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Dr. Gilbert White is Director of the Institute of Behavioral Science at the University of Colorado, Boulder, where he is responsible for natural Hazards Research and Applications Information Center supported by the National Science Foundation. He served in the Executive Office of the president in 1941-42, on the Federal Flood Control Policy Task Force in 1964-65, and on the U.S Geological Survey Advisory Panel on Earthquake Studies. Dr. White has authored five books on the social and economic aspects of natural resources, including water supply and river development, and on floods and other natural hazards.
Griggs and Steele Counties, in east-central North Dakota, are underlain by bedrock of Ordovician, Jurassic, and Cretaceous ages. The Fall River and Lakota Formations of Cretaceous age form the Dakota aquifer. The fractured upper part of the Pierre Formation (shale), also of Cretaceous age, forms another bedrock aquifer. The Dakota aquifer, which consists mainly of interbedded shale and sandstone units, may yield as much as 500 gallons per minute (32 liters per second) of sodium sulfate water to wells at selected locations. The Pierre aquifer yields from 1 to 10 gallons per minute (0.06 to 0.63 liters per second) of sodium bicarbonate or sodium sulfate water to wells. Four major glacial-drift aquifers are present in the study area. The Spiritwood aquifer system may supply as much as 1,500 gallons per minute (95 liters per second) of water to wells. Water samples contained dissolved-solids concentrations ranging from 244 to 9,800 milligrams per liter. The Galesburg aquifer will yield as much as 1,000 gallons per minute (63 liters per second) of water to wells. Water samples contained dissolved-solids concentrations ranging from 317 to 2,170 milligrams per liter. The McVille aquifer will yield as much as 500 gallons per minute (32 liters per second) to wells. Water samples contained dissolved-solids concentrations ranging from 449 to 2,200 milligrams per liter. The Elk Valley aquifer could yield 30 gallons per minute (2 liters per second) to wells. Water samples contained dissolved-solids concentrations ranging from 397 to 2,890 milligrams per liter. Six communities in the project area use ground-water supplies. Rural water districts are being developed in the two-county area that will provide dependable ground-water supplies for many farms and small municipalities. The Spiritwood aquifer system and the McVille and Galesburg aquifers are capable of supplying the water needs of these districts and could also provide water for irrigation.
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Water production from individual oil wells in the Uinta Basin ranges from 0 to 2,920,000 barrels (about 380 acre-feet) per year. The total dissolved solids in the water ranges from 500 to 26,000 ppm (parts per million); thus some of the water is classified as fresh and can be used, whereas the highly mineralized water, a minor percentage of the total water produced in the Uinta Basin, must be disposed of to prevent pollution of local fresh-water supplies.
Historical records of streamflow for an eastward- and a westward-draining stream in the northern Sierra Nevada have been analyzed for evidence of changes in runoff characteristics and patterns of variability. A trend of increasing and more variable winter streamflow began in the mid-1960s. Mean monthly streamflow during December through March was substantially greater for water years 1965-1990 compared to water years 1939-1964. Increased winter and early-spring streamflow during the later period is attributed to small increases in temperature, which increase the rain-to-snow ratio at lower altitudes and cause the snowpack to melt earlier in the season at higher altitudes. The timing of snowmelt runoff on the western slope of the Sierra Nevada is more sensitive than it is on the eastern slope to changes in temperature, owing to predominantly lower altitudes on the west side. This difference in sensitivity suggests that basins on the east side of the Sierra Nevada have a more reliable water supply (as snow storage) than western-slope basins during warming trends.
This report presents a summary of conclusions reached from the recently completed State Engineer-United States Geological Survey cooperative investigation of the geology and ground water resources of the central Sevier River Valley. The detailed report will be published as a United States Geological Survey water supply paper and will be available to the public.
Many Federal, State, and local agencies use low-flow data to establish water-use policy and help determine the total maximum daily loads and effluent limits of point and nonpoint sources of contamination of surface water during periods of decreased streamflow. Low-flow magnitude and frequency are used often by water-supply planners, reservoir managers, and hydroelectric facilities to manage water availability for supply and power generation. Low-flow statistics for eight selected U.S. Geological Survey streamgages in New York State were calculated for the period from 1976 through 2006 and for the entire period of continuous streamflow record. The 7-day, 2-year and 10-year low flows were computed and compared with those low flows published in the1979 U.S. Geological Survey report, Low-flow frequency analysis of streams in New York, Bulletin 74. Observed changes in low-flow frequency at each gage were then examined and compared to changes in precipitation and land use to determine whether a relation between similar patterns could be identified. A statewide U.S. Geological Survey study has not been done to develop equations for estimating low flows on rural unregulated streams in New York. Currently (2010) only one regional study developed for parts of the lower Hudson River Basin in 1986 is available to assist in estimating low flows on rural streams with unregulated streamflow in New York. Low-flow statistics published in the 1979 report need to be updated by using additional data collected since 1976 to determine current low-flow conditions across New York State. At-site low-flow statistics were updated for eight streamgages in New York by using continuous daily streamflow data through 2006 for the future development of a statewide research study. Selection of the eight streamgages used in this study identified a major deficiency in the number of available unregulated long-term U.S. Geological Survey streamgages needed for the development of regional low-flow equations in New York. A limited analysis of the changes in land use for the contributing drainage areas for each streamgage, changes in precipitation, and trends in the annual 7-day minimum flow also are presented. The 7-day, 2-year low flow showed increases of 14 to 35 percent and the 7-day 10-year low flow showed zero to 19 percent increases at rural streamgages with unregulated streamflows when statistics were computed by using data from 1976 through 2006 and compared with published data in Bulletin 74. When the entire period of record was used to compute low flow frequencies, the 7-day, 2-year low flows increased from about 6 to 15 percent whereas the 7-day 10-year low flows showed zero to 5 percent increases. Streamgages affected by urbanization and regulation for water supply showed the most significant changes in the 7-day, 2-year and 10-year low-flow frequencies. These streamgages are included to help identify the effects of urbanization and regulation on streamflow at these locations. The 7-day 10-year low flow increased by 65 percent at the U.S. Geological Survey streamgage Hackensack River at West Nyack, N.Y., and increased 120 percent at the U.S. Geological Survey streamgage Neversink River at Godeffroy, N.Y., when statistics were computed by using data from 1976 through 2006 and compared with the statistics for the regulated period computed in Bulletin 74.
The population status of the Everglade Kite (Rostrhamus sociabils plumbeus) was studied in Florida from 1968 through 1978. Sixty-four nestlings (40% of known fledged young) were leg-banded with unique color combinations, and of these, 17.2% were seen 1 or more years after they were banded. Kites were capable of breeding at 3 years of age or possibly younger. The population was nomadic; its sex ratio unknown. From 1968 through 1976 breeding success was determined for 175 nests, of which 48% were successful: 161 young were fledged, x = 20.1 per year, or 1.9 per successful nest (N = 84). The percentage of successful nests ranged from 17.1 (N = 35) in 1974 to 84.6 (N = 13) in 1968 (x= 54.1 per year). From 1968 through 1976 there was a significant increase (r = 0.685, P < 0.05) in the number of nests ohserved (excluding 1971, and reproduction was not studied in 1977 and 1978). The mortality rate for young in the nest was 41%. Some individuals live for at least 8+ years. The mean number of kites for 10 annual censuses was 120.2 with a range of 65 (1972) to 267 (1978). The severe drought of 1971 resulted in a significant decrease in the population for that year and 1972, with no nesting attempts being observed in the dry year. From 1974 through 1978 the population increased significantly (r = 0.92, P < 0.025), apparently the result of favorable water conditions and increased food supply. The loss of suitable habitat is the major problem facing the species in Florida. A high water level is essential, as this affects food supply and its availability, as well as nesting success.
The Quinnipiac River basin area in southcentral Connecticut covers 363 square miles, and includes all drainage basins that enter Long Island Sound from the Branford to the Wepawaug Rivers. Its population in 1970 was estimated at 535,000. Precipitation averages 47 inches per year and provides an abundant supply of water. Twenty-one inches returns to the atmosphere as evapotranspiration; the remainder flows directly to streams or percolates to the water table and discharges to Long Island Sound. Small amounts of water are exported from the basin by the New Britain Water Department, and small amounts are imported to the basin by the New Haven Water Company. The amount of water that can be developed at a given place depends upon precipitation, variability of streamflow, hydraulic properties and areal extent of the aquifers, and hydraulic connection between the aquifers and major streams. The quality of the water is determined by the physical environment and the effects of man. Stratified drift is the only aquifer capable of large sustained yields of water to individual wells. Yields of 64 screened wells tapping stratified drift range from 17 to 2,000 gpm (gallons per minute); their median yield is 500 gpm. Till is widespread and generally provides only small amounts of water. Wells in till normally yield only a few hundred gallons of water daily and commonly are inadequate during dry periods. Till is generally used only as an emergency or secondary source of water. Bedrock aquifers underlie the entire report area and include sedimentary, igneous, and metamorphic rock types. These aquifers supply small but reliable quantities of water to wells throughout the basin and are the chief source for many nonurban homes and farms. About 90 percent of the wells tapping bedrock yield at least 2 pgm, and much larger yields are occasionally reported. Maximum well yields of 305 gpm for sedimentary, 75 gpm for igneous, and 200 gpm for metamorphic bedrock have been reported. Water potentially available from stratified drift was estimated on the basis of hydraulic characteristics of the aquifers and evaluation of natural and induced recharge. Long-term yields estimated for 14 favorable areas of stratified drift range from 0.8 to 16.1 mgd (million gallons per day), but detailed verification studies are needed before development. The natural quality of water in the report area is good. The water is generally low in dissolved solid and is soft to moderately hard. Surface water is less mineralized than ground water, especially during high flow when it is primarily surface runoff. A median dissolved-solids concentration of 117 mg/l (milligrams per liter) and a median hardness of 58 mg/l was determined for water samples collected at 20 sites on 16 streams during high flow. A median dissolved-solids concentration of 146 mg/l and a median hardness of 82 mg/l was determined for samples collected at the same sites during low flow. In contrast water from 130 wells had a median dissolved-solids concentration of 188 mg/l and a median hardness of 110 mg/l. Iron and manganese occur in objectionable concentrations in parts of the report area, particularly in water from streams draining swamps and in water from aquifers rich in iron- and manganese-bearing minerals. Concentrations of iron in excess of 0.3 mg/l were found in 40 percent of the high-streamflow samples, 59 percent of the low-streamflow samples and 20 percent of the ground-water samples. Human activities have modified the quality of water in much of the basin. Wide and erratic fluctuations in concentration of dissolved solids in streams, high bacterial content of the Quinnipiac River, and locally high nitrate and chloride concentrations in ground water are evidence of man's influence. Streams, wetlands, and some aquifers along the southern boundary of the basin contain salty water. Overpumping has caused extensive saltwater intrusion in aquifers in the southern and eastern parts of New Haven. The total amount of fresh water used in the area during 1970 is estimated at 35,710 million gallons, or 183 gallons per day per capita. Public water-supply systems met the domestic requirements of about 90 percent of the population; all the systems supplied water that met the drinking water standards of the Connecticut Department of Health.
The United States Geological Survey is currently investigating the ground-water resources of Connecticut in cooperation with the State Water Commission. As part of this cooperative project, in order to summarize the knowledge already gained about ground water in the State, a bibliography of reports dealing with ground water in Connecticut has been prepared. A compilation entitled "Bibliography and index of publications relating to ground water prepared by the Geological Survey and cooperating agencies", by G. A. Waring and O. E. Neinzer, was issued as U.S. Geological Survey Water-Supply Paper 992 in 1947. The following compilation lists all the papers in Water-Supply Paper 992 that refer to Connecticut plus other short reports not included in the letter. The first studies of ground water in Connecticut were begun in 1903 by Professor H. E. Gregory of Yale University under the auspices of the U.S. Geological Survey. The early studies were of the reconnaissance type, covering large sections of the State, and were concerned mainly with the relation of the bedrock geology to the water supply. The results were published in several Water-Supply Papers of the Geological Survey. In 1911 a cooperative agreement for the study of the ground-water resources of Connecticut in which each party shared equally in the expenses was made between the Federal Survey and the Connecticut State Geological and Natural History Survey. As a result more detailed studies in smaller areas were undertaken. Active field work covering more than half the State was continued through 1923 under this arrangement and the results published in eight U.S. Geological Survey Water-Supply Papers. After an eleven year period of inactivity and with the inauguration of the Federal Emergency Relief Commission, detailed studies of ground water in Connecticut were begun again in October 1934 as a project of the Emergency Relief Commission (later the Works Progress Administration). The project was sponsored by the Connecticut State Water Commission, the State Planning Board, and the U.S. Geological Survey. The technical direction of the work was undertaken by the Geological Survey. The project consisted of an inventory and mapping of wells and springs in the State by towns and the recording of weekly observations of water levels in selected wells. The data collected through October 1939 were published in six mimeographed bulletins and one typewritten bulletin by the Works Program Administration. In 1939, when it became necessary to curtail the work being carried on by the Works Progress Administration, cooperation was arranged between the Federal Ecological Survey and the State Water Commission to continue investigations relative to the over-development of ground-water supplies in the New Haven area. From time to time additional funds have been made available to meet growing demands by the State for data on its ground-water supplied and the present cooperative program between the U.S. Geological Survey and the State Water Commission is a continuation of the original arrangement. It is estimated that about 14 per cont of the State has been covered by recent ground-water surveys and in addition some data are available for another 20 per cent of he State.
The 557 square miles of the lower Housatonic River basin in western Connecticut include the basins of two major tributaries, the Pomperaug and Naugatuck Rivers. Nearly all water is derived from precipitation, which averaged 47 inches per year during 1931-60, In this period an additional 570 billion gallons of water per year entered the basin in the main stem of the Housatonic River at Lake Lillinonah, and some water was imported by water-supply systems from outside the basin. Almost half the precipitation--21.6 inches--was lost from the basin by evapotranspiration. Except for small amounts exported, the remainder discharged as runoff and underflow into Long Island Sound. Variations in streamflow at 6 long-term continuous-record gaging stations are summarized in standardized graphs and tables that can be used to estimate streamflow characteristics at other sites. For example, mean flow and two low-flow characteristics, the 7-day annual minimum flow for 2-year and 10-year recurrence intervals, have been determined for many partial-record stations throughout the basin. Of the 37 principal lakes, ponds, and reservoirs in the basin, 6 have usable storage of more than 1 billion gallons. The “maximum safe draft rate” (described in: “Storage of Water in Lakes and Reservoirs”) of the largest of these, Thomaston Reservoir near Thomaston, is 75.6 million gallons per day for the 10-year and 20-year recurrence intervals of annual lowest mean flow. Floods have occurred during every month, at one time or another. The two greatest floods on the Naugatuck River in historical time occurred 2 months apart in 1955. The larger, in August, had a peak of 106,000 cfs (cubic feet per second) at Beacon Falls. Since then, the likelihood of major floods has been considerably reduced by a program of flood control in the basin. Water can be obtained from three aquifers under-lying the basin-stratified drift, till, and bedrock. Stratified drift covers about 16 percent of the basin, mostly in valleys and lowlands, and its saturated part generally ranges in thickness from 10 feet in small valleys to 200 feet in the Housatonic River valley. Its transmissivity ranges from 0 to 47,000 ft 2 /day (feet shared per day). Till, deposited directly by glacial ice, forms a widespread but discontinuous mantle over bedrock in most upland areas and extends beneath stratified drift in lowlands; it ranges in thickness from 0 to 200 feet. The median value of 31 published determinations of hydraulic conductivity of till in southern New England is 0.67 ft/day and ranges from 0.013 to 29 ft/day. Crystalline bedrock underlies most of the basin and is composed principally of granite, gneiss, and schist. Sedimentary volcanic bedrock underlies only the Pomperaug River basin. Regardless of rock type, water is obtained mostly from fractures. Streambed deposits are significant features of the hydrogeologic system because they affect the amount of water from streams and lakes that can be induced to infiltrate aquifers. Based on field tests, characteristic values of vertical hydraulic conductivity of streambed deposits are 0.40 ft/day for fine-grained deposits and 14 ft/day for gravelly deposits. Ground-water supplies generally range in yield from several millions of gallons per day from large well fields to 1 gpm (gallons per minute) from single wells. Large supplies, with yields of 100 gpm or more from individual wells, are most commonly obtained from stratified drift. Yields to be expected from screened wells tapping this aquifer can be calculated by use of a series of graphs in conjunction with estimates of transmissivity and aquifer thickness. The yields of 14 principal ground-water reservoirs are estimated from aquifer characteristics and also from the amount of water that can be obtained from aquifer storage, from interception or runoff, and from infiltration of streamflow at low-flow conditions, using a hypothetical well-field arrangement for each reservoir. It is assumed that induced infiltration is restricted to an amount equal to the 7-day annual minimum stream-flow for a 2-year recurrence interval. Yields range from 1.4 to 15 mgd (million gallons per day) during periods of no recharge, and from 2.0 to 17 mgd during recharge periods. Small to moderate water supplies can be obtained from any of the aquifers under suitable conditions. For example, data from 294 wells in the basin indicate that yields of a few gallons per minute can be obtained from bedrock at most sites. The likelihood of obtaining an adequate domestic supply is slightly greater in granite than in schist and also is greater where the overburden is stratified drift rather than till. Chemical analyses of precipitation samples collected monthly from five stations in the basin during a 9-month period in 1966 show that rainfall is acidic and that sulfate is the dominant anion, probably because of industrial fumes and smoke within and near the basin. Where unaffected by man’s activities, water in the basin is generally low in dissolved-solids concentration, is of the calcium magnesium bicarbonate type, and is soft to moderately hard. In general, streamflow is less mineralized than ground water, particularly when it consists largely of direct runoff. However, streamflow becomes more highly mineralized during low-flow conditions, when most of it consists of more highly mineralized water discharged from aquifers. The median value of dissolved-solids concentration of water at 22 stream sites was 51 mg/1 (milligrams per liter) during high flow, and 68 mg/1 during low flow within the study period. Iron and manganese occur naturally in objectionable concentrations in parts of the basin, particularly in streams draining swamps and in water from bedrock containing iron and manganese-bearing minerals. Man’s activities have degraded the quality of water in streams in much of the basin, except in the Pomperaug subbasin. In the Naugatuck River basin, the degradation in quality is shown by wide and erratic changes in dissolved-solids concentration, excessive amounts of certain trace elements, a low dissolved oxygen content, and abnormally high temperatures. Ground water is degraded principally by induced infiltration of stream water containing chemical wastes, by wastes stored on the ground and by effluents from septic tanks. Below its confluence with the Naugatuck River, much of the Housatonic River and adjoining marshes, wetlands, and aquifers contain salt water. Measurements of specific conductance during low-flow conditions in 1969 indicate that the dissolved-solids concentration of water in the estuary ranged from 210 mg/1 near Twomile Island to 20,000 mg/1 near Long Island Sound. The quantity and quality of water in the basin are satisfactory for a wide variety of uses, and, with suitable treatment, the water may be used for most purposes. In 1967, the total amount of water used in the basin was about 194 billion gallons. About 90 percent of this was used for industrial purposes, and 95 percent of the industrial water was obtained from surface-water sources. In the same year, 17 municipal and private water-supply systems supplied water of satisfactory quality to about three-fourths of the population.
The upper Housatonic River basin report area has an abundant supply of water of generally good quality, which is derived from precipitation on the area and streams entering the area. Annual precipitation has averaged about 46 inches over a 30-year period. Of this, approximately 22 inches of water is returned to the atmosphere each year by evaporation and transpiration; the remainder flows overland to streams or percolates downward to the water table and ultimately flows out of the report area in the Housatonic River or in smaller streams tributary to the Hudson River. During the autumn and winter precipitation normally is sufficient to cause a substantial increase in the amount of water stored in surface reservoirs and in aquifers, whereas in the summer, losses through evaporation and transpiration result in sharply reduced streamflow and lowered ground-water levels. Mean monthly storage of water in November is 2.8 inches more than it is in June. The amount of water that flows into, through, and out of the report area represents the total amount potentially available for use ignoring reuse. For the 30-year period 1931 through 1960, the annual runoff from precipitation has averaged 24 inches (294 billion gallons). During the same period, inflows from Massachusetts and New York have averaged 220 and 64 billion gallons per year, respectively. A total average annual runoff of 578 billion gallons is therefore available. Although runoff indicates the total amount of water potentially available, it is rarely feasible to use all of it. On the other hand, with increased development, some water may be reused several times. The water availability may be tapped as it flows through the area or is temporarily stored in streams, lakes, and aquifers. The amounts that can be developed differ from place to place and time to time, depending on the amount of precipitation, on the size of drainage area, on the thickness, transmissivity, and areal extent of aquifers, and on the variations in chemical and physical quality of water. Differences in precipitation cause differences in the amount of streamflow whereas differences in the proportion of stratified drift affect its timing. Water can be obtained from wells almost anywhere in the area, but the amount obtainable at any particular point depends on the type and water-bearing properties of the aquifers tapped. Stratified-drift aquifers are the only ones generally capable of yielding more than 100 gpm (gallons per minute) to individual wells. Drilled, screened wells tapping this unit yield from 17 to 1,400 gpm, with a median yield of 200 gpm. Till and bedrock are widespread but generally provide only small supplies of water. Till is tapped in a few places by dug wells, which can yield small supplies of only a few hundred gallons per day throughout all or most of the year. Bedrock is the chief aquifer for privately owned domestic and rural supplies; it is tapped by drilled wells, about 90 percent of which will supply at least 2 gpm. Only 1 of 10 bedrock wells, however, will supply more than 30 gpm. The amount of ground water potentially available in the report area depends upon the thickness and hydraulic properties of aquifers, the amount of salvageable natural discharge of ground water, and the quantity of water available by induced infiltration from streams and lakes. From data on transmissivity, thickness, recharge, well performance, and streamflow, preliminary estimates of ground-water availability can be made for most stratified-drift aquifers in the report area. Long-term yields estimated for eight areas of stratified drift especially favorable for development of large ground-water supplies ranged from 0.6 to 5 mgd (million gallons per day). Detailed site studies are needed to verity these estimates and to determine optimum yields, drawdowns, and spacing of individual wells before major ground-water development is undertaken in these or other areas. The chemical quality of water in the report area is generally good; carbonate-bedrock units exert considerable local influence on water quality. Samples of naturally occurring surface water collected at 24 sites during low flow averaged 90 mg/l (milligrams per liter) dissolved solids and 60 mg/l hardness. Water from wells is generally more highly mineralized than naturally occurring water from streams. About 37 percent of the wells sampled yielded water with more than 200 mg/l dissolved solids and 50 percent yielded water with more than 120 mg/l hardness. These concentrations reflect the high degree of mineralization of ground water in carbonate bedrock and unconsolidated deposits derived from this bedrock. The larger streams, which transport varying amounts of industrial and domestic effluents, averaged about 150 mg/l dissolved solids and 90 mg/l hardness. Iron and manganese concentrations in both ground water and surface water at some places exceed recommended limits for domestic and industrial use. Most wells in the report area yield water with little or no iron or manganese. In certain localities however, the probability is high of encountering water with excessive concentrations of these constituents. Schists, especially the unit in the northwestern corner of the basin, are the likely sources of water with excessive iron and manganese. Iron concentrations in naturally occurring stream water exceed 0.3 mg/l under low-flow conditions at 29 percent of the sites sampled. These excessive concentrations result from discharge of iron-bearing water from aquifers or from swamps where iron is released from decaying vegetation. Water temperature in the larger streams ranges from 0°C (degrees Celsius) to about 28°C. Ground water between 30 feet and 200 feet below the land surface has a relatively constant temperature, usually between 8°C and 11°C. The quantity of suspended sediment transported by streams under natural conditions is negligible. Even in streams affected by man, turbidity is rarely a problem. The total amount of water used in the report area for all purposes during 1967 was about 6,360 million gallons, or 140 gpd per person. Public supplies furnished the domestic needs of nearly half the population of the area. All of the 14 public supplies sampled provided water that meets the drinking water standards of the U.S. Public Health Service.
The description, location, log and meter tests of all the drilled wells on Oahu are given herein as of March 1 1938. Except for the discharges of plantation wells, which are published on pages 275 to 322 of Bulletin 1, head, chloride, and discharge records are listed only to the close of 1934, the date when this report was compiled. All head measurements and salt determinations made by the U.S. Geological Survey since 1934 will be found in the annual U.S. Geological Survey Water-Supply Papers entitled “Water levels and artesian pressure in observation wells in the United States.” Records of wells in the district of Honolulu are currently printed in the biennial reports of the Board of Water Supply, Honolulu. Most of the records of the plantation wells have been furnished by the owners. Plate 2 shows the location of the wells, whether they are sealed, and whether the log is known. The static level or head of a well is the height above mean sea level to which the water will rise when all flow from the well is shut off. In the nonartesian wells the static level is the level of the water table of the basal zone of saturation in the basalts of the Koolau and Waianae volcanic series. Many of the wells are subartesian; that is, the water stands in the well above the level at which it was first encountered but does not overflow.
Across the Central Valley of California, millions of wintering waterfowl rely on moist soil seed (MSS) plants that grow in managed seasonal wetlands as a critical source of food. Estimates of MSS plant production are used to set waterfowl habitat targets yet this information is not well known. We created the first Central Valley-wide time series maps of MSS plant distributions and productivity. We found that MSS plant seed yield declined in critical drought years, which corresponded with reduced water delivery to managed wetlands. Our results provide improved food resource estimates and information to help managers prioritize actions as water supply becomes more uncertain with climate change.
The area investigated comprises 33 square miles in the Price River drainage basin ad is in the High Plateaus section of Utah. Precipitation on most of the area ranges from about 20 to 23 inches per year, and the average annual precipitation for the entire area was assumed to be 22 inches, of which approximately 65 percent is lost by evapotranspiration. The geologic formations underlying the area are the Blackhawk and Price River Formations of Cretaceous age, the North Horn Formation of Cretaceous and Tertiary age, the Flagstaff Limestone and Colton Formation of tertiary age, and unconsolidated deposits of probable Quaternary age. Some ground water issues from springs and seeps and is used by stock and the cities of Price and Helper. The annual discharge from the springs and seeps in the area averages about 3,000 acre-feet. Two deep wells supply about 400 acre-feet per year for use at a steam-generating plant. The aquifers penetrated by the wells are in the Flagstaff Limestone and the North Horn formation, the deepest aquifer being about 1,500 feet below the land surface. Most of the ground water in the area is suitable for municipal and industrial use. The surface discharge from the area is approximately 6,000 acre-feet per year. By means of a water budget, it is calculated that approximately 4,000 acre-feet per year leaves the area by subsurface flow. Further development of ground water on a large scale can be accomplished only by the use of wells. It is possible, however, that part of any newly developed supply from wells may be drawn from existing spring discharge or streamflow.
The biblical Jordan River Valley , which extends from Lake Tiberias (the Sea of Galilee) to the Dead Sea, is decidedly similar to the Jordan River Valley of Utah , which joins Lake Utah and Great Salt Lake. Both Jordan Rivers drain relatively large fresh-water lakes and also are major sources of discharge into large salty lakes that have no outlets to the ocean.The two Jordan River valleys and the highlands and mountains that surround them, have many physiographic, geologic, and hydrologic similarities as well as some noteworthy differences. For example, an hypothesis for the formation of the Dead Sea- Jordan Valley rift is that the east Jordan block slid northward with respect to the west Jordan block. The amount of displacement is estimated to be about 65 miles and took place partly in Miocene and possible Pliocène and partly in Pleistocene time. Tectonc activity has also been a major factor in the formation of the Jordan valley of Utah , but the movement here probably was along large normal faults in late Tertiary and Quaternary time. The sediments underlying both Jordan River valleys were deposited in ancestral lacustrine and fluvial environments. Abundant supplies of ground water are found under both valleys , but probably larger supplies of better quality water can be obtained in Utah . Both valleys contain numerous small nonthermal and a few large thermal springs.