various aquifer units and the lateral movement between the two sites. An aquifer test of the lowest valley-fill aquifer at site A showed that the observation well completed in the same aquifer as the pumping well responded immediately; whereas a lag of about 100 min occurred between the lower valley fill and uppermost body of sand and gravel. This indicates that the hydraulic connection between these two layers is poor at the immediate site. Test results show that the lower sand-and-gravel aquifer has a transmissivity between 14,000 and 27,000 ft 2 /d (1,300 and 2,500 m 2 /d). Although the hydraulic gradient is vertically downward in the valley, much of the drift fill is poorly permeable. This suggests that the quantity of downward-percolating water reaching the lowest valley-fill aquifer is relatively small at the test site. Because valley cut through a number of bedrock aquifers in the region, they could potentially be an important avenue of contamination from land-surface waste. In addition, the vast network of bedrock valleys in the Twin Cities area might cause contaminants to disseminate rather rapidly throughout a large area.

Minnesota↗
USGS1978

Three-dimensional finite-difference model of ground-water system underlying the Muskegon County wastewater disposal system, Michigan

The spray irrigation system used by Muskegon County for wastewater treatment is the largest of its kind in the United States. It has 2200 hectares of irrigated farm land, 688 hectares of treatment lagoons, and 105 kilometers of drainage tile. The system has a design capacity of 1.8 cubic meters of wastewater per second. A three-dimensional finite-difference model was developed to study the effect of the disposal operation on ground-water conditions. Model calculations show that the water table at and adjacent to most of the wastewater site is lower as a result of the operation of the system to date. However, along the northwest boundary of the site, where irrigated land was not undertiled, the water table is 1 to 2 meters higher than it would be under natural conditions. Predictive simulations indicate that, even if the drainage tiles lost 75 percent of their effectiveness, the impact of disposal operations on ground-water levels would be negligible outside of the wastewater site.

Michigan↗
USGS1974

Time of travel and dye dosage for an irrigation canal system near Duchesne, Utah

Fracturing and subsidence of the land surface in the Milford area oil Utah have resulted from the decline of water levels due to pumping in unconsolidated deposits of Quaternary age. To the writers’ knowledge, these are the first such effects of ground-water withdrawal reported in Utah. The fracturing is in an area about 1 mile (1.6 km) wide and 11 miles (18 km) long near Milford, in an unsaturated clay-silt zone (locally peaty at top) in the upper part of the principal ground-water reservoir. The fractures range in length from several feet to more than 100 feet (30 m), and their maximum measured depth in 1972 was 4 feet (1.2 m). Land subsidence in the Milford area is demonstrated by three lines of evidence: (1) collapse structures, (2) well casings that protrude higher above the land surface than when first placed in the borehole, and (3) lower elevations at National Ocean Survey (formerly U.S. Coast and Geodetic Survey) bench marks in 1970 than in 1908. This evidence shows that land subsidence in the Milford area is of two types, each having a different origin. One type has a near-surface origin in the clay-silt zone in the upper part of the principal groundwater reservoir, and the other is in the lower artesian aquifers of the principal ground-water reservoir. The amount of observed subsidence ranges from 0.05 foot (0.015 m) at the bench mark at Read to about 6 feet (1.8 m) at collapse structures in the Hay Springs area.

Utah↗
USGS1978

Paleomagnetic evidence for a Late Cretaceous deformation of the Great Valley Sequence, Sacramento Valley, California

Paleomagnetic samples from five localities within the Great Valley sequence range in age from Late Jurassic to Late Cretaceous. All samples possess normal polarity, and alternating-field demagnetization experiments show that the remanence was acquired after the sequence was folded. A mean paleomagnetic pole position determined from 17 demagnetized samples is located at 72° N., 181° E., with the radius of the 95-percent circle of confidence equal to 5.4°. This pole position agrees very well with known Cretaceous poles from North America, a fact indicating that the deformation and remagnetization of the sequence must have occurred during the Late Cretaceous.

California↗
USGS1976

Cenozoic deposits of southeastern New Mexico and an outline of the history of evaporite dissolution

Sedimentary records of Cenozoic history in southeastern New Mexico begin with the Ogallala Formation of Miocene and Pliocene age. Later records include the Gatuna Formation of early or middle Pleistocene age, Mescalero caliche, an informal term, of middle Pleistocene age, and fluvial deposits of late Pleistocene age but there are many gaps in the record. The modern landscape is the result of erosion and deposition in climates that have ranged from semihumid to semiarid as well as dissolution of soluble rocks in Permian formations in the subsurface. This dissolution may have begun as early as Jurassic time and has continued intermittently to the present.

New Mexico↗
USGS1976

Bog stratigraphy, radiocarbon dates, and Pinedale to Holocene glacial history in the Front Range, Colorado

Radiocarbon dates and stratigraphic cores from bogs, kettle ponds, and former ice-marginal lakes on the east and west sides of the Front Range, Colo., between lat 40°00' and 40°24' N. suggest that (1) valley glaciers of Pinedale age began to recede from their terminal positions between about 14,600 and 13,000 yr ago, (2) revegetation of glaciated areas at altitudes of 2,600-2,900 m (8,600-9,500 ft) was complete by 11,000-10,000 yr ago, (3) at one site, 3,500±1,000 yr elapsed before peat began to form after deglaciation, (4) the formation of bogs within the glaciated areas kept pace with glacier recession in a general way, beginning at progressively later times as deglaciation proceeded upward, (5) Pinedale glaciers had disappeared or were reduced to small remnants by about 8,000 yr ago, (6) moraines that have been mapped as belonging to the early stade of Pinedale Glaciation are no younger than 13,000 yr B.P. and may be older than 14,600 yr, and those delimiting what has been mapped as late stade are no younger than about 7,600 yr B.P. and are probably older than 7,800 yr, and (7) most of the till mapped as Pinedale was deposited between about 14,600 and 8,000 yr ago.

Colorado↗
USGS1976

The volumetric properties of H2O — A graphical portrayal

A graphical display of the volumetric properties of H 2 O is presented as density (0.01 to 1.0 g-cm -3 ) contoured on pressure-temperature coordinates and pressure (1-10,000 bars) contoured on density-temperature coordinates over the temperature range 0-1,000 °C. Data were obtained from sources published during 1964-1969; several minor inconsistencies are observed and attributed to inadequacies in the equations of state used to describe experimental data obtained above 1,000 bars.

Journal of Research of the U.S. Geological Survey↗
USGS1976

The heat capacities at low temperatures and entropies at 298.15 K of low albite, analbite, microline, and high sanidine

The heat capacities of low albite and analbite, NaAlSi 3 O 8 , and of microcline and high sanidine, KAlSi 3 Og, have been measured from 15 to 375 K using an adiabatic calorimeter. Tables of the thermodynamic functions C° p , (H° T –H° 0 )/T, (G° T –H° 0 )/T, and S° T –S° 0 are presented for these four feldspars from 0 to 370 K. At 298.15 K (25.0°C) the values for S° T S° 0 for low albite, analbite, microcline, and high sanidine are 207.4±0.4, 207.7±0.4, 214.2±0.4, and 214.2±0.4 J/(mol . K), respectively. The effect of the state of Al/Si order upon the heat capacity is quite small. The difference, ΔC° p , between albite-analbite and microcline-sanidine never exceeds 0.5 percent at temperatures below 400 K. With the exception of microcline, the heat capacities of these four feldspars follow a smooth S-shaped curve between 15 and 375 K, with no indication of transitions or anomalous behavior. Above 250 K, the heat capacity of microcline shows a form of thermal hysteresis. In the temperature range 250 to 375 K, the heat capacity of microcline is dependent upon its past thermal history. At 375 K, microcline which had been cooled to 230 K before the measurement of C° p has a heat capacity greater by approximately 1.2 percent than microcline which had not been previously cooled below 295 K. After a day of annealing at about 300 K, C° p of the previously cooled microcline decreases to essentially the same value as the microcline which had never been at a temperature below 300 K.

Journal of Research of the U.S. Geological Survey↗
USGS1976

Definitive X-ray powder data for covellite, anilite, djurleite, and chalcocite

By using the Guinier-Hägg focusing X-ray powder camera with Cr Kα 1 and Cu Kα 1 radiations, new powder data for covellite (CuS), anilite (Cu 7 S 4 , djurleite (Cu 1.934 S), and low chalcocite (Cu 2 S) have been obtained from synthetic and natural materials. The powder data were treated by least-squares analysis to obtain the best unit-cell parameters consistent with the data. These powder data are intended to replace inferior and incomplete data previously published and to serve as standards for the study of copper sulflde minerals.

Journal of Research of the U.S. Geological Survey↗
USGS1976

Flameless atomic absorption determination of bismuth in soils and rocks

Recent advances in flameless atomic absorption allow determinations of bismuth in concentrations as small as 50 ppb in 0.2 g of rock or soil sample. The sample is fused with sodium bisulfate and the fusion product is leached with hot 2 M hydrochloric acid and treated with ammonium citrate, (ethylenedinitrilo) tetraacetic acid disodium salt, and finally with ammonium 1-pyrrolidinedithiocarbamate to form a complex which is extracted into methyl isobutyl ketone. Aliquots of the latter are pipetted into a graphite furnace and then subjected to an established and automated program of drying, charring, and atomizing. Recorded peak heights provide a measure of the amount of bismuth present.

Journal of Research of the U.S. Geological Survey↗
USGS1976

Interstation correlation of peak-flow estimates

Equations are given for using the correlation coefficient between annual peaks at a pair of stream gaging stations to estimate the interstation correlation coefficient of estimated T -year peaks, computed standard deviations, and computed skew coefficients at the same pair of stations. The equations are based on statistics computed from samples of annual peaks simulated from normal distributions with built-in interstation correlation. The interstation correlation of 50- year peaks was found to be about equal to the square of the interstation correlation coefficient of the annual peaks.

Journal of Research of the U.S. Geological Survey↗
USGS1976

Reassessment of mercury in surface water in the Adirondack region, New York

A study in 1970 established a natural background concentration of mercury in surface water in the Adirondack region of New York. In 1974, new methods of sample preservation and analysis were used in determining concentrations of mercury of samples of water from the same surface-water sites sampled in 1970-71. Concentrations of mercury for all sites in the 1974 study were virtually the same as those obtained in 1970-71, less than 0.5 microgram per litre, which is the detection limit of the methods.

New York↗