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At least 1,801 records · Page 100Linked to original sources
USGS1973

Floods of 1971 and 1972 on Glover Creek and Little River in southeastern Oklahoma

Heavy rains of December 9-10, 1971, and Oct. 30-31, 1972, caused outstanding floods on Glover Creek and Little River in McCurtain County in southeastern Oklahoma. This report presents hydrologic data that document the extent of flooding, flood profiles, and frequency of flooding on reaches of both streams. The data presented provide a technical basis for formulating effective flood-plain zoning that will minimize existing and future flood problems. The report also can be useful for locating waste-disposal and water-treatment facilities, and for the development of recreational areas. The area studied includes the reach of Little River on the Garvin and Idabel 7 1/2-minute quadrangles (sheet 1) and the reach of Glover Creek on the southwest quarter of the Golden 15-minute quadrangle (sheet 2). The flood boundaries delineated on the maps are the limits of flooding during the December 1971 and October 1972 floods. Any attempt to delineate the flood boundaries on streams in the study area other than Glover Creek and Little River was considered to be beyond the scope of this report. The general procedure used in defining the flood boundaries was to construct the flood profiles from high-water marks obtained by field surveys and by records at three stream-gaging stations (two on Little River and one on Glover Creek.). The extent of flooding was delineated on the topographic maps by using the flood profiles to define the flood elevations at various points along the channel and locating the elevations on the map by interpolating between contours (lines of equal ground elevation). In addition, flood boundaries were defined in places by field survey, aerial photographs, and information from local residents. The accuracy of the flood boundaries is consistent with the scale and contour interval of the maps (1 inch = 2,000 feet; contour interval 10 and 20 feet), which means the flood boundaries are drawn as accurately as possible on maps having 10- and 20-foot contour intervals.

Oklahoma↗
USGS1974

Estimated permeabilities for soils in the Sacramento Valley, California

Analysis of engineering and hydrologic data from 15 previous soil studies, analysis of particle-size distribution, and analysis of descriptions of soil profiles show that 50 percent of the Sacramento Valley area has soils having permeabilities characterized by infiltration rates of less than 2 feet per day (0.6 meter per day). Consolidated barriers that could impede vertical flow were found in 30 percent of the area.

California↗
USGS1974

Flood characteristics of Oklahoma streams techniques for calculating magnitude and frequency of floods in Oklahoma, with compilations of flood data through 1971

The 2-, 5-, 10-, 25-, 50-, and 100-year recurrence interval floods are related to basin and climatic parameters for natural streams in Oklahoma by multiple regression techniques through the mathematical model, Q x =aA b S c P d , where Q x is peak discharge for recurrence interval x, A is contributing drainage area, S is main channel slope, P is mean annual precipitation, and a, b, c, and d are regression constants and coefficients. One equation for each recurrence interval applies statewide for all natural streams of less than 2,500 mil (6,500 km 2 ), except where manmade works, such as dams, flood-detention structures, levees, channelization, and urban development, appreciably affect flood runoff. The equations can be used to estimate flood frequency of a stream at an ungaged site if drainage area size, main channel slope, and mean annual precipitation are known. At or near gaged sites, a weighted average of the regression results and the gaging station data is recommended. Individual relations of flood magnitude to contributing drainage area are given for all or parts of the main stems of the Arkansas, Salt Fork Arkansas, Cimarron, North Canadian, Canadian, Washita, North Fork Red, and Red Rivers. Parts of some of these streams, and all of the Neosho and Verdigris Rivers are not included because the effects of. major regulation from large reservoirs cannot be evaluated within the scope of the report. Graphical relations of maximum floods of record for eastern and western Oklahoma provide a guide to maximum probable floods. A random sampling of the seasonal occurrence of floods indicated about two-thirds of all annual floods in Oklahoma occur during. April through July. Less than one-half of one percent of annual floods occur in December. A compilation of flood records at all gaging sites in Oklahoma and some selected sites in adjacent States is given in an appendix. Basin and climatic parameters and log-Pearson Type III frequency data and statistics are given for most station records. A second appendix gives a reprint of the U.S. Water Resources Council Bulletin 15 which describes procedures for fitting a log-Pearson Type III distribution to gaging station data.

Oklahoma↗
USGS1974

Ground water in the alluvium along the Green River between its mouth and Woodbury, Kentucky

The are of investigation is that part of the Green River flood plain which is in the Western Coal Field region of Ken tucky. It extends from the mouth at the Ohio River to river-mile 149 (river-kilometer 240) at Woodbury, Ky. The flood plain varies in width from 0.4 mile (0.6 kilometer) to over 6 miles ( 9 kilo meters). Total surface area is about 345 square miles (89,400 hectares). Navigational pools are maintained on this part of the Green River by a series of locks and dams.

Kentucky↗
USGS1973

Stratigraphy of an archeological site, Ocmulgee flood plain, Macon, Georgia

Archeological excavations on the Ocmulgee River flood plain at Ocmulgee National Monument revealed eight sedimentary units of Holocene age. Types of deposits found are natural levee, oberbank deposit, and a probable point bar. Since the 18th century, locally more than 10 feet of sediment has been deposited. These modern sediments are similar to those on other flood plains in the southeastern United States and probably resulted from erosion that began when extensive areas were laid bare for farming. They are red to reddish brown in contrast to underlying sediment, which is various shades of gray, brown, and yellow. Earliest traces of man are "spinner-type" projectiles in the lower sand member (Qls). Marrow mountain-type points are found in mottled silty sandy clay (Qmssc). Triangular stemmed Savannah River points were found throughout the intermediate sand (Qis). Fiber tempered pottery shards and steatite bowls were found in upper one half of the intermediate sand member (Qis).

Georgia↗
USGS1974

Mathematical model of San Juan Valley ground-water basin, San Benito County, California

A mathematical model study of the San Juan Valley ground-water basin in San Benito County, Calif., has quantitatively described the ground-water hydrology of the basin under past, present, and future conditions of development. An analysis of conditions in the basin prior to large-scale ground-water development indicates that net recharge equaled 9.23 cubic feet per second and occurred as subsurface flow to the eastern part of the basin and infiltration of rain, direct runoff, and minor streamflows. Net predevelopment discharge equaled 9.23 cubic feet per second and occurred as aquifer discharge to the San Benito River. The 9.23 cubic feet per second of predevelopment recharge is considered to be perennial recharge to the basin. Large-scale ground-water development occurred in the area during the period 1945-68 and caused water levels to decline throughout most of the basin. Progressive depletion of aquifer storage during this period changed the San Benito River from a gaining (perennial) stream to a losing stream along most of its reach in the basin area. Net discharge from the basin during the period 1945-68 averaged 18.10 cubic feet per second. Of this amount 17.82 cubic feet per second occurred as pumpage from wells, and 0.28 cubic foot per second occurred as basin discharge to the San Benito River. Net recharge to the basin during the same period averaged 13.57 cubic feet per second. Of this amount 4.34 cubic feet per second occurred as infiltration from the San Benito River and 9.23 cubic feet per second occurred as perennial recharge. Use of the calibrated mathematical model to simulate quantities of imported water entering the basin from the San Benito River indicates that water levels in San Juan Valley will stabilize or recover when additional recharge equals or exceeds 3,000 acre-feet per year.

California↗
USGS1974

Estimating low-flow frequency for perennial Missouri Ozarks streams

A linear regression model, utilizing an independent variable described as the flow area of a stream, has been developed for use in estimating minimum streamflow at ungaged sites in the Ozarks region of Missouri. The basic premise in the method is that low-flow characteristics at any point on perennial Ozarks streams are significantly related to the average width and depth or flow area of the minimum flows. The standard errors of regression equations defining the 7-day Q2, 7-day Q10, and 7-day Q20 are 41, 60, and 76 percent, respectively. In comparison, standard errors of 170 to 390 percent were obtained during previous regionalization studies.

Missouri↗
USGS1973

Geology and quality of water in the Modesto-Merced area, San Joaquin Valley, California, with a brief section on hydrology

The Modesto-Merced area includes about 1,800 square miles on the northeast side of the San Joaquin Valley. The physiographic units in the area are (1) Sierra Nevada, (2) dissected uplands, (3) low alluvial plains and fans, (4) river flood plains and channels, and (5) overflow lands. Geologic units consist of consolidated rocks and unconsolidated deposits. The dominant structure of the geologic units is that of a homocline, which reflects the southwestward-tilted fault block of the Sierra Nevada. The consolidated rocks include: (1) basement complex (pre-Tertiary), (2) marine sandstone and shale (Cretaceous), (3) Ione Formation and other sedimentary rocks (Eocene), (4) Valley Springs Formation (late? Miocene), and (5) the Mehrten Formation (Miocene and Pliocene). In the eastern part of the area, the consolidated rocks generally yield small quantities of water to wells except for the Mehrten Formation which is an important aquifer. The unconsolidated deposits include: (1) continental deposits (Pliocene and Pleistocene?), (2) lacustrine and marsh deposits (Pleistocene), (3) older alluvium (Pleistocene and Holocene?), (4) younger alluvium (Holocene), and (5) flood-basin deposits (Holocene). The continental deposits and older alluvium are the main water-yielding units in the unconsolidated deposits. The lacustrine and marsh deposits (E-clay) and the flood-basin deposits yield little water to wells, and the younger alluvium in most places probably yields only moderate quantities of water to wells. There are three ground-water bodies in the Modesto-Merced area: (1) the unconfined water body, (2) the confined water body, and (3) the water body in consolidated rocks. The unconfined water body occurs in the unconsolidated deposits above and east of the E-clay, except in the western and southern parts of the area where clay lenses occur and semiconfined conditions exist. The confined water body occurs in the unconsolidated deposits below the E-clay and extends downward to the base of fresh water. The water body in consolidated rocks occurs under both perched and confined conditions. Ground-water movement in the unconfined and the confined water bodies is generally westward toward the valley trough. In the unconfined water body, the water also moves toward the major rivers, and toward pumping depressions at Modesto and near El Nido. Because of the higher head in the unconfined water body, water slowly moves from it through the E-clay to the underlying confined water body. Surface water is used extensively for irrigation in most of the study area; consequently, shallow water in the unconfined water body has to be controlled by pumping. Nevertheless, water levels near Modesto declined about 6 feet between 1958 and 1962, for the most part during the dry years 1959-61. Near El Nido, water levels declined about 70 feet between 1942 and 1967. In the confined water body, water levels were high in the winter and spring and low in the summer and fall, reflecting irrigation practices. In the southwestern part of the area, water levels in the confined water body declined about 14 feet from 1962 to 1968 and rose slightly after 1968, whereas in the northwestern part water levels remained fairly constant. Water from the upper reaches of the Stanislaus, Tuolumne, Merced, and Chowchilla Rivers is calcium bicarbonate in chemical type and is of excellent quality. As those rivers cross the valley floor, their water quality is generally degraded by return flows from irrigated land, and in the Tuolumne River by saline water discharged from abandoned gas wells. Average dissolvedsolids content in the major rivers, as indicated by chemical analyses, do not exceed 400 mg/1 (milligrams per liter) except in the San Joaquin River where average dissolved-solids content has not exceeded 1,050 mg/l. Water from minor streams in the area is bicarbonate in chemical type with dissolved-solids content ranging from 56 mg/1 to about 350 mg/l. Although chloride-type fresh ground water occurs in the unconfined and confined water bodies and in the water body in consolidated rocks, most of the fresh ground water is a bicarbonate type that has a dissolved-solids content of less than 500 mg/l. Water having dissolved solids in excess of about 2,000 mg/1 is considered to be saline. Saline water extends below the base of fresh water to the basement complex and, except in the extreme eastern part, underlies most of the study area. Saline water also occurs as lenses above the base of fresh water in the unconfined and confined water bodies.

California↗
USGS1974

Effects of urbanization on floods in the Dallas, Texas metropolitan area

The effects of urbanization on flood characteristics of streams in the Dallas metropolitan area were studied by use of a digital model of the hydrologic system. The model was calibrated by using observed rainfall and runoff data from 19 storms in six basins having various degrees of urbanization. The calibrated models were used with a 57- year rainfall record to simulate 57-year records of annual peak discharges in 14 basins. The flood-frequency characteristics were defined by fitting the simulated 57-year records to log-Pearson Type III distributions. Regional peak-discharge equations, which can be used to determine the maximum rates of discharge that could be expected to be equaled or exceeded on the average of once in 1.25, 2, 5, 10, 25, and 100 years, were derived from multiple-regression analyses. The relationships among flood frequency, drainage area, and a coefficient of impervious area are given in a nomograph. The analyses indicate that in a fully-developed residential area, the flood peaks will be 1.2 to 1.4 times those from an undeveloped area; and the annual direct runoff will be about double that from an undeveloped area. Data were not sufficient to determine the increase in runoff from a highly industrialized area where the effective imperviousness approaches 100 percent.

Water-Resources Investigations Report↗
USGS1974

Water quality in Rhode River at Smithsonian Institution Pier near Annapolis, Maryland, April 1970 through December 1973

Water temperature, salinity (computed from specific conductance data), turbidity, dissolved oxygen, pH, and water level data were collected by a continuously recording water quality monitor located in the Rhode River, at the Smithsonian Institution's pier near Annapolis, Md., from April 1970 through December 1973. Data, as presented in this report, consist of daily maximum and minimum values summarized by week to give weekly averages and extremes. Temperatures showed an overall range from 0.7 to 32.6°C. The water temperature data indicate successively warmer winters. Salinity ranged from 1.05 to 14.03 parts per thousand. In June 1972, salinity dropped markedly as fresh water from tropical storm Agnes entered the Rhode River from Chesapeake Bay. Most of the fresh water entering upper Chesapeake Bay as a result of tropical storm Agnes came from the Susquehanna River. Turbidity was usually low, averaging about 14 Jackson Turbidity Units; however, during spring and early summer of 1972, values averaged about 23 Jackson Turbidity Units. This increase in turbidity was due to the high Susquehanna River flows during that period. Extremes of turbidity ranged from about 5 to 80 Jackson Turbidity Units. Dissolved oxygen ranged from 0.0 to 19.8 milligrams per litre. Large daily changes in oxygen indicated a high state of biological metabolism. Values of pH ranged from 6.8 to 10.1 and daily changes coincided with oxygen changes. Tide-dominated water levels had an overall range of 5.9 feet (1.8 metres) and a mean tidal range of 1.5 feet (0.46 metres).

Maryland↗

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