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• 1. [Image] Preliminary report on the ground-water resources of the Klamath River Basin, Oregon

  	The Klamath River basin, including the adjacent Lost River basin, includes about ?,5>OO square miles of plateaus, mountain-slopes and valley plains in south-central Oregon* The valley plains range in altitude ...
  	Citation × Citation Citation Abstract Copy Title: Preliminary report on the ground-water resources of the Klamath River Basin, Oregon Author: Newcomb, Reuben Clair Year: 1958, 2005 The Klamath River basin, including the adjacent Lost River basin, includes about ?,5>OO square miles of plateaus, mountain-slopes and valley plains in south-central Oregon* The valley plains range in altitude from about U,100 feet in the south to more than li,500 feet at the northern end; the mountain and plateau lands rise to an average altitude of 6,000 feet at the drainage divide, some peaks rising above 9*000 feet. The western quarter of the ba3in is on the eastern slope of the Cascade Range and the remainder consists of plateaus, mountains, and valleys of the basin-and-range type* The rocks of the Klamath River basin range in age from Recent to Mesozoic* At the southwest side of the basin in Oregon, pre~Tertiary metamorphic, igneous, and sedimentary rocks, which form extensive areas farther west, are overlain by sedimentary rocks of Eocene age and volcanic rocks of Eocene and Oligocene age* These early Tertiary rocks dip east toward the central part of the Klamath River basin. The complex "volcanic rocks of high Cascades" include three units: The lowest unit consists of a sequence of basaltic lava flows about 800 feet thick5 the medial unit is composed of volcanic-sedimentary and sedimentary rocks?the Tonna formation-200 to 2,000 feet thick; the uppermost unit is a sequence of basaltic lava flows commonly about 200 feet thick. These rocks dip east from the Cascade Unpublished records subject to revision 2 Range and are the main bedrock formations beneath most of the basin. Extensive pumice deposits, which emanated ^?^ ancestral Mount Mazaraa, cover large areas in the northwestern part of the basin* The basin has an overall synclinal structure open to the south at the California boundary where it continues as the Klamath Lake basin in California* The older rocks dip into the basin in monoclinal fashion from the adjoining drainage basins* The rocks are broken along rudely rectangular nets of closely spaced normal faults* the most prominent set of which trends northwest* The network of fault displacements includes two main grabens, the Klamath and the Langell, which were downthrown approximately ?00 and 1,000 fast, respectively* The average annual precipitation varies with the altitude, the higher parts of the Cascade Range getting more than 60 inches, and the semierid valley plains receive as little as 13 inches in some places* Most precipitation occurs in the winter. \ The principal tributaries, Williamson and Sprague Rivers, rise near the higher parts of the eastern rim of the basin, flow through narrow valley plains to the western part, and discharge into Upper Klamath Lake* Wood River and associated creeks also empty into Upper Klamath Lake after draining southward along the eastern foot of the Cascade Range* The Klamath River receives the outflow from Upper Klamath Lake, via Lifak River and Lake Ewauna, and flows southwestward through Keno Gap and hence through a youthful canyon, to its lower valley in California* The ground water occurs largely in an unconfined, or water-table, condition, though areas of local confinement are present* The regional Unpublished records subject to revis&oa is graded to water table / a base level about equal to that of the major drainage* where water is confined, on the valley plains. The slope of the water tafele, ~ of/the piezomstric surface is downstream at about the same grade as that "of the surface drainage in each of the larger valleys, attd groufid*water divides occur between the upper parts of adjacent major valleys* The principal water-bearipg units are.the'lower lava rocks and upper lava rocks of the "volcanic rocks of high Cascades,* the pumice of Quaternaryage, and the allusriTuju In places layers of coarse flagmental material in the Tonna formation (Newcorub, 1958) also transmit water* The water-bearing units, especially the breccia layers of the lava rocks and the pumice, yield large amounts of water to wells and provide natural discharge outlets for the ground water. The spring outflows to the Williamson and Wood Rivers-Crooked Creek drainage, measured in September and October 1955, were at a rate equivalent to about 700,000 acre-feet per year. The spring outflows into the Sprague River were at a rate equal to 2l;5>000 apre-feet per year* Large springs occur along the edges of Upper Klamath Lake but their discharges could not be measured, and the known spring discharge from the lower lava rocks in the river canyon below Keno was not measured. The spring discharge into Lost River in the reach ?rom Bonanza to Harpold Bridge was at a rate equivalent to 75,000 acre-feet per year. Much of the water discharged from springs is used for irrigation during the growing season, but ground water has not been extensively Unpublished records subject to revision developed by means of wells except in the'Yonna Valley and other local areas. The total withdrawal of ground water from wells in 1951? was only about 30,000 acre-feet, of which 27,000 was used for irrigation* The ground water is of excellent quality in general, but sodium sulfate water occurs in the belts of warm rock along some faults and alkali bicarbonate water is present in the main evapotranspiration basins. Unpublished records subject to revision Title: Preliminary report on the ground-water resources of the Klamath River Basin, Oregon Author: Newcomb, Reuben Clair Year: 1958, 2005 The Klamath River basin, including the adjacent Lost River basin, includes about ?,5>OO square miles of plateaus, mountain-slopes and valley plains in south-central Oregon* The valley plains range in altitude from about U,100 feet in the south to more than li,500 feet at the northern end; the mountain and plateau lands rise to an average altitude of 6,000 feet at the drainage divide, some peaks rising above 9*000 feet. The western quarter of the ba3in is on the eastern slope of the Cascade Range and the remainder consists of plateaus, mountains, and valleys of the basin-and-range type* The rocks of the Klamath River basin range in age from Recent to Mesozoic* At the southwest side of the basin in Oregon, pre~Tertiary metamorphic, igneous, and sedimentary rocks, which form extensive areas farther west, are overlain by sedimentary rocks of Eocene age and volcanic rocks of Eocene and Oligocene age* These early Tertiary rocks dip east toward the central part of the Klamath River basin. The complex "volcanic rocks of high Cascades" include three units: The lowest unit consists of a sequence of basaltic lava flows about 800 feet thick5 the medial unit is composed of volcanic-sedimentary and sedimentary rocks?the Tonna formation-200 to 2,000 feet thick; the uppermost unit is a sequence of basaltic lava flows commonly about 200 feet thick. These rocks dip east from the Cascade Unpublished records subject to revision 2 Range and are the main bedrock formations beneath most of the basin. Extensive pumice deposits, which emanated ^?^ ancestral Mount Mazaraa, cover large areas in the northwestern part of the basin* The basin has an overall synclinal structure open to the south at the California boundary where it continues as the Klamath Lake basin in California* The older rocks dip into the basin in monoclinal fashion from the adjoining drainage basins* The rocks are broken along rudely rectangular nets of closely spaced normal faults* the most prominent set of which trends northwest* The network of fault displacements includes two main grabens, the Klamath and the Langell, which were downthrown approximately ?00 and 1,000 fast, respectively* The average annual precipitation varies with the altitude, the higher parts of the Cascade Range getting more than 60 inches, and the semierid valley plains receive as little as 13 inches in some places* Most precipitation occurs in the winter. \ The principal tributaries, Williamson and Sprague Rivers, rise near the higher parts of the eastern rim of the basin, flow through narrow valley plains to the western part, and discharge into Upper Klamath Lake* Wood River and associated creeks also empty into Upper Klamath Lake after draining southward along the eastern foot of the Cascade Range* The Klamath River receives the outflow from Upper Klamath Lake, via Lifak River and Lake Ewauna, and flows southwestward through Keno Gap and hence through a youthful canyon, to its lower valley in California* The ground water occurs largely in an unconfined, or water-table, condition, though areas of local confinement are present* The regional Unpublished records subject to revis&oa is graded to water table / a base level about equal to that of the major drainage* where water is confined, on the valley plains. The slope of the water tafele, ~ of/the piezomstric surface is downstream at about the same grade as that "of the surface drainage in each of the larger valleys, attd groufid*water divides occur between the upper parts of adjacent major valleys* The principal water-bearipg units are.the'lower lava rocks and upper lava rocks of the "volcanic rocks of high Cascades,* the pumice of Quaternaryage, and the allusriTuju In places layers of coarse flagmental material in the Tonna formation (Newcorub, 1958) also transmit water* The water-bearing units, especially the breccia layers of the lava rocks and the pumice, yield large amounts of water to wells and provide natural discharge outlets for the ground water. The spring outflows to the Williamson and Wood Rivers-Crooked Creek drainage, measured in September and October 1955, were at a rate equivalent to about 700,000 acre-feet per year. The spring outflows into the Sprague River were at a rate equal to 2l;5>000 apre-feet per year* Large springs occur along the edges of Upper Klamath Lake but their discharges could not be measured, and the known spring discharge from the lower lava rocks in the river canyon below Keno was not measured. The spring discharge into Lost River in the reach ?rom Bonanza to Harpold Bridge was at a rate equivalent to 75,000 acre-feet per year. Much of the water discharged from springs is used for irrigation during the growing season, but ground water has not been extensively Unpublished records subject to revision developed by means of wells except in the'Yonna Valley and other local areas. The total withdrawal of ground water from wells in 1951? was only about 30,000 acre-feet, of which 27,000 was used for irrigation* The ground water is of excellent quality in general, but sodium sulfate water occurs in the belts of warm rock along some faults and alkali bicarbonate water is present in the main evapotranspiration basins. Unpublished records subject to revision Close

• 2. [Image] Groundwater investigation of Bonanza Springs, Yonna, Poe and Langel valleys

  	PURPOSE, SCOPE AND METHODOLOGY A reconnaissance study was designed to collect, compile, and analyze data to determine if ground-water use would interfere with surface water sources near Big Bonanza Springs. ...
  	Citation × Citation Citation Abstract Copy Title: Groundwater investigation of Bonanza Springs, Yonna, Poe and Langel valleys Author: Gorman, Kyle G. Year: 1994, 2004 PURPOSE, SCOPE AND METHODOLOGY A reconnaissance study was designed to collect, compile, and analyze data to determine if ground-water use would interfere with surface water sources near Big Bonanza Springs. The study was to last one year from July 1992 to June 1993. Periodic water level measurements and stream flow measurements have been made since June 1993, to create a more complete data set. Water level measurements in selected wells were made periodically to determine groundwater level fluctuations over time. A continuous water level recorder was installed in one well in September 1992 and is currently scheduled to run until spring 1994, when its status will be evaluated. The emphasis on work in the local area around Bonanza included monthly water level measurements, Lost River stream flow measurements, and Bonanza Springs weir measurements. This area has the highest concentration of wells, both domestic and irrigation, and is of particular interest because of the large aggregate discharge of groundwater in a short reach of the Lost River. To quantify the discharge of the Bonanza Springs, wading stream flow measurements were made above and below the section of the Lost River where groundwater is known to discharge. The difference between the two measurements was assumed to give the discharge of the springs in that reach. To correlate the overall flow of Bonanza Springs to the direct measurement of some of the discharge points, various-sized rectangular weirs were placed in the northern channel of the springs in the Big Bonanza Springs Park. The comparison could then be made by making sets of measurements at all locations in a single day. The total potential use was determined by summing the number of cubic feet per second (cfs) on the pending applications filed with OWRD for the appropriation of groundwater in the area within the study boundaries. This area coincides with the valley lowland areas. The total maximum rate of appropriation under terms of existing permits was determined by valley only in Langell Valley for the 1992 irrigation season. This was done by summing the individual rates in permits for irrigation, stock and domestic purposes, if any. This total included all issued permits and emergency drought permits exclusively from groundwater. Sample drill cuttings were collected from wells under construction during the study period within the study boundaries. The samples were examined in an effort to correlate geology defined in past studies with present knowledge. They were also used to conceptualize the subsurface geology. A video log of the well bore in which the continuous water level recorder was installed was done in early October 1992. Since this well was constructed prior to the requirement of a well drilling report, a video log of the rock types throughout the well bore was recorded. This information was important in evaluating static water level information also collected by the recorder. Title: Groundwater investigation of Bonanza Springs, Yonna, Poe and Langel valleys Author: Gorman, Kyle G. Year: 1994, 2004 PURPOSE, SCOPE AND METHODOLOGY A reconnaissance study was designed to collect, compile, and analyze data to determine if ground-water use would interfere with surface water sources near Big Bonanza Springs. The study was to last one year from July 1992 to June 1993. Periodic water level measurements and stream flow measurements have been made since June 1993, to create a more complete data set. Water level measurements in selected wells were made periodically to determine groundwater level fluctuations over time. A continuous water level recorder was installed in one well in September 1992 and is currently scheduled to run until spring 1994, when its status will be evaluated. The emphasis on work in the local area around Bonanza included monthly water level measurements, Lost River stream flow measurements, and Bonanza Springs weir measurements. This area has the highest concentration of wells, both domestic and irrigation, and is of particular interest because of the large aggregate discharge of groundwater in a short reach of the Lost River. To quantify the discharge of the Bonanza Springs, wading stream flow measurements were made above and below the section of the Lost River where groundwater is known to discharge. The difference between the two measurements was assumed to give the discharge of the springs in that reach. To correlate the overall flow of Bonanza Springs to the direct measurement of some of the discharge points, various-sized rectangular weirs were placed in the northern channel of the springs in the Big Bonanza Springs Park. The comparison could then be made by making sets of measurements at all locations in a single day. The total potential use was determined by summing the number of cubic feet per second (cfs) on the pending applications filed with OWRD for the appropriation of groundwater in the area within the study boundaries. This area coincides with the valley lowland areas. The total maximum rate of appropriation under terms of existing permits was determined by valley only in Langell Valley for the 1992 irrigation season. This was done by summing the individual rates in permits for irrigation, stock and domestic purposes, if any. This total included all issued permits and emergency drought permits exclusively from groundwater. Sample drill cuttings were collected from wells under construction during the study period within the study boundaries. The samples were examined in an effort to correlate geology defined in past studies with present knowledge. They were also used to conceptualize the subsurface geology. A video log of the well bore in which the continuous water level recorder was installed was done in early October 1992. Since this well was constructed prior to the requirement of a well drilling report, a video log of the rock types throughout the well bore was recorded. This information was important in evaluating static water level information also collected by the recorder. Close