U.S. GEOLOGICAL SURVEY Water Resources Investigations 76-26 Prepared in cooperation with the Uivvei pt ffiiupist at Urbana-Ch3|ipai?ff M s •'j**** f'S-'vVr'.SJR'WtS^SBsa ffiS rw£$ pSP *?&&*?$■ * ' •'>- i,?v UNIVERSITY 0 R ILLINOIS LIBRARY at urbana-champak WATER RESOURCES OF THE WARM SPRINGS INDIAN RESERVATION, OREGON By J. H. Robison and Antonius Laenen U.S. GEOLOGICAL SURVEY Water Resources Investigations 76-26 Prepared in cooperation with the CONFEDERATED TRIBES OF THE WARM SPRINGS RESERVATION 1976 UNITED STATES DEPARTMENT OF THE INTERIOR Thomas S. Kleppe, Secretary GEOLOGICAL SURVEY Vincent E. McKelvey, Director For additional information write to: U.S. Geological Survey P.O. Box 3202 Portland, Oregon 97208 ii CONTENTS Page Abstract- 1 Introduction- 2 Geography- 2 Geology- A Clarno Formation- A John Day Formation- A Columbia River Basalt Group- 5 Dalles Formation--- 5 Basalt- 6 Andesite- 6 Gravel- 6 Alluvium- 6 Hydrology- 7 Climate- 7 Streams and streamflow- 7 Warm Springs River- 17 Shitike Creek- 19 Whitewater River- 20 Jefferson Creek- 22 Metolius River- 22 Deschutes River- 22 Other streams- 23 Streamflow distribution- 23 Quality of streamflow-26 Lakes and reservoirs- 26 Ground water- 33 Occurrence and movement- 33 Springs- 3A Hot springs-36 Wells- 36 Quality of ground water-A1 Standards for the usability of water-A2 Domestic use-A2 Use by livestock or fish-AA Irrigation use-AA Conclusions- A5 Glossary of selected terms-A6 Selected references-A8 Basic-data records-51 iii ILLUSTRATIONS [Plate is in pocket] Plate 1. Geohydrologic map of the Warm Springs Indian Reservation, Oreg. Page Figure 1. Map showing location of Warm Springs Indian Reservation- 3 2. Map showing average annual precipitation- 8 3. Graph showing monthly precipitation at Government Camp, Oreg., 1973-74 water years- 10 4. Map showing drainage basins and selected streamflow stations-- 11 5. Graph showing monthly mean runoff of Warm Springs River, Shitike Creek, and White River, 1973-74 water years- 12 6. Graph showing mean monthly runoff of White River below Tygh Valley, 1917-74- 13 7. Graph showing relation of annual mean discharges in 1973 to mean annual discharges for selected streams-14 8. Graph showing relation of low flow of the Whitewater River to concurrent flow of Squaw Creek- 15 9. Regional flood-frequency curve for White River below Tygh Valley, 1918-74------16 10. Map showing percentage of flow at several points on the Warm Springs River and its tributaries compared to flow at the mouth- 17 11. Graph showing streamflow of Shitike Creek, 1973-74, compared to suggested optimum and minimum flows for fish life-21 12-21. Diagrams showing hydrography, temperature, and dissolved oxygen for selected high lakes. 12. Harvey Lake- 27 13. Spoon Lake- 27 14. Long Lake- 28 15. Dark Lake- 28 16. Island Lake- 29 17. Trout Lake- 29 18. Boulder Lake-30 19. Blue Lake- 30 20. Gibson Lake- 31 21. Breitenbush Lake- 31 22. Diagram showing hydrography, temperature, and dissolved oxygen for Happy Valley Reservoir- 32 23. Diagram showing well- and spring-numbering system-34 24. Cross section showing probable conditions at Buck Springs- 35 25-31. Graphs showing water levels during drawdown tests of-- 25. Frank Suppah well-37 26. Sarena Boyd well- 38 27. Charles Jackson well-39 28. Elmer Quinn well- 39 29. Irene Wells well-40 30. Schoolie Flat 380-ft test well-40 31. Schoolie Flat 150-ft test well-41 32. Graph showing livability zones for rainbow trout-45 iv TABLES Page Factors for converting English units to International System Units (SI)---.--- v Table 1. Annual precipitation at selected weather stations in vicinity of Warm Springs Indian Reservation- 9 2. Selected streamflow data-24 3. Selected peak discharges-25 4. Daily discharge of the Warm Springs River, 1973-74- 52 5. Daily discharge of Shitike Creek, 1973-74- 54 6. Daily discharge of the White River, 1973-74- 56 7. Gain-loss investigations of the Warm Springs River and Mill Creek, 1973- 58 8. Coliform sampling at selected sites- 60 9. Turbidity and sediment sampling at selected sites-61 10. Chemical analyses of selected surface water-62 11. Streamflow measurements-63 12. Chemical analysis of water from Deschutes River near Biggs- 71 13. Quality of water in selected high lakes-72 14. Records of selected springs-73 15. Records of wells and test holes-76 16. Drillers' logs of wells-79 17. Chemical analyses of water from selected wells and springs- 83 FACTORS FOR CONVERTING ENGLISH UNITS TO INTERNATIONAL SYSTEM UNITS (SI) The following factors may be used to convert the English units in this report to the International System of Units (SI). The factors are shown to four significant figures; however, in the text the metric equivalents are shown only to the number of significant figures consistent with the values for English units. English Multiply by Metric acres 0.004047 2 km (square kilometres) acre-ft (acre-feet) .001233 hm (cubic hectometres) °F (degrees Fahrenheit) 5/9, after subtracting 32 o C (degrees Celsius) ft (feet) .3048 m (metres) ft /day (feet squared per day) .0929 2 m /day (metres squared per day) ft /s (cubic feet per second) .02832 m /s (cubic metres per second) 3 2 (ft /s)/mi (cubic feet per second per square mile) .01093 3 2 (m /s)/km (cubic metres per second per square kilometre) gal (gallons) 3.785 1 (litres) gal/min (gallons per minute) .06309 I/s (litres per second) in (inches) 25.4 mm (millimetres) mi (miles) 1.609 km (kilometres) mi (square miles) 2.590 km (square kilometres) tons (short) .9072 t (tonnes, or 1,000 kilograms) V Lake Simtustus WATER RESOURCES OF THE WARM SPRINGS INDIAN RESERVATION, OREGON By J. H. Robison and Antonius Laenen ABSTRACT Water-resources data for the 1,000-square-mile (2,600-square-kilometre) Warm Springs Indian Reservation in north-central Oregon were obtained and evaluated. The area is bounded on the west by the crest of the Cascade Range and on the south and east by the Metolius and Deschutes Rivers. The moun¬ tainous western part is underlain by young volcanic rocks, and the plateaus and valleys of the eastern part are underlain by basalt, tuff, sand, and gravel of Tertiary and Quaternary ages. There are numerous springs, some developed for stock use, and about 50 domestic and community wells; yields are small, ranging from less than 1 to as much as 25 gallons per minute (0.06 to 1.6 litres per second). Chemical quality of most ground water is suitable for stock or human consumption and for irrigation. Average flows of the Warm Springs River, Metolius River, and Deschutes River are 440, 1,400, and 4,040 cubic feet per second (12.5, 40, and 114 cubic metres per second), respectively. Shitike Creek, which has an average flow of 108 cubic feet per second (3.06 cubic metres per second) had a peak of 4,000 cubic feet per second (110 cubic metres per second) in January 1974. Chemical quality of the streams is good; most streams have fewer than 100 milligrams per litre of dissolved solids. Chemical and biological quality of the mountain lakes is also good; of 10 lakes studied, all had fewer than 50 milligrams per litre of dissolved solids and none had measur¬ able fecal coliform bacteria. 1 INTRODUCTION The Warm Springs Indian Reservation includes about 1,000 mi^ (2,600 km^), lying mostly in Jefferson and Wasco Counties of north-central Oregon (fig. 1). The reservation was established by a treaty of 1855 with the Tribes of Middle Oregon which are now referred to as the Warm Springs and Wasco Tribes. Tabulations of the Bureau of the Census show that in 1970 the reservation population was 1,324 in Jefferson County and 251 in Wasco County, or a total of 1,575. More than half the reservation is timberland, and timber is a major source of income. Grazing of horses and cattle is a substantial activ¬ ity, and cultivation of crops only a minor one. Recreation and tourism are rapidly increasing, attracted from outside the reservation by swimming, con¬ vention, and other facilities at the Kahneeta Hot Springs area. The present study is an inventory and appraisal of the water resources of the reservation, including determination of flow in major streams, yield of water to wells and springs, and quality of water. This study was conducted in cooperation with the Confederated Tribes of the Warm Springs Reservation. The cooperation and assistance of many officials of the Confederated Tribes, of the Bureau of Indian Affairs, and of the Indian Health Service helped greatly. Well-drilling and test-pumping data and other information generously furnished by Satish Puri, Tribal Engineer, were especially helpful. Selected technical terms used in this report are defined in a glossary on page 46. For use of readers who may prefer to use metric units rather than English units, the conversion factors for terms used in this report are listed at the front of the report. GEOGRAPHY The western boundary of the reservation lies generally near the crest of the Cascade Range. The Metolius and Deschutes Rivers form the southern and eastern boundaries. The northern boundary trends slightly north of west, beginning near lat 45° N. Altitude varies substantially, from 10,497 ft (3,199 m) on the top of Mount Jefferson, to about 1,000 ft (300 m) where the Deschutes River leaves the northeast corner of the reservation. The summit of the Cascade Range generally ranges from 4,000 to 6,000 ft (1,200 to 1,800 m) in altitude. The Cascade Range slopes eastward for 10 to 12 mi (16 to 19 km), where it abuts plateau uplands whose western edges lie at 2,600 to 3,600 ft (800 to 1,100 m), and then slopes eastward to about 2,400 ft (730 m). In the northeastern part of the area the Mutton Mountains rise to 4,000 ft (1,340 m). Plateaus in the southeast have been deeply dissected or removed entirely by the streams that drain eastward into the Deschutes River. 2 Hood River WCLAMTTTr Ort St^ • iTuWuin Rivar Crw* ■fiaptnitH C reak \Sj W>M » • 9 ?rr I fftflRSON Mancn Lam* Grizzly Min PnnevifTe ^TustonTjli 0 0 J__ I - 20 20 _l_ n 40 40 MILES 60 Kl LOMETRES INDEX MAP OF OREGON Figure 1. — Location of Warm Springs Indian Reservation. 3 GEOLOGY Rocks exposed on the reservation (pi. 1) range in age from early Tertiary to Holocene and include volcanic tuff, basalt, andesite, and asso¬ ciated rocks, and stream- and lake-deposited ash, sand, and gravel. Clarno Formation The Clarno Formation, the oldest unit, is exposed only in the north¬ eastern quarter of the reservation. It may underlie much of the reservation at unknown but varying depths, but younger formations cover and mask its true distribution. The Clarno was deposited between middle Eocene and early Oligocene time (Wolfe, 1972, p. 228). The Clarno Formation consists primarily of very resistant andesitic and basaltic rocks whose original texture and mineralogy have been slightly altered. Other volcanic rocks include breccia, tuff (compacted, fine-grained volcanic fragments), and tuffaceous siltstone. In many places, the topmost layer of the Clarno is a rather distinctive weathering layer of soft, reddish residual clay or silt known as saprolite. The Clarno Formation generally has a very low permeability, probably the least of all the formations. Yield of water to wells ordinarily can be ex¬ pected to be inadequate for most needs; however, a community well at Simnasho, which has a sustained yield of 10 gal/min (0.6 1/s), appears to be an exception. (See tables 15 and 17 in basic-data section.) Chemical quality of water from the Clarno is generally good. (See section on standards and table 17 of chemical analyses.) John Day Formation The John Day Formation overlies the Clarno Formation and is exposed in the central (including Agency) and northeastern parts of the area. The John Day formed within the late Oligocene and early Miocene Epochs (Peck, 1964) and, therefore, is about 20 to 30 million years old. The John Day Formation consists of air-fall and water-deposited ash, tuff, ash flows, welded tuffs, and rhyolitic flows. Much of the ash and tuff is soft and easily eroded, as in the lower Warm Springs River area and lower Skookum, Dry, Shitike, and Tenino Creeks areas. On the other hand, in many places the flows are resistant to erosion, as in the Mutton Mountains and the Eagle Butte-Kahneeta area; there the rocks may resemble some of those in the Clarno Formation. Parts of Eagle Butte and the Mutton Mountains were mapped as Clarno Formation by Hodge (1940) and later as John Day Formation by Waters (1968a). Material for the John Day Formation, which is as thick as 2,000 ft (600 m) , was probably extruded from volcanoes near the present site of the Cascade Range and east of the reservation. 4 Permeability of the John Day is very low, especially in the ash and other fine-grained units of the formation. By necessity, rather than by choice, many wells have been completed in the John Day, but yields typically range from inadequate to barely adequate. Chemical quality of water from the John Day Formation is variable; some exceeds recommended drinking-water limits for certain constituents. (See * section on standards and table 17 of chemical analyses, in basic-data section.) Columbia River Basalt Group The Columbia River Basalt Group is exposed on hills of the northern part of the reservation (Laughlin Hills) and on plateaus of the eastern part (Webster Flat). It occurs in Oregon, Idaho, and Washington and was formed during the Miocene and Pliocene Epochs, which extended from 26 to 3 million years before present. The Columbia River Basalt Group consists of basalt flows which are dense, hard, and not easily weathered or eroded, but where sufficiently fractured it will transmit water readily. On the reservation, the basalt is generally less than 300 ft (100 m) thick and lies mostly above the water table; a few springs occur locally, but the unit does not serve as an aquifer. In the Pine Grove-Wapinitia area north of the reservation, some deep irrigation wells penetrate the group and yield water from it. Most ground water from it is of good chemical quality. Dalles Formation The Dalles Formation is well exposed in the Seekseequa drainage area, in the middle Shitike and Tenino Creek areas, and in the canyons of the Metolius and Deschutes Rivers. At depth, the Dalles underlies the area of plateaus that include The Island; Schoolie, Mill Creek, and Miller Flats; and Tenino and Metolius Benches. The Dalles Formation was described by Waters (1968a) as consisting of "chiefly water-laid pumice-rich pyroclastic rocks, showing much cross-bedding and channeling. Contains numerous ash falls and less abundant ash flows, a few of which are welded. Also contains some interbedded basalt and andesite flows * * Those deposits that may be described as sandstone, gravel, or conglomerate are of particular interest because where they lie below the water table they usually serve as good aquifers. Total thickness of the Dalles is as much as 1,000 ft (300 m) in the Metolius River basin, but is generally less than 200 ft (60 m) in the Warm Springs River basin. In most places, the sedimentary deposits predominate, but near the Metolius and Deschutes Rivers, basalt may compose at least half the total thickness. 5 Basalt The unit mapped as "basalt" forms most of the plateaus in the central part of the reservation, including The Island; Schoolie, Mill Creek, and Miller Flats; and Tenino and Metolius Benches. Except where eroded, it usually caps the underlying Dalles Formation, and it is similar to basalt flows within the Dalles. In most places, the basalt is above the water table. It is not very permeable, but does affect movement of water and tends to perch ground water above the regional water table. The mapped unit is composed mostly of a dense, unweathered lava flow or flows, but drillers report sand and brown or red clay also. Thickness ranges from less than 50 ft (15 m) to more than 300 ft (100 m). Andesite The unit mapped as "andesite" occupies almost all the Cascade Range lying within the reservation. It is of Pliocene or Pleistocene age, with the high peaks generally consisting of the youngest rocks. The rocks include andesitic and basaltic lavas, mudflow, and pyroclastic (ejected volcanic) material. Overall, the formation is quite permeable, and it transmits water of excellent quality to many springs. Yields to some drilled wells, however, have been low. Gravel The formation mapped as "gravel" lies in the northwestern part of the reservation, generally between the base of the Cascade Range and the Warm Springs River. The gravel, of Pliocene or Pleistocene age, was derived from the andesitic rocks of the Cascade Range and was spread across the basalt- capped plateaus by eastward-flowing streams that antedated the present streams, which are deeply incised into the topography. In places, the gravel is more than 100 ft (30 m) thick. At best, only a few feet of the gravel is saturated with water, but the permeability is good, the water quality is good, and wells that produce water from this gravel are among the most productive on the reservation. Alluvium Alluvium occurs in deposits underlying or adjacent to rivers and streams throughout the reservation; only the more prominent or widespread are mapped separately from the underlying formations. Sources of the sand, gravel, and clay of the alluvium are mostly in the present drainage areas of the streams. Where it is sufficiently thick, the alluvium serves as an aquifer for the production of water by small-diameter wells. However, where the wells are shallow, they may be subject to pollution if they are improperly constructed. 6 HYDROLOGY Climate The climate is primarily continental, with some moderating effect due to the relative proximity of the Pacific Ocean. In summer, the climate in most of the reservation is generally arid, with very little rain from May through October, and maximum temperatures are near 100°F or 38°C (Celsius) for many days. Weather systems moving southward from Canada usually dominate winter months, but Pacific-spawned storms often cross the Cascade Range, dropping moisture and raising temperatures locally. The western part of the reservation lies on the slope of the Cascade Range, where the average annual precipitation is as much as 120 in (3,000 mm). In contrast, the eastern two-thirds of the reservation is in the rain shadow of the Cascade Range and the average annual precipitation there is only 10 in (254 mm) (fig. 2). Annual snowfall is about 200 in (5,100 mm) on the crest of the Cascade Range but diminishes to about 15 in (380 mm) on the lower and eastern part of the reservation. Table 1 shows annual precipitation at weather stations on or near the reservation and the variation that may occur from year to year. Monthly precipitation at Government Camp for 1973 and 1974 water years is shown in figure 3, which illustrates the monthly variation. Below-average snowfall in winter and early spring of 1973 resulted in a spring snowpack that was only 50 percent of normal for the Cascade Range. In 1974, snow accumulated throughout the winter and spring, resulting in a record spring snowpack. Streams and Streamflow At the start of this study, a continuous-stage recorder was installed on the Warm Springs River near Kahneeta Hot Springs, and a staff gage to be read daily was installed on Shitike Creek near Warm Springs. (See figure 4 for station locations.) Data from these stream-gaging stations were compared with long-term records collected at White River below Tygh Valley to define the pattern of flow (flow variability) during the 2-year study period. Figure 5, showing bar graphs of monthly runoff for the three stations, indi¬ cates seasonal variability in flow. The station on White River below Tygh Valley (14101500) was used for comparison purposes because (1) it is close geographically (see fig. 4), (2) it has a very long streamflow record (57 years), and (3) its basin lies in a topographic and climatic situation similar to the Warm Springs Reservation. 7 1 20°30 Hood River ill Otfianca'' \ 14103i ’otri »l»ur vviLLAWcm LINE ‘for rtjA f Raaervoin 7TK.-J,, 'T»ub £«•), River aiiwt »»« Creek _j Marion LakoQ) liman I.al e terimorid) &14075000 1 22°1 5' 45°45' 44° 1 5' 1 22°1 5' 45°45' 44° 1 5' 1 20°30' ? roel, /—•- f.**cenl Mi N I. - 1 j. '—i*-r— rr-^rw®"?^ , i Oi h* j> — L-. Jw j / Caviller /,-' i BMk»*o Cr»t«r£ »SJ *9 ' > Mtn : \ ' _ _\ 1 __ McKanr f P»n^ We* EXPLANATION 60-Precipitation, in inches 14075000 A c. ^ s', j, A Stream gage and Identification number -r O Rain gage \ Prinewille Cl ' C. r - 0 20 I- 1 -* i-H-r- 0 20 40 40 MILES “I- 1 60 Kl LOMETRES Figure 2. — Average annual precipitation, in inches. (Adapted from Columbia-North Pacific Technical Staff, 1970) 8 Table 1.-- Annual precipitation at selected weather stations in the vicinity of Warm Springs Indian Reservation [Based on records of the National Weather Service] Station Government Camp Lat 45°18' N. Long 121°45' W. Alt 3^980 ft Santiam Pass Lat 44°26' N. Long 121°56' W. Alt 3,780 ft Lat Long Alt Sisters 44°17' N. ; 121°32' W. 3,180 ft Simnasho Lat 44°58' N. Long 121°21' W. Alt 2,400 ft Madras Lat 44°38' N. Long 121°08' W. Alt 2,230 ft Calendar year Inches 1954 82.01 .. 7.82 1955 111.65 -- -- -- 9.79 1956 87.45 -- -- — 10.76 1957 79.62 — -- 15.85 12.84 1958 89.71 -- -- 13.80 8.92 1959 88.77 - - 8.62 - _ - - 1960 84.42 — 16.08 — 9.99 1961 99.35 -- 18.16 — 12.87 1962 85.53 — 13.85 — 11.63 1963 72.56 -- 12.94 — 11.31 1964 109.87 110.27 20.20 14.71 9.86 1965 65.70 71.27 11.80 9.56 9.57 1966 83.19 81.24 11.57 12.28 11.58 1967 79.58 80.16 12.59 -- 5.89 1968 101.51 96.53 12.52 — 10.99 1969 73.58 77.39 10.74 _ 13.54 1970 98.04 98.80 15.24 — 9.29 1971 113.43 -- 15.12 -- 9.05 1972 102.56 93.09 14.09 -- 8.97 1973 87.94 95.45 12.83 -- 10.82 1974 95.23 96.48 12.93 — 6.40 Average 90.08 90.07 13.71 13.24 10.10 9 / Figure 3, which shows the precipitation at Government Camp for 1973-74, should represent the precipitation pattern in the upper basins of the three aforementioned streams. Almost all major precipitation occurs from November through May, and snow starts to accumulate in November. Occasionally, rain and warm winter winds melt large volumes of snow, causing high winter flows such as occurred in 1974 (fig. 5). Figure 5 also shows 1973 as being a low runoff year and 1974 as a high runoff year. Figure 3.—Monthly precipitation at Government Camp, Oreg., 1973-74 water years. (Based on records of the National Weather Service.) 10 121 - 45 ' 1 21 ” 00 ' 11 3d±3l/\ICni» snvnos d3d CIN003S d3d Sd3±3lAI 01900 NI 'ddONOd 00 CN t— dodo 3HIAI 3dV00S d3d QN003S d3d 133d 01900 Nl 'ddONOd 12 Figure 5.—Monthly mean runoff of Warm Springs River, Shitike Creek, and White River, 1973-74 water years. Figure 6 is a graph of the mean monthly runoff of White River below Tygh Valley for 1917-74. It shows that the highest runoff normally results from snowmelt in the spring. All major streams on the reservation should have the same long-term variability as the White River and should normally experience maximum runoff periods in spring. Figure 6.—Mean monthly runoff of White River below Tygh Valley (14101500), 1917-74. Monthly measurements of selected streams, made during the 1973 water year, provided data to estimate mean annual and long-term average discharges and the variability of flow at each site. Figure 7 shows the relation of the mean flow in 1973 to the long-term average discharge for several streams. During the 1973 water year, flows in the Metolius and Deschutes Rivers were near average, but flows of the Warm Springs River, Shitike Creek, and several other streams on the reservation were only about three-fourths of average and White River below Tygh Valley was only 53 percent of average. These differ¬ ences probably reflect the carryover characteristics of a large ground-water reservoir in the Metolius and Deschutes Basins and a similar characteristic in the Warm Springs River basin. 13 10,000 o o LU co cc LU a. I— LU LU LL O m D O LU o DC < X o co < LU < 5 2 Z < CO 05 1. 2 . 3 . 4 . 5 . 6 . 7 . 8 . 9. 10 . 11 . MEAN ANNUAL DISCHARGE FOR PERIOD OF RECORD, IN CUBIC FEET PER SECOND 1 10 Lake Creek nr Sisters 14088000 Tumalo Creek nr Bend 14073000 Shitike Creek nr Warm Spr. 14093000 Squaw Creek nr Sisters 14075000 Deschutes R. nr La Pine 14050000 Warm Spr. R. nr Hehe Mill 14095500 White R. blw Tygh Valley 14101500 Warm Spr. R. n{ Warm Spr. 14097000 West Fork Hood R. nr Dee 141 18500 Metolius R. nr Grandview 14091500 Deschutes R. nr Madras 14092500 100 1000 - Above average flow -100 -10 100 - 1 100 1000 MEAN ANNUAL DISCHARGE FOR PERIOD OF RECORD IN CUBIC METRES PER SECOND 10,000 Figure 7.-Relation of annual mean discharges in 1973 to mean annual discharges for selected streams. Dependable low flow was determined by correlating measurements at a site to concurrent daily discharge at a long-term gaging station and then projecting this relation to the dependable low flow of the long-term Station (fig. 8). (See glossary for definition of dependable low flow.) The accuracy of dependable low flows for streams on the reservation is generally within 30 percent. 14 1973 ANNUAL MEAN DISCHARGE, IN CUBIC METRES PER SECOND FLOW OF SQUAW CREEK, IN CUBIC METRES PER SECOND 5 10 20 50 100 200 Figure 8.—Relation of low flow of the Whitewater River to concurrent flow of Squaw Creek (14075000). As the result of a rainstorm and warm temperatures that melted ice and snow, peak flows in January 1974 were unusually high. Peak discharges of some streams were measured directly or calculated indirectly. For streams within the reservation, the recurrence intervals of the floods were esti¬ mated on the basis of recurrence intervals of floods on nearby streams. As shown in figure 9, the January 1974 peak on the White River had a recurrence interval of about 15 years, and the December 1972 peak had a recurrence inter¬ val of about 2 years. 15 000 OS 0N003S B3d S3y±3lAI 019(30 Nl '3DyVH0SIQ 16 Warm Springs River Most of the surface flow in the northern two-thirds of the reservation is discharged by the Warm Springs River and its tributaries. The entire basin has an area of 540 mi^ (1,400 km^) and is the largest and most diverse on the reservation. Near its mouth, the river has a mean annual flow of 440 ft J /s (12.5 m J /s). In the upper part of the basin, snowmelt from fields, meadows, and lakes increases flow in spring and early summer. Substantial flows from springs issuing from beneath volcanic rocks on the slopes and foothills of the Cascade Range sustain streamflows in late summer and fall. In the lower part of the basin, which lies in a rain shadow, runoff occurs only when an intense storm passes through. Gain-loss investigation .--Two investigations of the Warm Springs River were made in late spring and in early fall 1973 to determine the magnitude and origin of the various sources of inflow. (See table 7, gain-loss investi¬ gations.) The following paragraphs explain the gains and losses of the Warm Springs River. All percentages of flow refer to the total flow at the mouth. (See figure 10.) 1 21 ° 45 ' 1 21 ° 00 ' 45 ° 00 ' Figure 10.—Percentage of flow at several points on the Warm Springs River and its tributaries compared to flow at the mouth. 17 Where the Warm Springs River enters the reservation at river mile 47.0, its flow was less than 1 percent. From the reservation boundary downstream, the flow of the main stem increased greatly in stair-step fashion due to many springs. At about river mile 41, the riverflow increased, in less than 0.3 mi (0.5 km), to about 25 percent. At this location, many small springs issue at a temperature of about 43°F (6°C) from the fractured basalt. Downstream, spring inflow in Warm Springs Meadow continued to increase the flow of the river in steps. The flow reached about 50 percent at Schoolie Bridge, river mile 36.3, which is about the eastern edge of the andesite. The South Fork Warm Springs River, which joins the main stem just below Warm Springs Meadow, contributed less than 1 percent of the flow. The first major tributary. Badger Creek, contributed only about 4 percent of the flow, with half its contribution issuing from springs just west of U.S. Highway 26. Mill Creek, the largest of the tributaries, contributed about 30 percent of the flow. The final major tributary, Beaver Creek, contributed about 15 percent of the flow. From the confluence of Beaver Creek to its mouth, the Warm Springs River showed no appreciable gain nor loss; minor spring inflow and evapotranspiration seemed to balance in the final reach of river. Because of its size and complexity, a separate gain-loss investigation was made for Mill Creek which contributes about 30 percent of the flow of the Warm Springs River. From its headwaters at river mile 24.0, flow of Mill Creek increased to river mile 15.8, where it was 55 percent of the total flow at the mouth. In the next 20 mi (32 km) along the stream, flow was lost by seepage into the sand and gravel. Boulder Creek also lost most of its flow, before it reached Mill Creek, to the sand and gravel. Although these losses reduce the available streamflow substantially, they serve as important con¬ tributions to recharge for the sand and gravel aquifers. Mill Creek flows are finally regained in the deep canyon west of U.S. Highway 26. Low flows .--The Warm Springs River near Kahneeta Hot Springs has a dependable flow of about 220 ft-^/s (6.2 m^/s). In 1973, one of the drier years of record, the 7-day low flow was 232 ft^/s (6.6 m-^/s), which has a recurrence interval of about 25 years. For the reach of the Warm Springs River below Beaver Creek, the Oregon State Department of Fish and Wildlife has suggested a June through August minimum flow, for fish propagation, of 80 ft3/s (2 m3/s) (written commun., K. E. Thompson, 1975). A flow of 80 ft3/s (2 m^/s) has a recurrence interval well in excess of 100 years. Water year 1973 represents a low stream runoff year for the Warm Springs River, and the data collected during that year can be useful for designing irrigation projects such as the proposed dam on the Warm Springs River near Hehe Mill. For example, 12,000 acre-ft (15 hm^) of reservoir storage would have been required in 1973 for irrigation and to maintain dependable low flows downstream. That storage, in addition to the direct diversion, would 18 have provided water to irrigate the proposed projects on The Island and Schoolie Flat (4,233 acres, or 17.13 kn/), based on irrigation requirements specified in a report by the U.S. Bureau of Indian Affairs (1969). About three times as much storage would have been required to supply water for the combined irrigable land on The Island, Schoolie Flat, Miller Flat, Dry Creek valley, and the bench above Shitike Creek. Peak flows .--For the most part, the river is confined within its banks during periods of high flow. The January 1974 peak at the gage site near the mouth had a magnitude of 6,350 ft^/s (180 m~Vs)--approximately a 15-year re¬ currence interval. Water quality .--Analyses of several water samples from the Warm Springs River and its tributaries show the water to be of excellent chemical quality, with low values of dissolved solids and hardness (table 10). The river above and below sewage lagoons near Kahneeta Hot Springs was sampled twice (table 8). Both sets of samples show a substantial downstream increase in coliform bacteria, which suggests that some incompletely treated waste water may have entered the river from the lagoons. The somewhat high values (see p.60) suggest that at times the river water below the lagoons may not be suitable for human consumption; periodic checks of conditions near the lagoons may be warranted. During winter storms, unusually large quantities of sediment enter the Warm Springs River from tributaries in the lower reach of the river (table 9). High sediment concentrations are the result of sparse vegetation, unconsoli¬ dated soils, and moderate to steep slopes. In contrast, as shown by data from Coyote Creek, sediment yields are small from the upper reach of Warm Springs River basin. Coyote Creek, a tributary of Beaver Creek, was sampled for sediment and turbidity (table 9). On the basis of the sediment-discharge relationship derived from the few samples collected, some gross estimates of yearly sedi¬ ment load can be made. The estimated yearly load for 1973 is 10 tons (9 tonnes), and the estimated yearly load for 1974 is 9,000 tons (8,000 tonnes). These values indicate relatively low sediment yields. The turbid¬ ity of the creek does not seem to be extremely high, but the stream does stay turbid even at near-zero flows. This phenomenon is attributed to mont- morillonite (clay) which remains in colloidal suspension. Shitike Creek O O Shitike Creek has a mean annual flow of 108 ft J /s (3.06 m J /s) near its mouth. Its drainage basin, which covers an area of 105 mi^ (272 km^) and is the second largest on the reservation, receives an average annual precipi¬ tation of more than 50 in (1,010 mm) (fig. 2). 19 Topographic divides in the upper basin do not necessarily define the drainage area because very permeable rocks permit substantial ground-water movement; hence, the basin may have more contributing drainage area than in¬ dicated in figure 4. Shitike Creek has a sustained spring runoff (fig. 5), probably due to late snowmelt from the steep north-facing slopes of its upper canyon. The creek also maintains a high base flow of more than 30 ft^/s (0.6 m-Vs) in late summer, because of ground-water inflow. The lower part of the Shitike Creek basin is in the same rain shadow as the Warm Springs River basin. Low flows .--In late summer, when base flow occurs, the creek gains flow from its headwaters at river mile 33 downstream to river mile 22, near the eastern edge of the andesite. Between Shitike Butte and the mouth of Wolford Canyon (river mile 5.5), the change in streamflow is insignificant, which is consistent with the very low summer flow of Seekseequa Creek and the zero summer flows of Tenino and Dry Creeks. Downstream from Wolford Canyon, the creek loses some flow into the gravel that forms the valley floor. Shitike Creek near Warm Springs has a dependable flow of about 28 ft^/s (0.79 m^/s). In 1973, a low summertime flow of 33 ft^/s (0.93 m^/s) occurred in September 1973. During a period of ice effect in December 1972, however, the low flow was 20 ft-Vs (0.57 m-^/s). In figure 11, low flows may be com¬ pared with minimum and optimum flows for fish suggested by the Oregon State Department of Fish and Wildlife (K. E. Thompson, written commun., 1975). Peak flows .--Shitike Creek near its mouth had higher peak flows than did nearby streams with drainage basins of comparable size. In January 1974, the peak on Shitike Creek was estimated as 4,000 ft^/s (110 m^/s). This flood topped the banks in the lower reaches and caused considerable bank erosion and movement of gravel along the channel. During floodflows, the channel has a tendency to meander within the width of the valley floor, which should in¬ fluence the design or location of structures proposed for the area. Based on records from nearby long-term stations, the recurrence interval for the January 1974 peak appears to be greater than 20 years. Water quality .--Shitike Creek water is of excellent quality; it is low in dissolved solids, hardness, and specific conductance (table 10). One set of samples taken above and below the sewage lagoons near Warm Springs Agency showed a coliform count well below recommended levels and no significant in¬ crease below the lagoon (table 8). Whitewater River Most of the Whitewater River drainage area is on the slope of the Cascade Range, but the lower part lies on the edge of the rain-shadow area. The entire river course is in a deep canyon which usually retains snow until late summer. In addition, melt water from the Whitewater Glacier of Mount Jefferson also helps to sustain the summer flow of the river. The glacier acts as a self-regulating reservoir because the rate of glacial melting depends on temperature and sunshine, increasing on bright, hot days and de¬ creasing on cool, overcast days and at night. Suspended rock flour in the melt water causes the river to become turbid when the rate of glacial melting is high. 20 5000 o o o QN003S d3d S3H13IAI 31903 Nl 'AA01dl/\IV3aiS S o o o o o o o in (n in cn t- in QN003S d3d 1333 31903 Nl 'M033IAIV3H1S 21 Figure 11Streamflow of Shitike Creek, 1973-74, compared to suggested optimum and minimum flows for fish life. The mean annual flow of the Whitewater River, near its mouth, is 105 ft 3 /s (3.0 m 3 /s). Average flow in July and August 1973 was about 70 ft 3 /s (1.4 m 3 /s). In July 1973 the entire flow of the river would have irrigated only 2,700 acres (11 km 3 ), although irrigation projects requiring water from the Whitewater River have been proposed for 2,914 acres (11.79 km 3 ) (U.S. Bureau of Indian Affairs, 1969). Jefferson Creek Jefferson Creek has a mean annual flow of 110 ft 3 /s (3.12 m 3 /s) near its mouth. The creek has the poorest defined drainage basin on the reservation because the areal extent of ground-water contribution is not known. The creek drains Waldo Glacier, a small part of Whitewater Glacier, and several high lakes and snowfields. It also lies in an area of diverse geology and next to a large lava flow. High permeability of the lavas enables ground water to sustain summer flows and gives the stream the highest base flow per square mile of all the streams on the reservation. Jefferson Creek never seems to become turbid, as the Whitewater River does, even though it also carries glacial melt water. Metolius River The Metolius River, just below the confluence of Jefferson Creek (fig. 4), has a mean annual flow of 1,400 ft 3 /s (40 m 3 /s). It has one of the highest base flows per square mile of drainage area of any stream in Oregon, being sustained by the many springs and other large ground-water contributions from very‘permeable volcanic rocks. The head of the Metolius is a huge spring where about 100 ft 3 /s (2.8 m 3 /s) issues from the base of Black Butte. In the 10 mi (16 km) from the headwaters to the reservation boundary, tributaries are few but flow increases more than tenfold. Running parallel to the crest of the Cascade Range, the Metolius intercepts almost all the flow from the crest eastward to its channel. The high permeability of the rock formations adds to flow in one segment of river but it may also decrease it in another. A comparison of concurrent records of flow indicates that losses are substantial in the reach between Jefferson Creek and the Whitewater River. The losses are regained in the lower reach between the Whitewater River and its mouth at the Deschutes River. At its confluence with the Deschutes River in Lake Billy Chinook, the Metolius River drains an area of 450 mi 3 (1,170 km 3 ) and has a mean annual flow of about 1,550 ft 3 /s (44 m 3 /s). On the basis of the limited sampling done, water quality appears to be excellent in the Metolius River, including the Metolius arm of Lake Billy Chinook where occasional algae blooms occur (McHugh, 1972). Deschutes River Where the Deschutes River reaches the south boundary of the reservation, it has a mean annual flow of about 4,040 ft 3 /s (114 m 3 /s) , including the flow of the Metolius River. At the north boundary of the reservation, the Deschutes has a mean annual flow of about 5,300 ft 3 /s (150 m 3 /s), including major contributions from Willow Creek, Campbell Creek, Shitike Creek, the 22 Warm Springs River, and Trout Creek. Flows of most creeks entering the Deschutes from the east are supplemented by return of water originally di¬ verted from the Deschutes for irrigation. The reach of the river bounding the reservation has two major dams. Lake Billy Chinook is formed behind Round Butte Dam which backs water far up the Metolius River. Lake Simtustus is formed behind Pelton Dam. Water quality .--Chemical quality of Deschutes River water is excellent; it is low in dissolved solids, hardness, and specific conductance (table 12). The coliform concentration in water at the outlet of Lake Billy Chinook (table 8) indicated a level just below the State standard. However, water collected from the Deschutes River just above its confluence with Shitike Creek near Warm Springs Agency, had a significantly lower coliform concen¬ tration than the water below Lake Billy Chinook. Very high coliform concen¬ trations were found in water from Willow and Campbell Creeks which flow into the Deschutes River between Lake Billy Chinook and Shitike Creek (table 8). Other Streams Most other streams on the reservation have little flow, because they lie in the rain shadow and have little or no drainage area on the slope of the Cascade Range. Most of these streams, regardless of drainage-area size, are ephemeral or nearly so. Seekseequa Creek, with a drainage area of about 50 mi^ (130 km^) is nearly dry in summer. Dry Creek, with a drainage area of 35 mi^ (90 km^), is dry in summer. The total mean annual flow of these two streams is only about 8 ft^/s (0.23 m^/s). Streams that flow into the Metolius River between Jefferson Creek and the Whitewater River have flows totaling about 25 ft^/s (0.7 m^/s), but individually do not have significant flows. Table 10 shows that no undesirable concentrations of objectionable chemical constituents were noted in any of the smaller streams on the reser¬ vation. Even streams adjacent to the reservation that had high levels of coliform had good chemical quality at the time of sampling. Except for the high iron concentration in water from Skookum Creek, all the analyzed chemical constituents were well below recommended limits for drinking water. (See basic-data section.) Streamflow Distribution The Warm Springs River, Shitike Creek, the Whitewater River, and Jefferson Creek are the major streams on the reservation. Streamflow from the reservation, on a mean annual basis, is approximately 740 ft J /s (21 m J /s) or 17 percent of the total flow of the Deschutes River at the northeast corner of the reservation. The Metolius River receives 180 ft^/s (5.1 m J /s), or 12 percent, of its mean annual flow from the reservation. Table 2 sum¬ marizes drainage area, mean flow, and dependable flow (see glossary for defi¬ nition of dependable flow) for 34 streamflow sites on or near the reservation. Discharge measurements made during this study are given in table 11. 23 Table 2.--Selected streamflow data Drain- Estimated flows age 1973 Mean annual Dependable Station number Stream name area (mi 3 ) mean (ft 3 /s) (ft 3 /s) [(ft J /s) /mi 3 l low flow (ft 3 /s) 14090200 Metolius River 163 1,300 1,300 8.0 1,000 14090350 Jefferson Creek 27.8 82 110 4.0 32 14090500 Whitewater River 31.8 76 105 3.3 33 14091500 Metolius River!./ 316 1,501 1,490 4.7 1,090 14092150 Seekseequa Creek 47.3 2.7 6.7 .14 .7 14092500 Deschutes River!/ 7,820 4,497 4,434 .57 1,200 14092900 Tenino Creek 20.7 -- 1.0 -- 0 14093000 Shitike Creek!/ 105 75 108 1.0 28 14093510 Dry Creek 33.7 .2 1.5 .04 0 14094000 Warm Springs River 18 — 15 -- 1.0 14095500 Warm Springs River 107 150 180 1.6 95 14095600 Badger Creek 37.2 24 28 .75 5.0 14096000 Mill Creek 5.4 — 3.5 — >.01 14096500 Mill Creek 28.8 -- 70 -- 20 14096550 Mill Creek 57.6 56 72 1.2 20 14096600 Boulder Creek 28.4 11 27 .95 0 14096700 Mill Creek 140 -- 110 -- 55 14096800 Beaver Creek 32.1 38 44 1.4 7.0 14096820 Coyote Creek 43.2 2.4 7.5 .17 0 14096830 Beaver Creek 115 61 79 .69 26 14096840 Quartz Creek 35 - - 5.0 - - 0 14097100 Warm Springs r!/ 526 330 440 .84 220 14097110 Skookum Creek 10.9 -- 1.0 -- 0 14097200 Eagle Creek 24.4 .3 1.0 .04 0 14097210 Deschutes River 9,330 — 5,300 -- 2,300 14097220 Nena Creek 15.9 .3 1.0 .06 > .01 14097230 Paquet Gulch 6.4 .2 .5 .08 0 14101500 White River!/ 417 228 427 1.0 74 14178500 Breitenbush River 1.6 -- 3.5 — .6 14207930 Slow Creek .8 — 2.0 -- .2 14207940 Lemiti Creek 3.4 — — 6.0 - - 0 14207950 Olallie Creek 1.6 -- 1.0 — 0 14208410 Oak Grove Fork 12.0 — 20 — 0 14208420 Clackamas Lake tributary 1.1 .5 0 1/ Daily streamflow site. 24 Nearly all streamflow on the reservation originates within or adjacent to its boundaries (fig. 4); Jefferson Creek and the Metolius and Deschutes Rivers, which serve as the south and east boundaries, derive streamflow both from within and outside the reservation. Less than 1 percent of the surface flow on the reservation originates outside the reservation, primarily from the uppermost reach of the Warm Springs River and from the outflow of Olallie Lake to Mill Creek. Because north and west boundary lines approximate major drainage divides, only minor streamflow crosses them. Less than 1 percent of the surface flow originating on the reservation leaves the reservation across its north and west boundaries, primarily in Paquet Gulch, Nena Creek, the Oak Grove Fork of the Clackamas River, Lemiti Creek, and the outflow of Breitenbush Lake. Of the streams that bound the reservation, Jefferson Creek is the only one that serves as a boundary for its entire length. The boundary divides the Jefferson Creek drainage approximately in half, and about half the flow is derived from the reservation. Except for 1941, in the past 50 years the lowest stream runoff from the reservation for many streams occurred in 1973. Thus, data for 1973 represent a near extreme, and should be valuable for planning. Peak flows in January 1974 had recurrence intervals of greater than 20 years on Shitike Creek, 15 years on the Metolius River, and 10 years on the Deschutes River. (See table 3.) During the winter of 1964-65, one of the Table 3.-- Selected peak discharges Station number Stream name Drainage area, in • 2 mi Discharge, in cubic feet per second Dec. 1964 Dec. 1972 Jan. 1974 May 1974 14090350 Jefferson Creek 27.8 350 _ _ _ _ 14090500 Whitewater River 31.8 — 670 160 14091500 Metolius River 316 7,530 2,910 4,370 1,900 14092150 Seekseequa Creek 47.3 -- — 1/400 8.7 14092500 Deschutes River 7,820 15,800 9,660 8,400 — 14092900 Tenino Creek 20.7 - - — 1/80 -- 14093000 Shitike Creek 105 690 1/4,000 425 14093510 Dry Creek 33.7 — 125 — 14095600 Badger Creek 37.2 -- — -- 109 14096550 Mill Creek 57.6 — — — 199 14096600 Boulder Creek 28.4 — — 124 14096820 Beaver Creek 71.5 — -- 1,200 208 14096830 Coyote Creek 43.2 -- — 970 -- 14096840 Quartz Creek — — — 1/200 — 14097100 Warm Springs R 526 — 1,560 6,350 1,030 14097230 Paquet Gulch 6.4 — - — 140 14101500 White River 417 11,300 2,830 7,910 1,510 1/ Estimate. 25 wettest seasons of record in Oregon, peak flows of streams near the reserva¬ tion had recurrence intervals ranging from 40 to more than 100 years. The May 1974 discharges in table 3 represent peaks from snowmelt. Quality of Streamflow Water samples were taken during the summer when it was expected that chemical quality would be poorest and biological activity would be at its highest level. Generally only one sample was taken per site, and specific changes in quality (either seasonal or long-term) were not documented. Chemical quality of streams on the reservation generally is excellent (table 10). A complete analysis was made of a sample collected in October 1974 from the Deschutes River at the mouth near Biggs, Oreg. (table 12). (See figure 2.) The analysis indicates the very good quality of water in the basin. Biological quality of water is highly variable and extremely dependent on temperature, nutrient, and source conditions. Taken about months apart, samples of the Warm Springs River near the sewage lagoons show a large range of total coliform in the river (table 8). Only general conclusions are warranted from analysis of biological samples taken on any one day. From the limited sampling done, biological quality seems generally good for all streams on or bordering the reservation. Lakes and Reservoirs Many high-altitude lakes and several reservoirs are on or adjacent to the reservation. In October 1974, 10 high lakes and one reservoir were visited to obtain selected data. Data for the reservoirs, Lake Billy Chinook, and Lake Simtustus were obtained indirectly and from other reports. High lakes .--Hydrography of the lakes--their inflows, outflows, and depths--are shown in figures 12 through 21. Most of the lakes are formed in depressions in the rough topography of young volcanic rocks. Those lakes that have little or no ground- or surface-water inflow receive water only from direct rainfall and snow accumulation in the depressions. All the high lakes are bog-type lakes with bottoms composed of fallen trees, talus, and mud ooze. High lakes of the reservation have water of excellent quality. Data for temperature and dissolved-oxygen profiles were collected at the deepest point in each lake. (See figures 12-21.) Table 13 shows the parameters that were analyzed for 10 of the lakes. In many instances, dissolved solids in these lakes were of the same concentrations as would be expected in local rainwater or snow. Because the volcanic rocks in the Cascade Range are subject to little chemical weathering, dissolved solids in the lakes are likely to remain low. There is no evidence of bacteriological pollution, even though there is recreational activity at most of the lakes. Unless the lakes are highly overused, the quality of their water should remain excellent. 26 Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitude 44°45'1 2" 1 21°46'02" 1974 24 5250 N 300 METRES TEMPERATURE, IN DEGREES CELSIUS 13 14 15 DISSOLVED OXYGEN, IN MILLIGRAMS PER LITRE Figure 12.—Hydrography, temperature, and dissolved oxygen for Harvey Lake. Location of Sampling site (▼) Date of survey Surface area (acres) Lake elevation (feet) Latitude Longitude 44° 46'34” 121°46'36” 12-74 1.8 5560 o o 500 FEET “I* 150 METRES TEMPERATURE, IN DEGREES CELSIUS 8 9 10 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 13.—Hydrography, temperature, and dissolved oxygen for Spoon Lake. 27 Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitute 44°47'57" 121°45'51" 9-12-74 28 4840 From Olallie Lake 2-3 gal/min. Shallow Depth, in feet To Dark Lake 1000 FEET -t 300 METRES TEMPERATURE, IN DEGREES CELSIUS 12 13 14 LU LU 20 Q. LU Q 30 1 ■ 1 / / < \ T ' \ \ V 7 / J : / o J_1 . / i / J - 1 w LU DC . P- 4 LU 6 CL _ UJ 8 Q -10 5.5 6.5 7.5 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 14.—Hydrography, temperature, and dissolved oxygen for Long Lake. Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitute 44°47'49" 121°45'29” 9-12-74 23 4700 o o 1000 FEET 300 METRES TEMPERATURE, IN DEGREES CELSIUS 13 14 15 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 15.—Hydrography, temperature, and dissolved oxygen for Dark Lake. 28 Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitude 44°47'42" 121 °44'48" 9-17-74 28 4685 1000 feet J 300 METRES 1 1 TEMPERATURE, IN DEGREES CELSIUS 12 13 IN MILLIGRAMS PER LITRE Figure 16.—Hydrography, temperature, and dissolved oxygen for Island Lake. Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitute 44-48W' 1 21°44'05” 9-17-74 23 4419 0 1000 FEET I-1- 1 -r-^ 0 300 METRES TEMPERATURE, IN DEGREES CELSIUS 12 13 14 15 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 17.—Hydrography, temperature, and dissolved oxygen for Trout Lake. 29 Location of Sampling Site (t) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitude 44°47'05" 1 21°43'31” 9-18-74 50 4651 TEMPERATURE, IN DEGREES CELSIUS Figure 18.—Hydrography, temperature, and dissolved oxygen for Boulder Lake. Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitude 44°50'36'' 1 21°44'20" 9-18-74 13 5058 I- 1 -'- 1 -r 0 300 METRES TEMPERATURE, IN DEGREES CELSIUS 12 13 14 15 16 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 19.—Hydrography, temperature, and dissolved oxygen for Blue Lake. 30 Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitude 44°26'26'' 1 21°46'44'' 9-13-74 5 5650 N 150 METRES TEMPERATURE, IN DEGREES CELSIUS 10 11 12 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 20.—Hydrography, temperature, and dissolved oxygen for Gibson Lake. Location of Sampling Site (T) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitude 44°46’13" 121°46'38" 9-11-74 55 5500 TEMPERATURE, IN DEGREES CELSIUS 11 12 13 DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 21 .—Hydrography, temperature, and dissolved oxygen for Breitenbush Lake. 31 Reservoirs .--Happy Valley Reservoir is formed by an earth-fill dam across Quartz Creek just southeast of Simnasho. During most of the summer there is no inflow nor outflow to the reservoir, and only winter rains and spring runoff from snowmelt sustain its level. A chemical analysis of Happy Valley Reservoir (see table 10) shows the good chemical quality of the water, with all analyzed constituents well below recommended limits. The fecal coliform content was 14 colonies/100 ml. Tem¬ perature and dissolved-oxygen profiles were made at the deepest point in the reservoir (fig. 22). Lake Billy Chinook and Lake Simtustus are part of the Deschutes River system and form part of the reservation boundary. Flow through the reser¬ voirs is large compared to their storage capacities; water constantly moves through them even in summer. Algae blooms occurring in late summer suggest that a warm, slow-moving or stagnant upper layer of water overlies a cooler, faster moving lower layer. Mullarkey (1967) observed that Lake Billy Chinook is stratified, and that in the Metolius arm, the upper layer usually moves upstream with the wind. Chemical analyses and coliform sampling for Lakes Billy Chinook and Simtustus are discussed under the section "Deschutes River" (p. 22). Because blue-green algae blooms occur in both lakes (McHugh, 1972), they probably receive some nutrient enrichment in suspended form. Nutrients probably do not attain very high levels because blue-green algae blooms usually occur in a low-nitrogen environment and late summer should provide the most favorable environment. Location of Sampling Site (▼) Date of Survey Surface Area (acres) Lake Elevation (feet) Latitude Longitute 44°58'08" 121°19'17'' 9-17-74 13 2500 No flow 200 METRES TEMPERATURE, IN DEGREES CELSIUS 12 18 co LLI DC h- LU CL¬ UJ O DISSOLVED OXYGEN IN MILLIGRAMS PER LITRE Figure 22.—Hydrography, temperature, and dissolved oxygen for Happy Valley Reservoir. 32 Ground Water Occurrence and Movement Ground water lies beneath the land surface, filling or saturating the openings of the rocks or deposits in which it occurs. An aquifer is a for¬ mation or part of one that contains sufficient saturated material to yield significant quantities of water to wells or springs. Where the upper surface of the ground-water body is at atmospheric pressure, the surface is called the water table; most of the ground water on the reservation occurs under water-table conditions. Perched ground water is separated from an underlying body of ground water by an unsaturated zone; perched water may occur in a few places on the reservation, including part of Schoolie Flat. Confined or artesian ground water has a hydraulic head (or a water level, in a well that penetrated an aquifer) that is above the top of the aquifer; no confined water has been observed on the reservation. The sources of ground water are precipitation, which percolates downward through unsaturated, permeable material to the water table, and water lost by leakage from lakes or streams that may lie temporarily or permanently above the water table. Ground water may leave an aquifer in several ways. Where the water table is shallow, it may contribute directly to the flow of a stream or the level of a lake, it may emerge locally as springs, it may evaporate at the land surface, or it may supply plants which transpire water to the atmosphere. On the res¬ ervation, a small quantity of ground water is withdrawn from wells. Movement of ground water within an aquifer is mostly lateral, from areas where altitude of the water table is high to areas where it is low; the movement is gener¬ ally parallel to the general slope of the topography. Ground water in the Warm Springs Indian Reservation moves very slowly, but rather steadily, eastward from the Cascade Range, where the topography and the water table are highest and precipitation is greatest. In the process, some of the ground water is intercepted by the larger streams that cross the reservation. Not all the ground water moves eastward; some, for example, moves westward from its source in the Mutton Mountains across Schoolie Flat and is intercepted by Beaver Creek or the Warm Springs River. The altitude (or depth below land surface) of the water table is known or may be inferred at selected points throughout the reservation, but in only a few areas is the water table regular enough or its level documented adequa¬ tely enough that it can reasonably be portrayed on a map. Areas where the water table can be portrayed are the northern plateaus (see pi. 1) that lie between Shitike and Beaver Creeks, and part of Schoolie Flat. Water-table contours, based on water levels in wells and the altitudes of streams, are shown at intervals of 100 ft (30 m). The water table is relatively smooth because the area is underlain by the Dalles Formation and the gravel and basalt units, which are fairly permeable and allow ground water to move freely. In areas underlain by less permeable rock, the water table can be ex¬ pected to be quite irregular, reflecting the topography and generally occur¬ ring at depths of less than 100 ft (30 m). 33 Springs Springs may occur where the water table intersects the land surface or where the land surface is intersected by formations with good permeability overlying those with low permeability. Springs are more likely to occur in areas where aquifers receive the most recharge from precipitation, as in the Cascade Range where they are abundant. However, springs may be found throughout the reservation wherever geologic conditions are favorable. Selected springs are shown on plate 1, and data for the springs are given in table 14. (See figure 23, well- and spring-numbering system.) In the drier, eastern part of the reservation, many of the springs are the prin¬ cipal or sole local source of domestic or stock water. In the mountainous western part, perennial streams are abundant and there are few people and livestock; thus, there is little need to depend on springs. Springs, in addition to those inventoried for this study, are shown on U.S. Geological Survey quadrangle maps at scales of 1:24,000 and 1:62,500. Figure 23.-Well- and spring-numbering system. 34 Springs occur in a variety of environments, but a few generalizations are relevant. Springs are more likely to lie near the bottom of a canyon, where the water table is nearest to the surface, than on a topographic high. A spring is more likely to emerge where a steep slope breaks into a gentle one, because the break may represent the contact between two geologic units that control movement of ground water. Buck Springs (8S/12E-29dbb), one of the largest on the reservation, is an example of a geologically controlled spring that discharges from a perched ground-water body. The springs emerge from talus (loose rock) in the canyon (see fig. 24) several hundred feet above the river. Source area of its water is Miller Flat, including the upper Dry Creek drainage. The ground water probably moves through permeable gravels at the top of the Dalles Formation where the Dalles underlies basalt and overlies the poorly permeable John Day Formation. The ground water moves eastward beneath Miller Flat until it reaches the canyon of the Warm Springs River, but it is unaffected by local topography and does not follow the upper Dry Creek channel where it bends to the southeast. Consequently, Dry Creek does not receive ground water that would otherwise be expected to contribute to the minimum flow of the stream. Figure 24.—Cross section showing probable conditions at Buck Springs (8S/12E-29dbb). 35 Many springs have been artificially developed for stock or domestic supplies, using collectors, piping, and storage facilities to obtain maximum yield or maintain sanitary protection. (See U.S. Public Health Service, 1962b, for descriptions of typical methods.) Springs need not have a large flow to be adequate; with storage tanks or cisterns, springs yielding as little as 1/8 gal/min (0.01 1/s) could supply water for more than a dozen horses or one small family. Hot Springs A group of warm or hot springs lies adjacent to the Warm Springs River in secs. 19 and 20, T. 8 S., R. 13 E. The springs are along a 1%-mi (2%-km) reach of the river, lie several hundred feet or less from the river, and issue only a few feet above river level. Discharges of individual springs range from small seeps to the 50 gal/min (3 1/s) estimated for the spring (8S/13E-20adc) that supplies the resort at Kahneeta Hot Springs. The springs that can be pinpointed and observed flow directly from fractures in rhyolite or welded tuff of the John Day Formation. Water from some springs may also be transmitted through rock fractures, but is dispersed through the overlying stream gravels. Temperatures of the hot springs vary, but are as great at 182°F (83.5°C) (8S/13E-19bad). Temperature of the spring supplying the resort fluctuates seasonally from about 117° to 126°F (47° to 52°C). Wells More than 50 wells or test holes have been drilled on the reservation for stock water, individual domestic supplies, and community supplies. Data for wells for which records are available are contained in table 15, and logs of wells, based on drillers' reports, are in table 16. The logs, adapted to a uniform format, include descriptions and depths of materials penetrated by each well and the authors' interpretations of which formations are represented. Altitude (above sea level) of the base of each unit is based on the land-surface altitude estimated from a topographic map. Well yields vary from one formation to another and from place to place-- from less than \ gal/min (0.03 1/s) to about 30 gal/min (2 1/s). Wells or test holes that obtain water totally or primarily from the Clarno Formation generally have low yields, and most probably will yield less than 2 gal/min (0.1 1/s) on a continuous basis. Yields of the Florence Pete test hole (7S/llE-14abd) and the Schoolie Flat 400-ft (120-m) test well (7S/12E-29cdd) were inadequate and the wells were never used. In 1955, S. G. Brown of the Geological Survey made a pumping test of the Frank Suppah well (7S/12E-34cab), which is probably completed in the Clarno Formation (fig. 25). Varying rates of pumping made the results difficult to interpret, but Brown concluded that the well yielded about 4 gal/min (0.25 1/s) on a short-term basis and that its sustained yield would be about 2 gal/min (0.13 1/s) or 3,000 gal/day (10,000 1/day). The test shows that the well taps rocks of low permeability. 36 The Simnasho community well (7S/12E-7dbb) may draw water from the Clarno Formation, although no driller's log is available to verify the aquifer. The reported yield, as much as 22 gal/min (1.4 1/s) during a short-term test and as much as 10 gal/min (0.6 1/s) on a continuous basis, is unusually high for a formation as poorly permeable as the Clarno is in most places. Because of its low permeability, the John Day Formation is not generally a good aquifer, although a number of wells and test holes have been drilled to develop water from it. Reported yields of short-term tests range from less than 1 to more than 10 gal/min (0.06 to 0.6 1/s); sustained yields probably would average less than 2 gal/min (0.12 1/s). The 250-ft (76-m) Sarena Boyd well (8S/13E-27cdc), which produces water from the John Day Formation, was test pumped for 4% hours on April 23, 1973 (fig. 26). During the first 2 hours of the test the drawdown was 28 ft (9 m) at a pumping rate of 5 gal/min (0.3 1/s). When the pumping rate was increased, first to 8 and then to 10 gal/min (0.5 to 0.6 1/s), the drawdown increased to 216 ft (65.8 m). Sustained yield of the well is unknown, but may be several gallons per minute or less. The Charles Jackson well (10S/12E-lcaa2), which is within 1/8 mi (200 m) of the Deschutes River, probably could yield as much as 3 or 4 gal/min (0.2 or 0.3 1/s) on a steady basis (fig. 27). 80 E £ 120 < Z UL — oc £ ^ < i 160 n fS SS 200 Q 1 5 gal/rninj 11.3 gal/min. gal/min. ^.Statjc level H \| , • • • • 7.4 *• • • • 6.9 240 n- 1 -1—i—i—rr Test on December 2, 1955; observed by S. Brown of U.S. Geological Survey. Well diam. 6in., total depth 300 ft. j_i_i l i -i-1-1-1—i—i—rr 7.9 gal/min. 7.5 8.9 J_i_1 .1 I. 30 co HI QC LU - 40 tL < 2 u- - CO DC Q h50£ z - 60 < 5 o I- I LU I- co a. LU O - 70 2 5 10 20 50 TIME SINCE PUMPING STARTED, IN MINUTES 100 Figure 25.—Water levels during drawdown test of Frank Suppah well 7S/12E-34cab. 37 Figure 26.—Water levels during drawdown test of Sarena Boyd well 8S/13E-27cdc. The Dalles Formation also is an aquifer that has rather low permeability. Tests made in two wells producing water from the Dalles Formation indicate that sustained yields might range from 3 to 12 gal/min (0.2 to 0.8 1/s). The Elmer Quinn well (8S/llE-25ccc) was tested at 17 to 18% gal/min (1.1 to 1.2 1/s) (fig. 28). By the end of the 4-hour test, the water level had stabi¬ lized, indicating that the well had intercepted a source of replenishment to the aquifer. The Irene Wells well (8S/llE-33ddd) was tested at 12 gal/min (0.76 1/s) with about 33 ft (10 m) of drawdown (fig. 29). Within about 2 hours the water level stabilized in a manner similar to that of the Quinn well. On Schoolie Flat, a test well 380 ft (116 m) deep (8S/12E-3cac), com¬ pleted in basalt overlying Clarno Formation, was tested initially at 2 gal/min (0.12 1/s) (fig. 30). Well 8S/12E-3cab is 150 ft (46 m) deep, and within several hundred feet of well 8S/12E-3cac. Well -3cab is completed in alluvium or basalt and has a shallower static water level than -3cac, suggesting that it may be perched above the water table. During one (fig. 31) of two pumping tests, the level dropped about 20 ft (6 m) in 2 hours of pumping at 3 gal/min (0.2 1/s). When the pumping rate was increased to 5 gal/min (0.3 1/s), the water level dropped rapidly, as it might if a shallow zone in the aquifer were dewatered. During a later test (not included in this report), the well was pumped for 4 hours at an average rate of 2.7 gal/min (0.17 1/s), drawing the water level down 20 ft (6 m), but without dewatering the shallow zone. 38 DEPTH TO WATER, IN FEET BELOW LAND SURFACE DEPTH TO WATER, IN FEET BELOW LAND SURFACE 60 80 100 120 140 160 180 "1 I I-1-1-TT _S_tatic level • • J_L J_I_ l l l i i i i—i—i—rr n-r 1 7 gal/min. 1 0 gal/min. 8 gal/min •• J_I_I_I_I_L 6 gal/min. /N - 30 J_I_L 2 5 10 20 50 100 200 TIME SINCE PUMPING STARTED, IN MINUTES Figure 27.-Water levels during drawdown test of Charles Jackson well 10S/12E-lcaa2. 20 m o < li¬ ar D co 6 UJ 00 CO UJ a: i— UJ -- 40 cc UJ I- < § o I- X I- Q- LU 50 O 500 298 299 300 301 i-1—i—i i I J_I_1111 -1-1-1-1-1-TTT Test on June 21, 1973; observed by S. Puri for Indian Health Service and J. Robison of U.S. Geological Survey. Static level 293.4 ft. below top of well casing. 1 7 gal/min. I - 17.5 gal/min. 18.5 gal/min. I I l l I • • 5 10 20 50 100 TIME SINCE PUMPING STARTED, IN MINUTES 200 - 91.0 - 91.2 91.4 h 91.6 500 Figure 28.—Water levels during drawdown test of Elmer Quinn well 8S/11 E-25ccc. 39 DEPTH TO WATER, IN METRES BELOW LAND SURFACE DEPTH TO WATER, IN FEET BELOW LAND SURFACE DEPTH TO WATER, IN FEET BELOW LAND SURFACE 240 -1-1-1—1—1—1 1 1 Static level > • -1-1-1-1—i—l i l Test on March 11,1974; observed by S. Puri for Indian Health Service. Pumping rate 12 gal/min. -1 1 1 • • • • • • < > • • - _i_i i i_l_i i i • • • _i i i_1_1_1 1 1 • • • • • _i i_1_ 260 75 280 - 80 - 85 300 90 5 10 20 50 100 200 TIME SINCE PUMPING STARTED, IN MINUTES 500 Figure 29.—Water levels during drawdown test of Irene Wells well 8S/11 E-33ddd. 120 i i- 1 - 1 —i—i—nr Static level * • »- • • • -1-1-1— • Test on August 21, 1974; • observed by S. Puri for • Indian Health Service. • Pumping rate 2 gal/min. • • - • • • - • - • _1_1_1_i i i i i _l_l_i_l_i i i i _1_1_l_ 160 '-40 200 - 50 - 60 240 70 5 10 20 50 100 200 TIME SINCE PUMPING STARTED, IN MINUTES 500 Figure 30.—Water levels during drawdown test of Schoolie Flat 380-ft test well 8S/12E-3cac. 40 DEPTH TO WATER, IN METRES BELOW LAND SURFACE DEPTH TO WATER, IN METRES BELOW LAND SURFACE 40 ID o < u. QC D if) Q 80 CD t— UJ ID LL GC ID 120 O I- I t- 0- ID Q 160 "i—rr-r Static level Test on August 19, 1974; Observed by S. Puri for Indian Health Service J_I_I_I_L 1-1-1—i—i—r i i 3 gal/min J_I_I I I i-1-r 2 < 5 gal/min. 5gal/min. 1 5 LU o < LL GC D 20 00 O r~ 25 q _i UJ CD if) UJ 30 GC I— ID 35 --40 o Q. UJ 45 Q 2 5 10 20 50 100 200 TIME SINCE PUMPING STARTED, IN MINUTES Figure 31 .—Water levels during drawdown test of Schoolie Flat 1 50-ft test well 8S/12E-3cab. 500 The Albert Comedown well (7S/llE-32bdd), which produces water from the gravel unit that overlies basalt on Mill Creek Flat, was tested by the driller and observed by personnel of the Geological Survey. At a pumping rate of 22 gal/min (1.4 1/s), the water level declined 0.1 ft (0.03 m) within a few minutes, but after several hours had not dropped as much as 0.2 ft (0.06 m) . Because precision of the equipment for discriminating the small changes in water level was not adequate, the permeability of the formation could not be determined; it is obviously much higher, however, than for any other forma¬ tion tested. Results similar to the Comedown well were reported by the driller of the Grant Waheneka well (7S/11E-32bab). The well, also completed in gravel, yielded 25 gal/min (1.6 1/s) with 1 in (25 mm) of drawdown reported after 5 hours of pumping. Quality of Ground Water Ground water from most wells and springs is of good chemical quality, low in dissolved constituents (table 17), and suitable for use by humans, stock, or for irrigation. Only 20 percent of the samples exceeded recom¬ mended limits for iron, and none exceeded recommended sulfate, chloride, or nitrate limits. (See page 83.) Except for hot springs, no samples exceeded fluoride or dissolved-solids limits. Samples from five supplies intended for human consumption exceeded 0.01 mg/1 of arsenic, a limit recommended 41 when other supplies are available, but none exceeded the recommended per¬ missible limit of 0.05 mg/1. Most of the water sampled was soft; only two samples were more than moderately hard. Chemical character of water, as indicated by the proportions of major constituents, can be seen from the chemical diagrams on plate 1. Water of similar sources and histories typically has similarly shaped diagrams, and dissimilar sources produce dissimilar shapes. Ground water from the western part of the reservation and from most wells adjacent to streams in the central part contains more calcium or magnesium than sodium ions. Water from poorly permeable formations, such as the John Day and Clarno Formations, is likely to have a greater proportion of sodium because of increased contact with sodium-bearing minerals, including clays. The chemical diagrams enable visual comparison of ground water with surface water; because of less contact with rocks, surface water generally has fewer dissolved minerals than does ground water. Water from the several hot springs (8S/13E-19bad, -20acd, and -20bdb) in the Kahneeta area contains several times as much dissolved solids as most of the ground water, and it may have a taste that is unpleasant to some persons. The chemical character is distinct, and the hot water has a higher proportion of sodium and chloride than does other water. The water is quite suitable for swimming and the associated recreational uses that have been made of it; because of excessive fluoride and arsenic, hot-springs water would not be suitable as a domestic or community supply intended for general human consumption. Standards for the Usability of Water Domestic Use For drinking water, the Federal Water Pollution Control Administration (1968) recommended standards for public supplies, based on those of the U.S. Public Health Service. Some of the standards for chemical constituents reported for this study include: Constituent Recommended per¬ missible limit of concentration (mg/ 1 ) Constituent Recommended per¬ missible limit of concentration (mg/ 1 ) Iron (Fe) 0.3 Nitrate (NO 3 ) + 44 Sulfate (SO 4 ) 250 nitrite (NO 2 ), Chloride (Cl) 250 expressed as Fluoride (F) 1/1.3 nitrate Arsenic (As) .05 Dissolved solids 500 1/ Value based on average maximum daily air temperature in the vicinity of Warn Springs. Temperature is an indication of the probable consumption of water by individuals. 42 The above are recommended limits for public supplies; concentrations ex¬ ceeding these values may be acceptable to many users and are used in many places Where more acceptable supplies are not available. Excessive iron causes staining of plumbing fixtures and laundry and can give a peculiar taste to the water. Chloride in excess of 500 mg/1 and dissolved solids in excess of 1,000 mg/1 give a salty or mineral taste to the water. Sulfate causes permanent hardness of water and in excessive concen¬ trations can have a laxative effect on persons not accustomed to the water. Fluoride is beneficial up to the recommended limit because it retards dental decay, but in concentrations of more than several milligrams per litre can eventually cause darkening or mottling of children's teeth. Large amounts of nitrate can cause methemoglobinemia (blue-baby effect) in infants. Excessive hardness is undesirable but seldom is cause for rejection of a water supply. Commercial softeners can be used for most supplies. The U.S. Geological Survey uses the following rating for hardness: Hardness range (as CaC 03 ) (mg/1) Rating 0-60 Soft 61-120 Moderately hard 121-180 Hard More than 180 Very hard Excessive arsenic, ingested over a prolonged period, can result in chronic poisoning. Diagnosis is difficult because many of the symptoms are often attributable to other causes. Coliform bacteria are organisms that usually occur in sewage and in pol¬ luted waters; they may be detected after subjecting a sample of the water to a process that will allow growth of colonies of the bacteria. Common sources of coliform are soil, vegetation, and animal or human feces. A large concen¬ tration of coliform does not necessarily indicate a pollution problem, but the water may be considered to have disease-producing potential. Fecal coli¬ form, whose source is the feces of warmblooded animals, is a variety con¬ sidered to be a more positive indication of disease-producing potential. Standards considered by the Federal Water Pollution Control Administration (1968) for public water supplies include a "desirable" limit, prior to treat¬ ment, of less than 100 colonies/100 ml (millilitres) for total coliform, less than 20 colonies/100 ml for fecal coliform; and a "permissible" limit of as much as 10,000 colonies/100 ml for total coliform and as much as 2,000 colonies/100 ml for fecal coliform. After the water is treated for drinking, the coliform colonies should not exceed 4 colonies/100 ml. For contact water sports, the Oregon Department of Environmental Quality (oral commun., August 9, 1973) has established a conditional upper limit of 1,000 colonies/100 ml for total coliform. 43 Excessive sediment in water is objectionable primarily because of its physical appearance; most individuals would rather not drink the water. Excessive sediment clogs pipes and water tanks. There are no generally established limits for sediment concentration, but usually the higher the concentration the more objectionable it is. Removal of sediment in water can be expensive if concentration is high and continued. Turbidity is a general measure of the optical properties of the water. High turbidity values usually reflect high sediment concentrations, but not always. It is possible to have a very low sediment concentration with high turbidity if the suspended matter is very fine or highly reflective. The desirable limit for drinking water set by the Public Health Service (1962) is 5 NTU (Nephelometric turbidity units). Transparency is related to turbidity and is the depth to which an object (usually a black and white Secchi disk) can be seen below the surface of the water. Use by Livestock or Fish Ideally, the same standards would apply for water consumed by livestock as for water consumed by humans; however, animals are more tolerant of saline water than are humans--as much as about 3,000 mg/1 dissolved solids for poultry and as much as 10,000 mg/1 for cattle. If fish are living in a water supply, it is probably suitable for livestock consumption. Dissolved oxygen (DO) is essential for maintaining fish and other aquatic life. The solubility of oxygen varies inversely with temperature and altitude. The availability of oxygen is controlled by the degree of mixing of the water, pollution, and other factors. For trout and salmon, the optimum concentration is 6 or more mg/1. Figure 32 shows livability zones for rainbow trout that depend on dissolved oxygen and temperature; the zones range from the most desirable (I) to lethal (IV). Irrigation Use General salinity, as shown by dissolved solids or by electrical con¬ ductivity, may control plant growth; dissolved solids exceeding 1,000-2,000 mg/1 may have an adverse effect on crops. The SAR (sodium-adsorption-ratio) indicates the effect that a water will have on soil-drainage characteristics. Water with a high SAR value eventually causes clogging of most soils. An SAR of about four is the limit for crops that are sensitive to the effect of soil clogging. Boron is necessary up to about 0.5 mg/1, but in higher concentrations it has a toxic effect on plants; yellowing of leaves is one symptom. Some plants are more sensitive than others; among the more sensitive are citrus, peaches, apples, pears, and walnuts. Water that contains more than 4 mg/1 of boron may be unsuitable even for tolerant crops. 44 Figure 32.—Livability zones for rainbow trout based on combinations of dissolved oxygen and temperature. (Adapted from Smith and Bella, 1973, p. 129.) CONCLUSIONS Flows of the three major streams in or bounding the reservation--the Warm Springs, Metolius, and Deshutes Rivers--are large and have relatively constant high base flows. Flows of the smaller streams are more variable, and some streams can be expected to go dry. Chemical and biological quality of the streams is generally good, as is the quality of reservoirs and high lakes. Availability of ground water to drilled wells is variable, ranging from less than % gal/min (0.03 1/s) to about 30 gal/min (2 1/s). Except in the Cascade Range, most springs yield only a few gallons per minute or less. Thus, ground water is available in quantities adequate only for stock, domestic, and very small community supplies; it is generally inadequate for irrigation or for industrial or municipal supplies. Chemical quality of ground water is generally good, although dissolved constituents in water from some wells approach recommended limits for drinking water. A 5 GLOSSARY OF SELECTED TERMS Aquifer .--A formation, group of formations, or part of a formation that con¬ tains sufficient saturated permeable material to yield significant quan¬ tities of water to wells or springs. Base flow (base runoff).--The runoff component of a stream that is composed primarily of ground-water inflow. A stream at its seasonal minimum usually contains only base flow. Correlation .--The relation between one variable and one or more related variables„ Discharge (outflow).--A measure of the total water that passes a given point or location, reported either as a volume (acre-feet or cubic hectometres) or as a rate (cubic feet per second, cubic metres per second, or acre-feet per year). Drawdown .--In a well, the extent of lowering of the water level during pumping. The difference, in feet or metres, between the static water level and the pumping level. Dependable low flow .--As used in this report, the lowest average rate of dis¬ charge during a 7-day period (excluding short periods of winter ice effect) that may be expected on the average of once in 50 years. Depend¬ able low flows for long-term stations were determined by using a log- • Pearson Type III frequency analysis. Mean annual . .--The arithmetic average value (of streamflow or other quantity) that is obtained from all yearly values during a specific period. It differs from the Annual mean. . which is the average value for one particular year. Similar usage also applies to other periods, such as months or days. Permeability .--A general term that denotes the relative ease with which a porous medium, such as a geologic formation, can transmit water or other liquid. Recurrence interval .--The average interval of time between the occurrence of events of a specified magnitude. A flood with a magnitude that has a recurrence interval of 25 years has a 4 percent chance of occurring in any given year. The actual spacing of the events is not necessarily regular; two floods of 25-year frequency can occur in consecutive years or at intervals much longer than 25 years. Sediment yield .--The total load of fragmental material transported by or sus¬ pended in water and that passes a given location. The yield is usually reported as tons or as tons (or cubic feet) per square mile of drainage area. 46 Specific conductance .--The ability of water or other substance to conduct an electric current. Conductance of water increases with increasing con¬ centration of dissolved-mineral matter; it is therefore an approximate index to the concentration of dissolved solids. Specific conductance may be measured with simple instruments either in the field or in a laboratory. Static level .--The level at which water stands in a well that is not affected by recent pumping. The level is usually reported in feet or metres below land surface. Streamflow .--All the discharge that occurs in a natural channel. (See Discharge .) Runoff is that part of the streamflow that is unaffected by artificial diversions, storage, or other manmade changes. Transparency .--The depth to which an object (usually a black and white Secchi disk) can be seen below the surface of the water. It indicates the relative clarity of the water. Transpiration .--The process by which water escapes as vapor from a living plant, principally from the leaves, and enters the atmosphere. Water table .--The upper surface of a zone of saturation of an unconfined water body. It is defined by the levels at which water stands in wells that penetrate the water body just far enough to hold standing water. In wells that penetrate to greater depths, the water level will stand above or below the water table if an upward or downward component of ground-water flow exists. Water year .--The 12-month period, October 1 through September 30. It is designated by the calendar year in which it ends. 47 SELECTED REFERENCES Columbia-North Pacific Technical Staff, 1970, Columbia-North Pacific region comprehensive framework study. Appendix V, Water resources: Pacific Northwest River Basins Comm, rept., v. 2, p. 545-629. Confederated Tribes of the Warm Springs Reservation of Oregon, 1967, Water resources inventory and water management plan for the Warm Springs Indian Reservation: Warm Springs, Oreg., 48 p. _1969, Comprehensive plan - Warm Springs Reservation: Warm Springs, Oreg., 70 p. Federal Water Pollution Control Administration, 1968, Water quality criteria: Federal Water Pollution Control Adm., 234 p. Goldblatt, E. L., Van Denburgh, A. S., and Marsland, R. A., 1963, The unusual and widespread occurrence of arsenic in well waters of Lane County, Oregon: Lane County Dept. Health, Eugene, Oreg., 24 p. Hem, J. D., 1970, Study and interpretation of the chemical characteristics of natural water [2d ed.]: U.S. Geol. Survey Water-Supply Paper 1473, 363 p. Hodge, E. T., 1940, Geology of the Madras quadrangle: Oregon State Coll. Mon. 1, Studies in Geology. McHugh, R. A., 1972, An interim study of some physical, chemical and bio¬ logical properties of selected Oregon lakes: Oregon State Dept. Environmental Quality, 109 p. Mullarkey, W. G., 1967, Observations on the limnology of Round Butte Reser¬ voir, Oregon: Oregon Fish Comm. Research Briefs 13, p. 60-86. Newcomb, R. C., and Hogenson, G. M., 1956, Availability of ground water in the Schoolie Flat area, Wasco County, Oregon: U.S. Geol. Survey open-file rept., 13 p. Oregon State Water Resources Board, 1961, Deschutes River basin: Salem, Oreg., 188 p. Peck, D. L., 1964, Geologic reconnaissance of the Antelope-Ashwood area, north-central Oregon: U.S. Geol. Survey Bull. 1161-D, 26 p. Phillips, K. N., Newcomb, R. C., Swenson, H. A., and Laird, L. B., 1965, Water for Oregon: U.S. Geol. Survey Water-Supply Paper 1649, 150 p. Riggs, H. C., 1968, Frequency curves: U.S. Geol. Survey Tech. Water-Resources Inv., book 4, chap. A2, 15 p. _1969, Mean streamflow from discharge measurements: Bull. Internat. Assoc. Sci. Hydrology, XIV, 4, p. 95-110. 48 Riggs, H. C., 1972, Low-flow investigations: U.S. Geol. Survey Tech. Water- Resources Inv., book 4, chap. Bl, 18 p. Smith, S. A., and Bella, D. A., 1973, Dissolved oxygen and temperature in a stratified lake: Jour. Water Pollution Control Federation, v. 45, no. 1, p. 119-133. Stearns, H. T., 1931, Geology and water resources of the middle Deschutes River basin, Oregon: U.S. Geol. Survey Water-Supply Paper 637-D, p. 125-220. U.S. Bureau of Indian Affairs, 1969, Irrigation reconnaissance report - Warm Springs irrigation project: Bur. Indian Affairs, Portland, Oreg., 46 p. U.S. Geological Survey, 1958, Compilation of records of surface waters of the United States through September 1950, pt. 14, Pacific slope basins in Oregon and lower Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1318, 550 p. _1963, Compilation of records of surface waters of the United States, October 1950 to September 1960, pt. 14, Pacific slope basins in Oregon and lower Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1738, 327 p. _1971, Compilation of records of surface waters of the United States, October 1961 to September 1965, pt. 14, Pacific slope basins in Oregon and lower Columbia River basin: U.S. Geol. Survey Water-Supply Paper 1935, 957 p. U.S. Public Health Service, 1962a, Drinking water standards, 1962: U.S. Public Health Service Pub. 956, 61 p. _1962b, Manual of individual water supply systems: U.S. Public Health Service Pub. 24, 121 p. Waters, A. C., 1968a, Reconnaissance geologic map of the Madras quadrangle, Jefferson and Wasco Counties, Oregon: U.S. Geol. Survey Misc. Geol. Inv. Map 1-555. _1968b, Reconnaissance geologic map of the Dufur quadrangle, Hood River, Sherman, and Wasco Counties, Oregon: U.S. Geol. Survey Misc. Geol. Inv. Map 1-556. Wells, F. G., and Peck, D. L., 1961, Geologic map of Oregon west of the 121st meridian: U.S. Geol. Survey Misc. Geol. Inv. Map 1-325. Williams, Howel, 1957, A geologic map of the Bend quadrangle, Oregon, and a reconnaissance geologic map of the central portion of the High Cascade mountains: Oregon Dept. Geology and Mineral Industries Map. Wolfe, J. A., 1972, An interpretation of Alaskan Tertiary floras in Alan Alan Graham, ed., Floristics and paleofloristics of Asia and eastern North America: New York, Elsevier Publishing Co., p. 201-233. Yoder, E. E., 1960, Water resources, in Warm Springs research project final report, v. IV: Oregon State Coll., Corvallis, Oreg., 390 p. 50 BASIC-DATA RECORDS 51 Table 4.-- Dally discharge of the Warm Springs River. 1973-74 14097100 WARM SPRINGS RIVER NEAR KAHNEETA HOT SPRINGS, OREG. LOCATION.— Lat 44°51'24", long 121°08'55", in SESsSWh; sec. 23, T.8 S., R.13 E., Wasco County, Warm Springs Indian Reservation, on right bank at mile 4.6 (7.4 km). DRAINAGE AREA.—526 mi 2 (1,362 km 2 ). PERIOD OF RECORD.—October 1972 to September 1974. EXTREMES.—Water year 1973: Maximum discharge, 1,560 ft 3 /s (44.2 m 3 /s) (6.43 m 3 /s) Aug. 15, 16, Sept. 6. Water year 1974: Maximum discharge, 6,350 ft 3 /s (180 m 3 /s) Jan. (6.63 m 3 /s) Oct. 1-4. Period of record: Maximum discharge, 6,350 ft 3 /s (180 m 3 /s) Jan. 227 ft 3 /e (6.43 m 3 /s) Aug. 15, 16, Sept. 6, 1973. Dec. 21, gage height, 3.81 ft (1.161 m); minimum, 227 ft 3 /s 16, gage height, 8.68 ft (2.646 m); minimum, 234 ft 3 /s 16, 1974, gage height, 8.68 ft (2.646 m); minimum. REMARKS.—Records excellent. No regulation. Diversions above station. DISCHARGE. IN CUBIC FEET PtH SECOND, WATER YEAR OCTOBER 1972 TO SEPTEMBER 19/3 MtAN VALUES DAY OCT NOV DEC JAN EEb MAH APR MAY JUN JIJL AUG SEP 1 319 317 31 7 416 370 377 333 330 276 253 234 232 2 319 331 317 414 373 377 326 327 277 252 232 231 3 317 336 318 398 368 366 325 325 278 252 232 232 4 315 348 306 354 369 366 320 327 276 2 50 233 231 S 314 352 302 37 7 372 363 324 33u 279 249 234 231 6 317 338 300 359 364 361 329 325 273 248 237 230 7 317 332 295 340 354 359 320 325 271 250 237 236 B 317 326 290 340 350 358 320 331 268 249 234 238 9 317 324 290 335 348 357 321 335 265 246 234 235 10 318 327 285 330 353 372 321 331 266 2 44 235 234 11 324 331 285 330 347 394 324 327 264 242 234 232 12 325 326 285 344 350 378 331 319 268 241 232 231 13 326 326 280 672 349 375 369 314 268 241 233 231 14 323 326 280 958 343 370 343 311 265 241 231 231 IS 322 323 280 774 340 363 343 312 265 240 230 231 16 320 323 280 753 345 362 344 314 266 238 230 231 17 319 324 280 683 361 366 362 311 283 237 231 232 18 317 321 450 604 353 361 359 308 285 237 231 239 19 320 319 830 578 341 360 356 305 276 243 231 239 20 319 317 907 524 341 357 352 300 271 247 232 246 21 318 315 1220 501 337 354 343 301 267 249 231 245 22 314 314 1360 450 335 348 337 299 266 241 231 2S2 23 313 314 991 456 335 334 338 297 265 238 231 259 24 312 314 836 453 336 336 338 301 265 238 234 258 25 313 315 753 439 345 340 334 306 265 237 240 264 26 316 335 632 389 363 340 334 306 265 237 237 249 27 317 332 577 391 367 340 340 300 261 237 234 241 28 321 324 548 399 367 338 335 297 25 7 244 233 238 29 319 321 492 378 — 329 335 291 254 238 234 238 30 316 319 463 388 — 334 333 287 253 237 234 236 31 314 - — 441 385 — 338 — 283 ——— 234 233 —— — TOTAL 9858 9770 15490 14512 98 76 11073 10089 9675 8058 7530 7229 7153 MEAN 318 326 500 468 353 357 336 312 2b9 243 233 238 MAX 326 352 1360 958 373 394 369 335 285 253 240 264 MIN 312 314 280 330 335 329 320 283 253 234 230 230 CFSM .60 .62 .95 .89 .67 .68 • 64 .59 .51 • 46 .44 .45 IN. .70 .69 1.10 1.03 . 70 .78 .71 .68 .57 .53 .51 .51 AC-ET 19550 19380 30720 28780 19590 21960 20010 19190 15980 14940 14340 14190 WTR YR 1973 TOTAL 120313 MEAN 330 MAX 1360 MIN 230 CFSM .63 IN 8.51 AC -FT 238600 52 Table 4.-- Dally discharge of the Warm Springs River, 1973-74 --Contlnued 14097100 WARM SPRINGS RIVER NEAR KAHNEETA HOT SPRINGS, OREG.--Continued DISCHARGE. IN CUBIC FEET PER SECOND MEAN . rfATEK VALUES YEAH OCTOBER 1973 TO SEPTEMBER 1974 DAY OCT NOV DEC JAN FEB MAH APR MAY JUN JUL AUG 1 236 355 605 719 1120 804 1150 798 774 513 336 2 237 305 459 599 962 769 1110 813 780 509 333 3 237 280 401 570 892 662 981 797 831 491 332 4 237 281 377 530 961 635 909 788 903 463 331 S 238 290 360 500 937 6b9 895 798 1120 459 327 6 240 281 360 470 823 716 859 834 1110 458 324 7 246 282 665 450 777 650 809 916 1030 44 7 323 8 243 286 732 430 746 618 777 967 951 432 324 9 244 351 607 44 0 717 625 773 1020 878 438 325 10 257 455 538 470 68 7 606 742 1020 835 433 325 11 255 619 495 506 671 625 713 973 823 427 324 12 254 682 467 570 655 669 764 984 839 416 322 13 251 564 497 609 631 644 733 946 866 406 324 14 249 432 464 1640 618 642 709 884 890 397 327 lb 247 423 560 4730 605 809 700 870 w06 38 7 327 16 241 489 665 5670 651 953 696 819 900 386 324 17 238 511 1130 4360 629 802 698 778 875 388 323 18 238 423 942 3890 615 759 708 739 855 382 322 19 239 373 772 3570 1380 753 717 703 832 382 324 20 255 352 781 2580 1010 720 714 672 806 370 326 21 263 355 1390 2020 923 702 716 655 772 364 324 22 262 343 1090 1720 834 690 738 648 725 358 322 23 259 329 963 1530 780 675 822 654 695 355 322 24 255 335 836 1330 727 667 851 669 661 351 320 2b 254 347 1130 1240 705 672 890 698 628 348 318 26 249 350 980 1150 690 68 7 861 766 608 346 318 27 246 333 931 1060 68<. 695 803 854 584 344 315 28 247 386 1610 1020 775 761 772 877 556 344 315 29 256 492 1240 931 — 893 761 850 535 342 315 30 249 589 985 884 -— 1310 767 821 521 34 7 310 31 258 — 900 926 — 1210 792 —- 340 308 TOTAL 768U 11693 23932 4 7114 22205 23092 24138 25403 24089 12423 10010 MEAN 248 396 772 1520 793 745 805 819 803 401 323 MAX 263 682 1610 5670 1380 1310 1150 1020 1120 513 336 MIN 236 280 360 430 605 606 696 648 521 340 308 Cf SM .47 .75 1.47 2.89 1.51 1 .42 1.53 1.56 1.53 .76 .61 IN. .54 .84 1.69 3.33 1.57 1.63 1.71 1.80 1.70 .88 .71 AC-FT 15230 23590 47470 93450 44040 45b00 47880 50390 47780 24640 19850 CAL YR 1973 TOTAL 128700 MEAN 353 MAX 1610 MIN 230 CFSM .67 IN 9. 10 AC -FT 255300 WTR YR 1974 TOTAL 241022 MEAN 660 MAX 5670 MIN 236 CF SM 1.25 IN 17. 05 AC -7T 478100 SEP 309 309 309 300 303 30 2 302 302 304 306 305 304 303 302 302 302 300 299 299 299 298 299 299 299 298 2^6 296 299 299 299 9043 301 309 296 .57 .64 17940 53 Table 5.-- Dally discharge of Shltike Creek, 1973-74 14093000 SHITIKE CREEK NEAR WARM SPRINGS, OREG. LOCATION.—Lat 44°45'41", long 121°13'57", In NVAiNVAs sec.30, T.9 S., R.13 E., Jefferson County, Warm Springs Indian Reservation, on left bank 1.9 mi (3.1 km) east of Warm Springs and at mile 0.3 (0.5 km). DRAINAGE AREA. —105 mi 2 (272 km 2 ). PERIOD OF RECORD.—October 1972 to September 1974. GAGE.—Nonrecording gage. Altitude of gage is 1,380 ft (421 m), from topographic map. EXTREMES.—Water year 1973: Maximum daily discharge, 690 ft 3 /s (19.5 m 3 /s) Dec. 21; minimum daily, 20 ft 3 /s (0.57 m 3 /s) Dec. 8-15. Water year 1974: Maximum dally discharge, 2,300 ft 3 /s (65.1 m 3 /s) Jan. 15; minimum dally, 31 ft 3 /s (0.88 m 3 /s) Oct. 18. Period of record: Maximum daily discharge, 2,300 ft 3 /s (65.1 m 3 /s) Jan. 15, 1974; minimum daily, 20 ft 3 /s (0.57 m 3 /s) Dec. 8-15, 1972. REMARKS.—Records fair. No regulation. Some water is diverted for mill pond at point 0.3 mi (0.5 km) above station. DISCHARGE. IN CUBIC FEET RtK SECONU, WATER YEAR OCTOBtR 1972 TO SEPTEMBER 1973 MEAN VALUES DAY OCT NOV DEC JAN FEB MAR APR MAY JUN JUL AUG SEP 1 66 57 57 100 75 71 60 67 75 64 38 35 d 64 90 57 91 75 71 57 67 75 64 35 38 i 64 76 59 86 71 67 57 67 75 57 38 35 4 64 102 37 78 71 67 57 75 71 60 41 33 5 61 85 37 82 71 67 57 71 71 60 41 33 6 59 76 37 71 67 67 57 71 78 57 41 33 7 59 71 30 60 67 67 60 71 88 53 38 35 8 59 66 20 44 67 64 60 71 91 50 38 41 V 69 61 20 67 64 64 60 71 86 47 38 35 10 61 68 20 75 67 67 60 71 82 50 38 35 11 68 66 20 86 64 71* 60 67 60 50 38 33 12 64 64 20 158 64 67 64 71 67 47 38 33 13 66 61 20 500 64 67 64 78 75 44 38 33 14 66 61 20 450 64 64 64 86 71 47 35 33 15 66 57 20 248 60 64 71 105 75 47 35 33 16 59 61 54 216 64 64 75 152 75 44 38 33 1 7 61 61 126 182 60 64 78 122 78 44 38 33 18 57 59 215 158 64 64 78 116 60 44 35 33 19 57 57 495 140 64 60 71 128 64 47 35 35 20 54 57 470 128 64 60 71 105 67 50 35 38 21 57 52 690 122 60 64 71 78 71 47 35 41 22 57 57 625 no 57 57 71 78 71 47 35 53 23 52 52 376 105 60 62 67 82 75 44 35 60 24 52 52 280 100 60 64 67 128 75 44 41 78 25 52 61 224 96 60 64 67 116 75 41 41 ins 26 57 150 170 78 62 64 67 100 82 41 44 57 27 52 80 164 86 64 60 75 75 91 41 44 52 28 52 71 140 82 67 60 78 71 71 41 41 44 29 57 66 128 82 — 64 78 71 64 41 38 44 30 57 61 116 82 — 67 71 71 64 41 35 41 31 52 110 78 — 64 — 71 — 41 35 TOTAL 1831 2058 4857 4041 1817 2007 1993 2673 2223 1495 1175 1265 Mt AN 59.1 68.6 157 130 64.9 64 . 7 66.4 86.2 74.1 48.2 37.9 42.2 MAX 68 150 690 500 75 71 78 152 91 64 44 105 MIN 52 52 20 44 57 57 57 67 60 41 35 33 AC-FT 3630 4080 9630 8020 3600 3980 3950 5300 4410 2970 2330 2510 WTR YR 1973 TOTAL 27435 MEAN 75.2 MAX 690 MIN 20 AC-FT 54420 54 Table 5.-- Dally discharge of Shltike Creek, 1973-74 --Contlnued 14093000 SHITIKE CREEK NEAR WARM SPRINGS, OREG.--Continued 01SCHANGE * IN cubic FEET PER SECONU. WATER TEAR OCTOBER 1V73 TO SEPTtMbER 1974 MEAN VALUES DAY OCT NUV OEC JAN FEB MAR APR MAY JUN JUL AUG SFP 1 41 187 130 136 182 128 235 1 72 323 25 7 124 78 2 41 94 98 136 190 124 214 168 356 189 124 81 3 37 81 89 123 180 121 189 168 390 176 129 78 4 37 81 85 98 160 117 180 164 390 185 129 77 5 37 69 81 95 14V 117 176 168 546 194 126 77 6 37 57 81 85 138 117 172 185 390 214 116 80 7 37 53 203 80 138 114 164 263 323 176 109 77 8 37 61 255 80 134 108 156 2 68 280 168 109 77 9 41 61 187 80 13*. 111 153 280 246 164 113 77 10 41 61 143 85 136 111 145 250 235 156 113 76 11 37 98 136 95 126 111 145 230 268 149 116 76 12 37 123 123 100 126 114 142 230 292 149 116 76 13 37 130 117 130 119 108 142 230 349 145 106 74 14 37 136 107 500 119 117 134 225 356 156 103 74 IS 35 123 107 2300 122 114 128 219 427 147 100 74 16 35 165 123 2100 121 124 128 214 390 142 100 72 17 33 136 165 1200 124 128 134 209 336 142 100 70 IB 31 102 284 1100 124 138 134 192 342 160 102 68 19 33 107 220 1000 194 138 134 185 323 156 94 68 20 35 98 345 760 153 134 139 185 329 168 94 67 21 53 94 460 610 145 126 142 185 310 156 91 67 22 53 85 356 450 140 131 142 185 298 147 91 67 23 53 81 314 350 133 131 145 189 310 142 94 67 24 41 81 212 300 129 131 145 199 246 134 94 67 25 41 77 378 255 129 131 156 356 251 131 91 65 26 53 69 274 230 129 134 164 427 219 131 88 65 27 57 65 293 210 133 134 160 427 185 138 88 65 28 64 94 284 190 138 164 145 349 194 142 91 65 29 67 102 255 180 — 206 145 298 313 142 85 63 30 50 117 229 175 — 286 149 280 235 147 83 64 31 71 -— 187 174 — 2*6 - - - 263 — 131 81 - — TOTAL 1339 2886 6321 13407 3945 4216 4637 7363 9452 4934 3200 2152 MEAN 43.2 96.3 204 432 141 136 155 238 315 159 103 71.7 MAX 71 187 460 2300 194 286 235 427 546 257 129 81 MIN 31 53 81 80 119 108 128 164 185 131 81 63 AC-FT 2660 5730 12540 26590 7820 b360 9200 14600 18750 9790 6350 4270 CAL YR 1973 TOTAL 29237 MEAN 80.1 MAX 500 MIN 31 AC-FT 57990 WTH YR 1974 TOTAL 63854 MEAN 175 MAX 2300 MIN 31 AC-f T 126700 55 Table 6.r- Daily discharge of the White River. 1973-74 14101500 WHITE RIVER BELOW TYGH VALLEY, OREG. LOCATION.'—Lat 45°14'30", long 121°05'38", in NE*tNE*s sec.7, T.4 S., R.14 E., Wasco County, on left bank 200 ft (61 m) downstream from former Pacific Power & Light Co. powerplant at White River Falls, 3.9 mi (6.3 km) east of town of Tygh Valley, and at mile 2.0 (3.2 km). DRAINAGE AREA.—417 mi 2 (1,080 km 2 ). PERIOD OF RECORD.—October 1917 to September 1974. GAGE.—Water-stage recorder. Datum of gage is 870.15 ft (265.222 m) above mean sea level (levels by Pacific Power & Light Co.). Prior to July 28, 1931, at site 750 ft (229 m) downstream at different datum. July 28, 1931, to Sept. 30, 1954, at site 700 ft (213 m) downstream at different datums. AVERAGE DISCHARGE.—57 years (1917-74), 431 ft 3 /s (12.2 m 3 /s), 312,300 acre-ft/yr (385 hm 3 /yr). EXTREMES.—Water year 1973: Maximum discharge, 2,830 ft 3 /s (80.1 m 3 /s) Dec. 21, gage height, 5.77 ft (1.759 m); minimum, 83 ftVs (2.35 m 3 /e) Sept. 4, 17. Water year 1974: Maximum discharge, 7,910 ft 3 /s (224 m 3 /s) Jan. 16, gage height, 9.74 ft (2.969 m); minimum, 94 ft 3 /s (2.66 m 3 /8) Oct. 4. Period of record: Maximum discharge, 13,300 ft 3 /s (377 m 3 /s) Jan. 6, 1923, gage height, about 13.3 ft (4.05 m), site and datum then in use, from rating curve extended above 5,000 ft 3 /s (142 m 3 /s); minimum, 7.5 ft 3 /s (0.21 m 3 /s) Aug. 31, 1961, minimum daily, 71 ft 3 /s (2.01 m 3 /s) Aug. 31, 1941. REMARKS.—Records good. No regulation. Diversions above station for irrigation. DISCHARGE. IN CUBIC FEET Ft* SECOND, WATER YEAR OCTOBER 1972 TO SEPTEMBER 1973 MEAN VALUES DAY OCT NOV DEC JAN FEB MAR APR MAY JUN JUL AUG SEP 1 150 14S 187 420 312 293 201 234 167 128 107 94 2 14b 175 188 416 300 292 195 238 170 123 107 90 3 141 181 186 388 297 268 187 238 165 121 113 87 4 13b 200 169 332 293 285 190 245 160 121 109 85 b 133 203 142 352 286 281 205 241 154 123 109 90 6 130 177 131 308 279 2 7b 214 231 149 121 115 88 7 130 1 b7 130 286 265 272 205 231 147 123 105 92 8 130 162 130 251 258 2b9 197 231 147 121 99 94 9 130 157 129 258 255 271 198 231 144 119 97 90 10 131 163 129 308 258 312 199 225 139 119 97 92 11 141 163 130 324 251 325 211 228 137 119 97 94 12 140 157 132 425 248 304 219 218 133 115 97 88 13 142 154 134 1 140 248 303 226 221 133 115 101 87 14 145 152 138 1240 248 291 228 234 130 115 101 87 15 142 149 143 936 245 262 222 241 137 117 99 67 lb 140 149 154 901 251 283 241 245 135 121 97 85 17 140 149 253 810 262 263 265 231 149 123 99 83 18 138 148 583 708 255 273 248 225 152 115 96 85 19 137 149 763 642 245 269 245 215 135 117 94 87 20 137 145 762 560 238 262 248 205 126 121 94 96 21 136 142 2180 520 234 255 238 199 121 121 90 9b 22 137 141 1460 470 231 24 7 248 196 123 117 92 107 23 135 139 1130 450 231 241 269 196 128 117 90 115 24 132 151 1060 430 234 240 258 209 126 111 103 130 25 132 157 936 416 246 238 238 218 130 111 107 147 2b 141 428 756 368 269 239 238 209 147 113 94 123 27 146 273 714 368 276 235 255 199 144 117 90 109 28 14b 226 642 356 279 229 245 199 135 117 88 1 1 1 29 145 209 550 340 — 209 241 190 130 113 92 111 30 143 194 505 340 — 203 241 185 126 109 97 115 31 142 465 332 — 205 — 176 — 105 97 TOTAL 4294 5305 15111 15395 729b b255 6815 6784 4223 3648 3073 2965 MEAN 139 177 487 497 261 266 227 219 1 4 1 118 99.1 98.8 MAX 150 428 2180 1240 312 325 269 245 170 128 115 167 MIN 130 139 129 251 231 203 187 176 121 105 86 83 AC-FT 8520 10520 29970 30540 14470 16370 13520 13460 8380 7240 6100 5880 CAL YR 1972 TOTAL 215252 MEAN 588 MAX 4810 MIN 129 AC-f T 427000 WTR YR 1973 TOTAL 83164 MEAN 228 MAX 2180 MIN 83 AC-1 T 165000 56 Table 6.-- Dally discharge of the White River. 1973-74 --Contlnued 14101500 WHITE RIVER BELOW TYGH VALLEY, OREG.--Continued DISCHARGE, IN CUBIC FEET PEW SECOND, WATER YEAH OCTOBER 1973 TO SEPTEMBER 1974 MEAN VALUES DAY OCT NOV DEC JAN FEB MAR APR MAY JUN JUL AUG SEP 1 109 339 473 841 1190 635 1190 1110 977 708 238 152 2 101 193 407 738 1060 606 1140 1050 1110 635 231 152 3 99 157 375 650 977 545 1030 1020 1280 578 218 150 4 99 152 351 540 1040 529 956 1030 1480 561 215 152 s 97 157 328 500 956 589 915 1050 1820 556 205 150 6 99 160 343 480 861 64 1 895 1230 1580 529 190 147 7 109 157 782 470 802 589 841 1390 1390 488 182 145 B 103 162 950 460 751 556 815 1510 1220 463 179 142 9 103 305 732 450 714 534 b21 1510 1 130 463 176 142 10 103 49b 623 470 677 519 789 1400 1130 425 176 147 11 101 671 556 500 647 545 815 1310 1210 412 173 145 12 103 802 503 540 623 578 929 1320 1390 391 176 142 13 101 647 508 623 595 545 847 1170 1530 363 17b 140 14 99 486 458 1540 572 578 815 1070 1600 359 171 137 15 99 425 572 5930 561 770 815 984 1620 359 168 137 16 103 653 815 6460 589 802 795 881 1500 347 162 135 17 103 545 1380 4340 567 808 815 795 1500 34 7 162 137 16 103 444 1220 4090 600 782 854 732 1530 343 162 135 19 101 375 1030 3470 936 757 867 683 1480 339 168 135 20 115 347 1050 2590 795 720 854 653 1390 332 173 133 21 117 332 1930 2040 745 689 874 612 1230 328 165 133 22 123 309 1610 1 740 689 671 956 629 1160 324 162 130 23 121 290 1400 1570 635 641 1040 683 1080 316 160 130 24 133 290 1250 1410 595 629 1030 738 950 301 165 126 25 130 287 1760 1350 578 647 1060 901 874 290 162 123 2b 126 276 1410 1280 572 677 1010 1150 795 283 160 126 27 113 269 1390 1 180 550 714 956 1260 714 276 157 128 26 109 371 1480 1160 623 6o2 943 1200 671 272 155 126 29 133 420 1370 1080 — 943 943 1110 647 265 152 140 30 115 444 1160 1030 — 1190 1020 1050 683 258 152 147 31 162 — 1030 1100 — 1220 - — 998 — 248 155 — TOTAL 3452 10965 29246 50622 20500 21451 27630 32229 36671 12159 5446 4 164 MEAN 111 366 943 1633 732 692 921 1040 1222 392 176 139 MAX 162 802 1930 b460 1190 1220 1190 1510 1820 708 238 152 MIN 97 152 328 450 550 5l 9 789 612 647 248 152 123 AC-FT 6650 21750 58010 100400 40660 42550 54800 63930 72740 24120 10800 8260 CAL YH 1973 TOTAL 102117 MEAN 280 MAX 1930 MIN 83 AC-FT , 202500 WTR YR 1974 TOTAL 254535 MEAN 697 MAX 6460 MIN 97 AC-FT 1 504900 57 Table 7.—Gain-loss investigations of the Warm Springs River and Mill Creek In 1973 To study channel gains and losses, discharge measurements of the Warm Springs River and its tributaries and diversions were made from May 31 to June 6 and again from October 2 to 5. Measurements were made along the entire length of Mill Creek, which contributes 30 percent of the total flow at its confluence with the Warm Springs River and has therefore been treated as a subreach of the river. Measurements were made during periods when flows of the streams were reasonably constant. During the first measuring period (May 31- June 6), flows at the gaging station at Kahneeta Hot Springs varied less than 2 percent for any 2 days and only about 3.5 percent for the entire period. During the second measuring period, flows at the gaging station varied by less than 1 percent. No measurable precipitation had fallen within the drainage basin for 5 days prior to the first set of measurements nor for 7 days preceding the second set. In compiling this table, tributary flow was considered to be a contribution, not a gain; diversion was considered to be a de¬ duction, not a loss. Indicated gains or losses may be substantially in error because of inaccuracies in open-channel measurements. Water temperatures have been included in this tabulation because they were helpful in locating major springs. WARM SPRINGS RIVER Stream Discharge, in cubic feet per second Water Date or diversion Location River mile Main stem Tributary(+) diversion(-) Gain or loss in section Total gain temp. °C Warm Springs River Headwater 51.4 — -- ■— -- -- do McQuinn line (reservation boundary) 47.0 -- -- -- -* 5-31-73 Dry Creek Near McQuinn line in sec.36, T.6 S., R.8 E. 45.2 ~ “ +0.25 * “ _ “ Do Warm Springs River do 44.8 2.03 “ “ “ * 2.03 8.5 Do do At old reservation boundary in sec.6, T.7 S., R.9 E. 43.4 2.24 — +0.21 2.24 7.0 6- 4-73 do do 43.4 2.29 -- 2.29 8.5 Do R.B. tribu¬ tary In sec.4, T.7 S., R.9 E. 41.5 +1.40 10.0 Do Warm Springs River 10 ft below confluence with tributary in sec.4, T.7 S., R.9 E. 41.5 5.34 — +1.70 5.34 13.0 Do R.B. tribu¬ tary 0.1 mi upstream from upper bridge in sect.3, T.7 S., R.9 E. 40.5 — +1.50 “ ” Do Warm Springs River At upper bridge on road W240 in sec.3, T.7 S., R.9 E. 40.4 66.7 +59.9 66.7 7.5 Do Bunchgrass Creek Near Warm Springs Meadows in sec.2, T.7 S., R.9 E. 39.7 “ “ +2.02 “ “ ~ “ 11.0 Do Warm Springs River 30 ft below confluence with Bunchgrass Creek in sec.2, T.7 S., R.9 E. 39.7 76.8 “ ~ +8.10 '6.8 10.5 Do Big Springs Near Schoolie Bridge in sec.7, T.7 S., R.10 E. 36.3 “ “ +1.12 “ ~ " ~ 9.5 Do Warm Springs River At Schoolie Bridge in sec.7, T.7 S., R.10 E. 36.3 128 — +50.1 128 13.5 Do S.F. Warm Springs River Near Schoolie Pasture at road B200 crossing in sec.18, T.7 S., R.10 E. 36.1 +1.84 14.5 6- 5-73 Warm Springs River At old gage site (14095500) at HeHe Mill, in sec.18, T.7 S., R.ll E. 29.3 129 -1.0 129 14.0 Do Badger Creek At Highway 26 crossing approximately 1.5 mi from mouth, in sec.20, T.7 S., R. 11 E. 26.4 +14.8 11.1 Do Mill Creek Canal At Highway 26 crossing approximately 2.5 mi from mouth in sec.25, T.8 S. , R.ll E. 21.0 +2.29 13.5 6- 6-73 Mill Creek At Highway 26 crossing approximately 2.9 mi from mouth in sec.21, T.8 S., R.ll E. 20.3 +86.2 12.0 6- 5-73 Warm Springs River 300 ft above confluence with Beaver Creek in sec.18, T.8 S., R.12 E. 18.3 244 ” " +12.0 244 14.5 Do Beaver Creek At mouth in sec.18, T.8 S., R.12 E. 18.3 -- +45.4 -- -- 17.0 6- 6-73 Warm Springs River Near Tohet Springs in sec.35, T.8 S., R.12 E. 14.4 272 — -17.0 272 18.0 6- 4-73 Warm Springs River At fish hatchery in sec.24, T.8 S., R.12 E. 10.3 261 -11.0 261 •* Do do At gage site (14097100) nr Kahneeta Hot Springs in sec.23, T.8 S. , R.13 E. 4.5 278 +17.0 278 MILL CREEK Mill Creek Headwater 24.0 _ _ _ _ _ _ _ m _ _ 6- 6-73 do Outflow of Island Lake near Trout Lake 22.0 15.2 -- +15.2 15.2 15.5 Do do Outflow of Trout Lake, in sec.12, T.9 S., R.8 E. 21.4 12.1 “ “ -3.10 12.1 16.5 Do N.F. Mill Creek Outflow of Blue Lake, 3.0 mi from mouth, in sec.25, T.8 S., R.8 E. 17.9 + .026 14.0 Do Mill Creek At road B244 crossing in sec.27, T.8 S., R.9 E. 15.8 48.9 +36.8 48.9 10.0 Do do 30 ft above diversion structure, in sec.17, T.8 S., R.10 E. 10.0 46.6 ““ -2.30 46.6 12.5 Do Mill Creek lateral 30 ft below diversion structure, in sec.17, T.8 S., R.10 E. 10.9 -7.68 “ “ ““ 12.5 6- 5-73 Mill Creek At road crossing below Potters Pond, in sec.19, T.8 S., R.ll E. 6.2 48.7 +9.80 48.7 11.0 Do Boulder Creek At B100 road crossing, 1.6 ml upstream from mouth, in sec.31, T.8 S., R.ll E. 4.6 Dry Do Mill Creek At Highway 26 crossing, in sec.21, T.8 S., R.ll E. 2.9 86.2 +37.5 86.2 12.0 58 Table 7.— Gain-loss Investigations of the Warm Springs River and Mill Creek in 1973 --Continued WARM SPRINGS RIVER Stream River Discharge, in cubic feet per second Water Date or diversion Location mile Main stem Tributary(+) diversion(-) Gain or loss in section Total gain temp. *C Warm Springs River Headwater. 51.4 — -- — — -- ... do ... McQuinn line (Reservation boundary). 47.0 -- -- -- -- -- 10- 5-73 ... do ... At old reservation boundary in sec.6, T.7 S., R.9 E. 43.4 0.26 “ “ “ “ 0.26 3.0 Do... R.B. Tribu¬ tary In sec.4, T.7 S., R.9 E. 41.5 " - 40.10 “ * “ “ 9.5 Do.. . Warm Springs River 10 ft below confluence with tributary in sec.4, T.7 S., R.9 E. 41.5 .99 +0.63 0.99 5.0 Do.. . R.B. tribu¬ tary 0.1 mi upstream from upper bridge in sec.3, T.7 S., R.9 E. 40.5 ““ +.10 “ “ “ “ “ • Do... Warm Springs River At upper bridge on road W240 in sec.3, T.7 S., R.9 E. 40.4 66.6 “ “ +65.5 66.6 5.0 Do... Bunchgrass Creek Near Warm Springs Meadows in sec.2, T.7 S., R.9 E. 39.7 — +1.30 * “ “ ” 6.5 Do... Warm Springs River 30 ft, below confluence with Bunch- grass Creek in sec.2, T.7 S., R.9 E. 39.7 73.8 +5.90 73.8 6.0 Do... Big Springs Near Schoolle Bridge in sec.7, T.7 S., R.10 E. 36.3 “ “ +1.00 “ “ " “ ” • Do... Warm Springs River At Schoolie Bridge in sec.7, T.7 S. f R. 10 E. 36.3 116 +41.2 116 7.5 Do... S.F. Warm Springs River Near Schoolle Pasture at road B200 crossing in sec.18, T.7 S., R.10 E. 36.1 +. 30 10- 3-73 Warm Springs River At old gage site (14095500) at Hehe Mill, in sec.18, T.7 S., R.ll E. 29.3 118 +2.0 118 7.5 Do... Badger Creek At Highway 26 crossing approx. 1.5 ml from mouth, in sec.20, T.7 S., R.ll E. 26.4 +8.16 Do... Mill Creek Canal At Highway 26 crossing approx. 2.5 ml from mouth in sec.25, T.8 S., R.ll E. 21.0 +.3 10- 2-73 Mill Creek At Highway 26 crossing approx. 2.9 mi from mouth in sec.21, T.8 S., R.ll E. 20.3 +70.4 9.0 10- 3-73 Warm Springs River 300 ft above confluence with Beaver Creek in sec.18, T.8 S., R.12 E. 18.3 195 — ” -2.0 195 18.5 Do... Beaver Creek At mouth in sec.18, T.8 S., R.12 E. 18.3 +35.7 “ “ 10.0 Do... Warm Springs River Near Tohet Springs in sec.35, T.8 S., R.12 E. 14.4 227 -4.0 227 7.0 Do... Warm Springs River At fish hatchery in sec.24, T.8 S., R.12 E. 10.3 240 +13.0 240 7.0 Do... ... do ... At gage site (14097100) nr Kahneeta Hot Springs in sec.23, T.8 S., R.13 E. 4.5 237 -3.0 237 7.0 MILL CREEK 10- 5-73 Mill Creek ... do ... Headwater. Outflow of Trout Lake, in sec.12, T.9 S., R.8 E. 24.0 21.4 4.37 — — 4.37 12.0 Do... N.F. Mill Creek Outflow of Blue Lake, 3.0 mi from mouth, in sec.25, T.8 S., R.8 E. 17.9 0 10- 2-73 Mill Creek At road B244 crossing in sec.27, T.8 S., R.9 E. 15.8 32.8 — — +28.4 32.8 4.5 Do... ... do ... 30 ft above diversion structure, in sec.17, T.8 S., R.10. 10.0 37.2 +4.4 37.2 4.5 Do... Mill Creek lateral 30 ft below diversion structure, in sec.17, T.8 S., R.10 E. 10.9 -4.37 4.5 Do. .. Mill Creek At road crossing below Potters Ponds, in sec.19, T.8 S., R.ll E. 6.2 28.2 “ — -4.6 28.2 8.5 Do... Boulder Creek At B100 road crossing, 1.6 ml upstream from mouth, in sec.31, T.8 S., R.ll E. 4.6 dry Do. .. Mill Creek At Highway 26 crossing, in sec.21, T.8 S., R.ll E. 2.9 70.4 +42.2 70.4 9.0 59 Table 8.-- Coliform sampling at selected sites Station Dis¬ charge Date of col- Coliform, in colonies per 100 ml number Stream name (ft 3 /s) lection Total Fecal 14092100 Deschutes River below Round Butte Dam 4,570 7-30-74 800 — 14092350 Willow Creek near Madras 100 do 4,600 -- 14092460 Campbell Creek near Warm Springs 15 do 12,800 — 14092700 Deschutes River near Warm Springs 4,600 do 520 — Shitike Creek above sewage lagoons 130 do 262 — 14093000 Shitike Creek at Warm Springs 152 do 343 Warm Springs River above sewage lagoons at Kahneeta village 347 do 440 “ “ do 299 9-19-74 10 2 14097100 Warm Springs River below sewage lagoons near Kahneeta 347 7-30-74 2,100 — — do 299 9-19-74 320 16 60 Table 9.-- Turbidity and sediment sampling at selected sites Station number Stream name Date Dis¬ charge (ft 3 /s) Turbid¬ ity (NTU) Sediment concen¬ tration (mg/ 1 ) Sediment discharge (tons/day) 14090500 Whitewater River 8 - 2-73 83.8 81 -- -- do 8-31-73 49.7 14 -- 14092460 Campbell Creek 6 - 7-73 21 -- 185 10 do 7-30-74 15 -- 32 1.3 14096820 Coyote Creek 2- 6-73 .9 28 12 .03 do 3- 5-73 2.9 43 14 .11 do 4- 3-73 .4 24 16 .02 do 5- 2-73 .03 19 4 .0003 do 1-14-74 150 76 264 107 do 1-28-74 55 40 -- 14096830 Beaver Creek 3- 5-73 52.3 24 4 .56 14096840 Quartz Creek 1-14-74 200 -- 2,170 1,170 14097050 Warm Springs River tributary do 29 -- 224 17 14097100 Warm Springs River do 1,910 412 2,120 do 1/15/74 4,610 -- 917 11,400 61 /Analyses by the U.S. Geological Survey/ (HVS) -uof qdaospB-mrrjpos sO O co *0 r- r-4 CO -4 sO sO —4 CM CO CO *0 sO n- o* ^ in (i 0 ) aanqBaaduiaj, CO Mt r4 *0 co in m vO m m —4 sO CO sO CM m in o sO —4 vO CO sX5 CM m n* m 55 65 (D 0 ) BjnqBaaduiBx O sO o in O vO 13.0 19.0 18.0 15.5 O co *-4 16.0 20.0 in o CM i-4 —4 r-4 15.5 16.0 CM r- r-4 O B“4 13.8 13.0 18.5 B3 Ou f-4 00 O 00 CM 00 o CM ^4 00 CO CO 00 m sO O O' CM CM 00 00 —4 00 o oo ^4 OO sO r>. CO 00 O' r>. O 0 SZ uio/soquiojoxui) 9 dub 3onpuoo OfjTOBds CN 00 co sO O ^4 232 323 CM ^4 O f-4 m in o f—4 as 3 f-4 00 m O' sO r4 r4 CM ^4 r4 162 150 E 00»0 * b ‘BBaupjBH sO CM r4 1-4 ^4 o 83 100 00 CO CO CM —4 o —4 —4 CO O' CM -4 CO CO o CO CM CO CM CM co r-. O' r-» m /Y b PT 1 ° b panioisfa f". r- m *0 sO in \C O' 203 218 CM O ^4 m O' 5 o 00 CM O' no m m O' r* CO CM 00 CO r-4 r4 O' 145 115 (a) UOJOH 0.02 (bv) 0T U3B - I V 1 1 i • i • CM o o o 1 1 1 1 1 CM O o r-4 o o 1 1 i i i i i t ? CO o o O' CM O 1 1 1 1 1 1 (^Od) aqBqdsoqj 0.25 O' o O' o r4 ^4 .18 .25 i—4 o r-4 1-4 o r-4 0* CM O' ^4 O S i-4 CM CO o 'O m CM CO CM (N) »3T«TU + B3BJ5TN m o o' CM o 3 CO ^4 CO i—4 f*^ r-4 00 O' i-4 —4 O' r4 CM n* m m co o ^4 o •m o CO o CO o O' o .10 .24 (I) apfjonij f-4 o ^4 co m —4 —4 f-4 —4 O CM o o CM CO ^4 CM CM V u U •r4 (TO) 9PfJ°mo in n* m O' ^4 2.6 10 —4 CM O' f—4 r>. Mt O' m oo O' CO ^4 O* CM ^4 CO O' r4 r- so r-4 ^4 U 0) a. (Vqs) B3Bjxn S f—4 CM f-4 CM co co sO CO 3.3 17 m m ^4 CO f-4 r-4 CM CM o o CM CM o CM r*v in sO CO 00 CM 2.4 1.6 to 0 (0 u (fOD) 33BuoqaB0 O O o O o o o o o sO CM o o o O o O o o o •H f-4 •H ( C 00H) 93BuoqjBopa co m sO CM O' CM O' sO 148 159 vO sO o n- CM CM O 00 o* so CO CO so m i-4 m i-4 SO CM sO CM 105 99 X (51) uinxsseqoj co 1—4 r-. O' O CM 5.8 4.7 00 m O CM O' O' 3- O' r'- i-4 i-4 r- m 20 15 (uw) asaueSuew O O O f-4 o o o i i CO f-4 o o r —4 o • 1 1 o o f-4 i-4 o o i-4 o co O o o o o CM o O O 1 • 1 (aj) uoax 0.02 O o CM Mt p4 .11 .12 co CM -t o . O T3 6/ 7/73 6/ 6/73 6/ 5/73 5/31/73 9/10/73 O TJ 5/ 9/74 6/ 7/73 5/30/73 9/17/74 Discharge (ft 3 /s) o co CM r4 sO CO m 00 4,570 1.4 26 f-4 CM O O SO v CO rH 00 tH co a 0) • • • P p 5-4 rH CN 00 vO co m VO tH m 00 cu a) P 5-i p 0) rH A A A tH A A A H cd B a i a C7v 00 •n r-'. r^. ov av CN in i-l r^. vO vO 1 CU /'“‘V p P COi-t a) cd o CO CN vO CO tH CO CN CN o P o 00 CN CN rH •H o pq B pq pq ^ 'w' 1 CM rH r". LO Ov m m vO m 00 r—1 cd O • • • ■ • • • • • •H O -H 00 rH CO tH 00 CO CO •rl CO B CN rH S “ / 1 P •H O a) o a a P U 5-i CO vO CO vO o av VO VO m co (1) *P X P o O rH rH CO co rH a

•H X oo \ rH 00 O m r-. 00 m o •H r~1 T—1 •H tH 00 CN tH rH co CN rH tH Q O o CO 6 CO CO re at 0) 00 CN 00 CO tH P rH rH o o T-1 o 1—1 o rH tH cd ct\ 1 i TO X 1 X 1 X) 1 i Q tH CTv ON CTv CTv av av /—N P 0) cu u «/ P Ai Sd p P •p B kO '—' 'w' X CU CU P p p X > o 00 AS cd P >— i p CU CO -P •H pq p o p p 1—1 O P cu P pq pcs • >> u sz 44 c r—l X a; ■u G CO co 0 co •rl O <0 0 co •H > 0 14-1 44 CD 44 sz fa z <0 0 u •rl • CO 44 SZ fa u 4J 3 Of 4J CO - CO O ■ 4-1 C0 r4 CD 44 CD 0 CD 00 co 3 00 «—1 O 44 CO 0 r4 3 >N 44 CO •* 0 J 14-1 CO CD 0 • 3 fa • sz 0) CO -K'* O fa 44 CO r-4 u-l U X G fa u CO •H • 0 CD CO CO X <0 CO O 0 O CO C 00 44 • 3 fa 0 > CO • (D <0 • c £ sz z U-4 0 CO 0 CO 03 fa 0 Z N fa 0 CO fa 0 co c CO • CO CO a> 01 • 1-4 3 3 0 3 as X CD CO C 3 C JZ • H 03 0 Z CO ti • • u • 4 r-4 e nO m 1 m CM 1 CM 1 CM 1 CO 00 CM 1 1 CM l 1 CM m 1 CO <0 p- CM 1 CM CM 1 CM 1 1 1 —1 1 1 l 1 1 a *r4 H CO 00 w p. 1 Z co z Z C/3 fa 03 z fa 03 X 1 03 fa Z z Z C/3 X X 1 fa O x Ml- Mf CM m m co <3 -3 >3 *3 <3 >3 m in pi pi p- p- r>* n- m NO p- r-. co p- 0 - pv nO NO r-4 r—l O 3 00 00 1 CO O 1 CM CM O O O O m 00 <3 CM O CM Pv m 1 44 3 co 00 rl r^- NO CM 00 r-l rl ■U X 4-1 O nO CO nO nO nO n* 00 NO nO NO p- nO 00 P- rv. m <3 r—4 3 U4 < fa P-' X CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM r -1 r-4 r—l fa 1 1 1 CO x _ • O CM 1 •H 1 x 00 1 NO 1 1 1 1 1 1 1 O O CM P- l 1 O O 1 1 • 1 1 c 1 fa x l 4 l 1 1 1 1 1 m CO CM 1 1 p- O 1 1 1 1 1 fa r-4 00 co CO co fa C/3 C/3 03 03 fa 00 fa •u fa 4J vD CO m NO 1 O NO O CM 1 CO O CM O O O O m O r—4 O a- u_i CO 44 CNI CO r —4 pi 1 m 3 CM 00 P- O NO 0 O O O m CM CM O 00 m m CM X CM co Q 5 w *—( fa r4 m m >3- CO CM co CO CO co ro r-4 r4 r-4 CM X V- l 0) O CO m CM 3 <3 m CO *3 00 m X X CO 0 44 p- pi nO p« pi co co 1 — co co nO CO nO n- m NO NO nO < a --4 1 —1 a 4-1 14-1 1 1 1 1—4 fa O O O rl 0 O 00 m N CO C r—4 CO r—l y <0 O 3 r-4 r-4 c r-4 >N <0 O •r-4 44 •r4 44 44 44 u CO r-4 •u 03 X 0 r-l CO sz CO U CO CT3 03 CO 2 £ 00 fa 0) c <0 X 0 r-l CO 3 <0 C co u r-l 0 a CO fa (1) 0 c 5 fa fa 3 c <—4 r-4 CD fa fa CJ 44 44 44 U_| 3 z G CO C0 0 3 O <0 3 co 3 CD y <0 ID CO I) CO CD 44 r—l fa fa >N u sz •H 03 4J fa O' fa •r4 C/3 C/3 C/3 £ fa * 01 OO 0 0 pi 0 r-* CO m r>. O >3 0 NO P- CO P- 00 O' X *3 O fa »— 4 co m CM r-4 CO *3 ^4 0 m CM CM m 0 0 X "3 ifa O' CO p. n. CM 0 O' 00 m CM m NO P- pv p- CM O' 00 x CM CM CM CM CM CM r-4 r-4 CM CM CM CM CM H r4 r-4 r4 r4 0 0 00 fa r-4 H i-4 r—4 r-4 r^ r-4 r4 rl r4 r-4 r-4 a CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM CM 0 1—4 r-4 r-4 r-4 <—* r—4 ■—l r-4 <—< is 01 X nO m O O m CO NO CM nO vO CO NO O' CO O' co nO X O 3 O CO O O CM CO O O CM CO CO O m CM CM 44 fa NO m 00 m m m CO m m CM O I* ;* 4J 0 m m m m m m m m m m m >3 >3 m m X X CO m 3 *3 >3 3 3 3 -S’ Mf <3 <3 -3 •<3 >3 <3 *3 <3 3 -3 *3 >3 •3 3 3 3 3 3 rO <0 X sz X CO X fa CO 0 X X X O 0 O <0 sz CO X JZ fa X CO X O 0 X X X fa u X fa fa X X X co rO JO O fa 0 O CO X 0 X X 0 CO co X X O 0 CM X •3 CM CM NO X O' >3 u NO X X >3 CO u 0 X Pi X X CM CM r4 X X X p. CM X NO r-4 CM X X X X X >3 r4 CM CM U fa fa fa fa fa fa fa fa fa fa fa fa fa fa fa fa fa fa fa fa O O r4 r—l r-4 r-4 CM CM CM r4 r—4 r4 r4 r4 CM CM CM CM X X X r—l r-4 H t—4 r4 r-4 r-4 r4 r-4 r-4 r-4 r4 r4 r4 r-4 r—4 r-4 r4 r4 r-4 r-4 M \ M \ \ '—. -V. *1»S Pi Pi *P. I, Is 1 ^ \ C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 C/3 X P^ Pi pi CP Pi Pi pi 00 00 00 00 00 00 00 00 00 00 00 00 76 Table 15.--Records of wells and test holes--Continued 0) r >-• fa • * u 3 3 a; *H 0J fa 0) O E X X o X3 4> •pH X G • eg C • CO • • • • •H TD • • B o X fa X) G X fa X) XI X 0) X 4> 3 4J O 0) CO 0) >> 0) a> OcL c CO 6 co •H CO 0) • CO T3 O CO CO CO 3 3 3 • fa X 3 0) V-i 3 3 X C C C0 C X a; e l-l u e • e < X • • X > X ai = C X CO • X o • o CJ o u CO So O O a> u Q CJ a» 3 V-4 T) fa x> C o 01 fa fa u fa fa fa fa fa fa fa X hJ fa hJ h 3 ►j 0) CO o a Q Q Q O D D Q a Q CO X 1 CO Q o O X Q o i G CO fa cd £ G /-s (0 3 U M O UH Q X w O O »—i 3 r O r* O co in ” 3 CO 3 3 3 d X *rH ^ B 4) \ ■H pH 5m CO ptf* 3 3 a Ph CO CO 25 3 vO 3 ON r*» o rH pH pH (N (N «J 4J S E a» 0 3 OJ H tl fa 4> co fa x o m in os so i •H 0) W 3 W pH 3 <; 4J w o O' m o o o oo 3 O' o 00 sO o CM o sr 00 o CO G •H fa CM O 0 ) £ ' Q 3 CO CM 3 3 o 00 o o 0 PQ CO G 0) u G *L O X CO •3 CO z •H CJ 4) B fa •U 3 B C co fa CO o c CO >s X 4) o 41 0) 3 o o 0 a u pH •pH 4) *H fa CO CO eg CO e J2 0 CJ c 4) U r-. 0 CO O X g 0 Z OH JS pH CJ CO 3 X x u UH u X c CO CJ O G o pH c •pH V-I CO r—1 3 cO X 41 co CO X u u o fa O Q Q CJ fa fa CO Q CO CO vO o co CM CO < CM m 00 pH m CM p - c CO CO CM in in CO CO o >3 v£) CO vO vO m in O' 00 x> r>* r*n. *3 pH Mf CM r-l p-^ r-4 pH pH pH p-H pH •—* i—1 •—> p-H p-t pH pH pH CM CM CM CM CM CM CM CM CM CM CM CM CM r—l i—l p-^ p-H »-H f-H pH pH pH pH O' r- Mf »—< CO sO r*. in 00 r- o o CM m CM CM O <3 *3 CM CM 00 O' r^. O'* vO m >3 >3 r-* >3- >3 ^3 -3 -3 *3 3 >3* ■4 <»■ 3 3 3 "3 Mf 3 ^3 >3 3 -3 3 V X 3 4) X 3 O' CO 3 o 3 o fa CM O O 8 3 O' 3 3 3 s fa 3 00 3 3 3 5 3 5 U X X X ca u X co fa a CO co o co X X CO X X X X (0 u X « O CO co fa fa CO co X a fa a u X CO X O X u X X X « X X co fa fa X CO o o 2 fa fa X X r- r*. CM CO o o pH X o fa 3 3 3 cn CM X 3 3 3 SO r- CM CM co co pH CM CM CM X o CM pH pH pH CM X X X X X X pH 1 1 1 1 1 1 1 ^3 pH 1 1 1 1 i i 1 i 1 1 1 fa U fa fa fa fa fa fa l 1 fa fa fa fa fa fa w fa fa fa fa fa X CO CO CO •3 «3 >3 3 fa fa pH CM CM CM CM CM CM CM CM CM CM X pH pH pH pH pH pH pH pH 00 00 pH pH pH pH pH pH pH pH pH pH pH pH \ \ '■'S. \ '»N^ '*>. -*» CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO CO 00 00 00 00 00 00 00 00 O' O' O' O' O' O' O' O' O' O' O' O' O' O' 77 Table 15.--Records of wells and test holes--Continued 8 o H ■U 3 CO C o o 0) r4 • o 4J CO T> z 0J *d 4 r -4 E r-4 r—4 r-4 CM 0) • CO 00 r fa CO Z CO X X X CO X fa fa fa fa p Pm m o cn m r-4 X X X X r*. so f"- X 0) V. \ \ — oo 00 4 J 05 o sO sO in O CO X o 1 ■st r>- X CO CM CM r-4 CM r—4 X t —4 X 1 O' O' Q -- \ r—4 \ r—4 0) o CM m cn r-4 r-4 r—4 X > t—1 r-4 O' 05 O' 05 O' O' O' O' O' O' O' O' O' >* O ^ r—4 r-4 r—4 t-4 1-4 r-4 t-4 a 0 C p u J 0 2 4-1 CM fa CO a CO 14 fa X c nj c r-4 m • CO 0 0 o X t-4 0 c p U 0 fa 0 0) > CO CO 44 J3 w o r-4 0) z »4 s jp X •r4 c w r-4 t-4 X w X CO Q o 0 X c CO t-4 c r—4 p CO z CO OJ CO u 0 X :s •f 4 0 W w 4) r-4 a) 4) a g P fa u 4) 14 •r4 X a 0) X B co 4J X C 52 g r—4 •r4 >s u 4* 0 3 0 X OJ 0 < CM CJ < o o fa fa < CO *-) o in 00 00 cn O' 00 00 O r-4 CM CM 0) o Mf CM X o X 'd' t-4 r -4 'd' o CM P CM n* 00 O' O' o t-4 r-4 r- X O 4J —4 r4 r-4 r4 r-4 r—4 CM CM CM CM •r4 oo r-4 r4 ^4 r—4 r-4 r-4 r-4 r-4 r-4 X t-4 1-4 r-4 a CM CM CM CM CM CM CM CM CM CM CM CM CM 0 r-4 r-4 r-4 r4 —4 r—4 —4 r-4 r4 t-4 r-4 —4 r-4 t-4 < u X X X CM o X X 00 O' CM X O' CM p CM X CM CM X o CM » CO CO CO CO CO CO CO CO CO CO CO CO CO o o o o o o o O o o r4 O' r-4 r-4 r-4 r—l r-4 r—4 —4 r-4 H t-4 r-4 r-4 78 Table 16.-- Drillers' logs of wells Materials Thick¬ ness Depth Alti¬ tude Materials Thick ness Depth Alti¬ tude (feet) (feet) (feet+) ( {eet ) (feet) (feeti) 5S/10E-22dcb . Bear Springs Campground. Alt 3,050 +50 ft. Drilled by Keller Well Drilling Co., 1970. Casing: 6-in diam to 26 ft; unperforated. Water level 8 ft, 1970. Reported yield 6 gal/min with 75 ft drawdown in 3% hr 7S/12E-34cab . Frank Suppah. Alt 2,811 +1 ft. Drilled by R. J. Strasser Drilling Co., about 1935. Casing: 6-in diam to 12 ft. Water level 100 ft, 1955. Sustained yield about 2 gal/min based on U.S. Geological Survey tests Soil and gravel- . 3 3 3,047 Clay, brown- Andesite: . 9 12 3,038 Clay and rock- . 11 23 3,027 Rock, gray, soft- . 8 31 3,019 Rock, medium-hard- . 8 39 3,011 Rock, hard---- . 5 44 3,006 Rock, soft- . 1 45 3,005 Rock, gray, soft--- . 25 70 2,980 Rock, soft- 72 2,978 Rock, hard--- . 9 81 2,969 Rock, broken- . 3 84 2,966 Rock, hard—-- . 6 90 2,960 Rock, red, soft- . 5 95 2,955 Clay, brown--- . 5 100 2,950 7S/10E-25daa . Dorothy Wally. Alt 2,650 +10 ft. Drilled by Archie Fox Well Drilling, 1973. Casing: 6-in. diam to 133 ft; screen 133-138 ft. Water level 118 ft, 1973. Reported yield 25 gal/min with 4 ft drawdown in 4 hr Soil. Gravel: Gravel and clay- Gravel- Clay- Gravel, water-bearing 2 2 2,648 55 57 2,593 8 65 2,585 66 131 2,519 9 140 2,510 7S/llE-14abd . Florence Pete. Alt 2,310 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in. diam to 15 ft; hole abandoned Alluvium: Clay, brown, and sand- Gravel, coarse- Clarno Formation: Clay, red- 7S/llE-32bab . Grant Waheneka. Alt 2,625 Archie Fox Well Drilling, 1972. Casing: 6 screen 76-81 ft. Water level 63 ft, 1974. gal/min with 1 in drawdown in 5 hr Soil. Gravel: Clay, yellow, and broken rock- Clay, brown, sandy-— Gravel, water-bearing--- Basalt: Rock, broken, water-bearing- less than 1/2 gal/min Soil. Basalt: Lava, medium-hard---------- Clay, yellow-------------- Sandstone, brown-- Clay, red- Clay, brown, and gravel- Clay, light-gray, and gravel- Clay, light-tan- John Day Formation: Claystone---- Clarno Formation: Rock, fractured- 12 12 2,298 3 15 2,295 107 122 2,188 ft. Drilled by .-in diam to 76 ft; Reported yield 25 1 1 2,624 29 30 2,595 41 71 2,554 2 73 2,552 8 81 2,544 .. Alt 2,700 +5 ft. •ng: 6- ■in diam to 30 ■ . Reported yield 4 4 2,696 10 14 2,686 12 26 2,674 64 90 2,610 10 100 2,600 40 140 2,560 15 155 2,545 95 250 2,450 20 270 2,430 130 400 2,300 Soil and gravel John Day Formation: Basalt, soft--- Clarno Formation: Basalt, hard- Rock, fractured 12 12 2,799 108 120 2,691 58 178 2,63: 122 300 2,511 8S/llE-16dca . Phillip Guerin. Alt 2,615 +5 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 30 ft; unperforated. Water level 30 ft, 1965. Reported yield 30 gal/min with 146 ft drawdown in 1 hr Clay, brown, and sand- •. 3 3 2,612 Gravel: Gravel, coarse, and clay- ■. 27 30 2,58 Basalt: Basalt, gray- •. 6 36 2,579 Claystone, yellow- ■. 10 46 2,569 Basalt- •. 129 175 2,440 Dalles Formation: Sandstone, brown- •. 21 196 2,419 Claystone, red- •. 4 200 2,415 Basalt- •. 8 208 2,407 8S/llE-25ccc . Elmer Quinn. Alt 2,642 +5 ft. Drilled by Archie Fox Well Drilling, 1973. Casing: 6-in diam to 300 ft, 5-in diam to 350 ft; screened 300-305 ft and 345-350 ft. Water level 290 ft, 1973. U.S. Geological Survey-observed test yielded 18 gal/min with 6 ft drawdown in 4 hr Soil. 1 1 2,641 Clay, yellow- 3 4 2,638 Basalt: Basalt, broken- 56 60 2,582 Clay, red, soft- 10 70 2,572 Basalt, broken, and clay- 40 110 2,532 Clay, red, soft- 15 125 2,517 Basalt, broken-- 25 150 2,492 Basalt, hard- 15 165 2,477 Basalt, soft, broken, and clay- 20 185 2,457 Basalt, hard- 15 200 2,442 Basalt, soft, and brown clay- 50 250 2,392 Basalt- 10 260 2,382 Dalles Formation: Clay, brown, soft, and broken basalt- 30 290 2,352 Clay, brown, soft- 10 300 2,342 Sand, water-bearing--- 5 305 2,337 Sandstone, black- 40 345 2,297 Sand, water-bearing--- 7 352 2,290 8S/llE-33ddd . Irene Wells. Alt 2,735 +10 ft. Drilled by Archie Fox Well Drilling, 1974. Casing: 6-in diam to 322 ft; screen 322-327 ft. Water level 255 ft, 1974. Reported yield 12 gal/min with 30 ft drawdown in 2 hr Soil. Clay. Basalt: Rock, broken, and clay- Lava rock-—- Sand and clay- Lava rock-- Sand and clay--------- Lava rock--- Dalles Formation: Sand and clay---- Sand and gravel, water-bearing 1 1 2,734 2 3 2,732 4 7 2,728 76 83 2,652 14 97 2,638 5 102 2,633 16 118 2,617 129 247 2,488 73 320 2,415 7 327 2,408 79 Table 16.-- Drillers' logs of wells --Contlnued Materials Thick¬ ness Depth Alti¬ tude Materials Thick¬ ness Depth Alti¬ tude (feet) (feet) (feet+) (feet) (feet) (feeti) 8S/llE-34ddd . Miller Well. Alt 2,680 +5 ft. Drilled by R. J. Strasser Drilling Co., 1934. Water level 208 ft, 1934 Casing: 6-in. diam to 20 ft. Basalt: Basalt- . 248 248 2,432 Dalles Formation: Gravel, cemented- . 72 320 2,360 8S/13E-23cdc . Kip Culpus. Alt 1,410 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Hole abandoned Alluvium: Gravel, coarse- . 25 25 1,385 John Day Formation: Clay, red- . 195 220 1,190 8S/12E-3acd . Velma Peters. Alt 2,810 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Abandoned test hole 8S/13E-27bb . Franklin Suppah. Alt 1,420 +20 ft. Drilled by George McClanahan Well Drilling, 1965. Hole abandoned; exact location not confirmed Alluvium: Clay, red- ■. 12 12 2,808 Claystone, yellow- Basalt: 30 42 2,778 Basalt, fractured- .. 168 210 2,610 Basalt- . 44 254 2,566 Basalt, fractured- .. 54 308 2,512 8S/12E-3cab. Schoolie Flat 380-ft test well (Ella Wolfe). Alt 2,770 +10 ft. Drilled by Archie Fox Well Drilling, 1973, Casing: 6-in diam to 302 ft; perforated 70-75, 245-250, 290-300 ft. Water level 132 ft, 1974. Reported yield 2 gal/min with 33 ft drawdown in 1 hr Basalt(?): Rock, broken, and yellow clay- . 18 18 2,752 Gravel and reddish-brown clay- . 7 25 2,745 Clay, brown, soft, and gravel- . 15 40 2,730 Gravel and red clay- . 10 50 2,720 Clay, red, sticky- - 10 60 2,710 Clay, light-brown, and sand— . 10 70 2,700 Clay, white, and sand- . 10 80 2,690 Clay, red, soft- . 5 85 2,685 Clay, red, and gravel- . 5 90 2,680 Rock, yellow, soft, and clay-- .. 140 250 2,520 Clarno Formation: Rock, brown, hard- . 130 380 2,390 8S/12E-4ddd . Schoolie Flat Well (Yahtin). Alt 2,710 +10 ft. Drilled by Lawrence Kowaleski, 1958. Casing: 6-in eTiam to 15 ft. Water level 82 ft, 1974 Soil.. Gravel- Basalt (?) : Clay, red-- Clay, gray- Clay, red . "Bed rock" 2 2 2,708 4 6 2,704 113 119 2,591 16 135 2,575 4 139 2,571 11 150 2,560 8S/13E-17dbd . Margaret Charley. Alt 1,580 +10 ft. Drilled by Lawrence' Kowaleski, 1959; reconditioned by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 30 ft; unperfor¬ ated. Water level 7 ft, 1965. Reported yield 2 gal/min with 31 ft drawdown in 2 hr John Day Formation: Clay, yellow, and gravel- 16 16 1,564 Clay, red- 109 125 1,455 8S/13E-23cbc . Ella Wolfe. Alt 1,410 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 31 ft; unperforated. Water level 15 ft, 1965. Reported yield 5 gal/min with 15 ft drawdown in 1 hr Alluvium: Clay, brown, and sand- . 7 7 1,413 Gravel, coarse- - 5 12 1,408 John Day Formation: Clay, red- . 150 162 1,258 8S/13E-27cdc . Sarena Boyd. Alt 1,590 +20 ft. Drilled by Archie Fox Well Drilling, 1973. Casing: 6-in diam to 250 ft; perforated 42-250 ft. Water level 15 ft, 1974. Reported yield 8 gal/min with 220 ft drawdown in 4 hr John Day Formation: Clay, sandy, loose- Clay, yellow, sandy- Clay, white- Clay, light-red- Clay, white, sandy- Clay, dark-red, sticky- 8S/13E-33cab . Delbert Frank. Alt Archie Fox Well Drilling, 1972. Casing: 19 ft, 1972. in 6 hr Reported yield 7 Clay, yellow- Gravel- John Day Formation: Clay, tan- Clay, reddish-brown- Clay, tan- Clay, red-brown, with white specks- Clay, gray-tan- Clay, red- Clay, gray- Clay, gray, hard- Sandstone, brown- Clay, red, hard- Sandstone, water-bearing- Clay, red, hard- Sand, gravel, and clay- Clay, red--- 75 75 1,515 75 150 1,440 20 170 1,420 10 180 1,410 10 190 1,400 60 250 1,340 :t. Drilled by i-in diam to 247 ft. Water level i 230 l ft drawdown 7 7 1,798 2 9 1,796 16 25 1,780 10 35 1,770 15 50 1,755 35 85 1,720 25 110 1,695 20 130 1,675 55 185 1,620 40 225 1,580 10 235 1,570 48 283 1,522 5 288 1,517 87 375 1,430 5 380 1,425 5 385 1,420 8S/14E-17dcd. Clarence Meanus. Alt 1, 300 +5 ft. Drilled by George McClanahan Well Drilling, 1965 . Casing: 6-in diam to 100 ft; unperforated. Water level 30 yield 3 gal/min with 110 ft drawdown ft, 1965. in 1 hr Reported Alluvium: Gravel and sand — -- 23 23 1,277 John Day Formation: Clay, white, and fine sand--- --- 70 93 1,207 Sandstone, brown- — 69 162 1,138 Soil. . 3 3 1,407 Alluvium: Clay, red, and sand- . 8 11 1,399 Gravel, coarse—---- . 5 16 1,394 John Day Formation: Clay, brown- . 15 31 1,379 Claystone, white—-- . 1 32 1,378 Claystone, brown---- — . 3 35 1,375 8S/14E-20bda. Sanders Heath. Alt 1,290 +10 ft. Drilled by Archie Fox Well Drilling, 1971. Casing: 8-in diam to 125 ft; perforated 55-60, 120-125 ft. Reported yield 4 gal/min with 40 Water level 26 ft, ft drawdown in 4 hr 1971. John Day Formation: Clay, yellow, and gravel- . 13 13 1,277 Clay, yellow---- •. 17 30 1,260 Clay, blue-green--- •. 27 57 1,233 Clay, green- •. 18 75 1,215 Clay, gray.. ■. 50 125 1,165 80 Table 16.-- Drillers 1 logs of we 11s --Continued Materials Thick¬ ness Depth Alti¬ tude Materials Thick¬ ness Depth Alti¬ tude (feet) (feet) (feeti) (feet) (feet) (feett) 8S/14E-20dac . Nathan Heath. Alt 1,280 +10 ft. Drilled by Lawrence Kowaleski, 1958. Casing: 6-in diam to 33 ft. Water level 27 ft, 1958. Reported yield 12 gal/min with 3 ft draw¬ down in 3 hr Soil, sand- Alluvium: Gravel, coarse, and clay- 6 28 6 34 1,274 1,246 8S/14E-21acb . Clara Moody. Alt 1,270 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 20 ft; unperforated. Water level 5 ft, 1965. Reported yield 12 gal/min with 9 ft drawdown in 1 hr A1luvium: Clay, brown, and sand- 7 7 1,263 Gravel, coarse- 12 19 1,251 Gravel, medium- 3 22 1,248 9S/8E-4ddb . Olallie Lake Guard Station. Alt 4,950 +25 ft. Drilled by Steinman Bros., 1962. Casing: 6-in diam to 26 ft, 5-in diam 234-254 ft; perforated 240-253 ft. Water level 226 ft, 1962. Reported yield 7 gal/min with total drawdown (28 ft) in 1 hr Clay, brown, sandy- Andesite: Rock, gray, soft- Rock, gray, medium-soft-- Rock, brown, soft- Rock, brown, broken- Rock, brown, medium-hard- Rock, brown, soft- Rock, brown, medium-hard- Rock, gray, hard- Rock, brown, hard- Rock, gray, hard- Cinders, red, loose- 20 29 6 4 12 21 50 56 60 72 4,949 4,929 4,900 4,894 4,890 4,878 13 254 4,696 9S/8E-10cba . Olallie Lake Peninsula Campground. Alt 4,948 +25 ft. Drilled by Steinman Bros., 1962. Casing: 6-in diam to 22 ft, 5-in diam 190-242 ft; perforated 225-240 ft. Water level 0 ft, 1974. Reported yield 15 gal/min with total draw¬ down in 1 hr Clay, brown, sandy, and broken rock-- 3 3 4,945 Andesite: Rock, gray, medium-hard- 7 10 4,938 Rock, gray, broken- 3 13 4,935 Rock, gray, medium-soft- 22 35 4,913 Rock, gray, hard- 13 48 4,900 Rock, brown, hard- 20 68 4,880 Rock, gray, hard- 49 117 4,831 Rock, brown, hard—-- 3 120 4,828 Rock, gray, hard- 37 157 4,791 Rock, brown, hard- 5 162 4,786 Rock, gray, hard- 32 194 4,754 Cinders, red, loose- 8 202 4,746 Rock and clay, red, decomposed- 34 236 4,712 Rock, red, decomposed (water¬ bearing)— -- 6 242 4,706 9S/llE-2baa . Prosanna Williams. Alt 2,680 +5 ft. Drilled by Archie Fox Well Drilling, 1973. Casing: 6-in diam to 370 ft; screened 370-375 ft. Water level 352 ft, 1973. Reported yield 18 gal/min with 6 ft drawdown in 4 hr Soil. 3 3 2,677 Basalt: Basalt, broken, and clay------ 47 50 2,630 Clay, red, soft- io 60 2,620 Basalt, broken, and clay- 18 78 2,602 Clay, red, soft- 19 97 2,583 Basalt, broken, and clay- 56 153 2,527 Clay, red, soft. 202 355 2,325 Dalles Formation: Sand and gravel, water-bearing- 20 375 2,305 9S/12E-14dac . Dan Macy. Alt 1,665 +5 ft. Drilled by Cunningham Well Drilling, 1971. Casing: 6-in diam to 40 ft; perforated 24-40 ft. Water level 18 ft, 1973 Soil. John Day Formation: Basalt, soft- Clay, brown- Sand, water-bearing- 9S/12E-32cda . Delton Switzler. Alt 1, Lawrence Kowaleski, 1966. Casing: 6 Water level 56 ft, 1966. Reported yi ft drawdown in 1 hr Soil, black- Gravel- John Day Formation: Clay, yellow- Clay, gray- Clay, yellow, with basaltic fragments- Clay, yellow, hard, with basaltic fragments- Clay, blue- 9S/12E-33ccc . Dan Macy. Alt 1,730 +10 ft. Drilled by Cunningham Well Drilling, 1971. Casing: 8-in. diam to 20 ft. Water level 38 ft, 1971. Reported yield 4 gal/min with "no" drawdown in 1 hr 4 4 1,661 27 31 1,634 65 96 1,569 6 102 1,563 +20 ft. Drilled by diam to 21 ft, 12 gal/min with 26 2 2 1,838 8 10 1,830 32 42 1,798 38 80 1,760 11 91 1,749 38 129 1,711 3 132 1,708 13 85 4,865 Soil- . 2 2 1,728 20 105 4,845 John Day Formation: 43 148 4,802 Clay- . 58 60 1,670 11 159 4,643 Clay, sandy- -. 60 120 1,610 82 241 4,709 Sand, water-bearing- . 30 150 1,580 9S/12E-34aba . Clifford ("Pete") Courtney. Alt 1,590 +10 ft. Drilled by Lawrence Kowaleski, 1963. Casing: 6-in diam to 20 ft; unperforated. Water level 15 ft, 1963. Reported yield 4% gal/min with 450 ft drawdown in 2 hr John Day Formation: Clay, red- Clay, yellow- Claystone, blue- Claystone, red- Sand, black, water-bearing- Clay, red, and fine sand--- Sand, black, fine- Clay, red- 9S/12E-34bcdl . Bart Clements. Alt 1,620 George McClanahan, 1965. Casing: 6-in unperforated. Water level 8 ft, 1965. gal/min with 57 ft drawdown in 1 hr Alluvium: Clay, brown, and sand--- John Day Formation: Claystone, brown- Sandstone, gray- 9S/12E-34bcd2 . Ed Manion. Alt 1,620 _ Lawrence Kowaleski, 1967. Casing: 6-in diam to 63 ft; un¬ perforated. Water level 5 ft, 1967. Reported yield 10 gal/min with 48 ft drawdown in 1 hr Alluvium: Clay, black----- Sandstone, light-green--- Sand, loose- Pumice and black clay- John Day Formation: Clay, blue, with sand- Clay, black, with sand and decayed wood- Clay, blue, with gravel--- Clay, yellow, with sand and gravel- 20 20 1,570 65 85 1,505 95 180 1,410 102 282 1,308 3 285 1,305 160 445 1,145 1 446 1,144 54 500 1,090 +10 ft. Drilled by diam to 64 ft; Reported yield 2 10 10 1,610 60 70 1,550 12 82 1,538 ft. Drilled by 18 18 1,602 3 21 1,599 6 27 1,593 2 29 1,591 6 35 1,585 13 48 1,572 9 57 1,563 27 84 1,536 81 Table 16.-- Drillers' logs of wells --Continued Materials Thick¬ ness Depth Alti¬ tude Materials Thick¬ ness Depth (feet) (feet) (feeti) (feet) (feet) Alti¬ tude (feett) 9S/12E-36dda . Stanley Smith, Jr. Alt 1,380 +10 ft. Drilled by Archie Fox Well Drilling, 1971. Casing: 6-in diam to 25 ft; screen 25-30 ft. Water level 9 ft, 1971. Reported yield 15 gal/min with 4% ft drawdown in 3% hr Soil. A1 luvium: Sand, gravel, and clay, consolidated-- Sand and gravel, unconsolidated- Sand, gravel, and clay, consolidated-- Sand and gravel, unconsolidated- John Day Formation: Clay, yellow- 9S/13E-17dad . Dry Creek Campground. Alt 1,350 +10 ft. Drilled by Lawrence Kowaleski, 1964. Casing: 6-in diam to 19 ft; un¬ perforated. Water level 7 ft, 1973. Reported yield 5 gal/min 1 1 1,379 11 12 1,368 1 13 1,367 7 20 1,360 10 30 1,350 5 35 1,345 10S/12E-29add . Orin Johnson. Alt 1,940 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 24 ft; unperforated. Water level 6 ft, 1965. Reported yield 10 gal/min with 10 ft drawdown in 1 hr Alluvium: Clay, brown, and sand- Gravel, coarse, and sand- Dalles Formation: Sandstone, gray- 10S/12E-29bdd . Ray Johnson. Alt 1,950 +10 ft. Drilled by Bert Abrams, 1971. Casing: 4-in diam to 42 ft; unperforated. Water level 21 ft, 1971. Reported yield 9 gal/min with 11 ft drawdown in 2 hr Alluvium: 7 7 1,933 10 17 1,923 35 52 1,888 with 4 ft drawdown in 1 hr Silt, sandy- 17 17 1,933 Silt, sandy, with gravel- 7 24 1,926 Soil, sandy- . 7 7 1,343 Dalles Formation: Alluvium: Sandstone, dark- 4 28 1,922 Gravel- . 5 12 1,338 Sandstone, light-colored, with Clay, soft- . 4 16 1,334 gravel-- 19 47 1,903 Gravel- 3 * 19% 1,330 9S/13E-17dcd . Andrew David. Alt 1,360 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 19 ft; unperforated. Water level 15 ft, 1965. Reported yield 8 gal/min with 3 ft drawdown in 1 hr 10S/12E-30abc . Karen Wallulatum. Alt 2,020 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 24 ft; unperforated. Water level 16 ft, 1965. Reported yield 7 gal/min with 8 ft drawdown in 1 hr Loam sandy- Alluvium: Gravel, coarse- 8 12 8 1,352 20 1,340 2,016 14 18 2, ,002 11 29 1, ,991 13 42 1. ,978 10S/12E-lcaal . Zane Jackson. Alt 1,410 +10 ft. Drilled by Bert Abrams, 1960. Casing: 6-in diam to 27 ft; perforated 16-27 ft. Water level 14 ft, 1960. Reported yield 5 gal/min with 50 ft drawdown in 3 hr Alluvium: Sand, consolidated- Sand, loose- Gravel, coarse, and hardpan- John Day Formation: Clay, silty- Clay, tuffaceous- 10S/12E-lcaa2 . Charlie Jackson. Alt 1,47( Archie Fox Well Drilling, 1973. Casing: perforated 75-175 ft. Water level 79 ft, 7 gal/min with 90 ft drawdown in 4 hr Clay, soil, and gravel- Alluvium: Gravel- Rock, broken, and clay- Gravel, water-bearing^- John Day Formation: Clay, brown, and sand- Clay, green, and sand- Clay, red-brown, sticky- Alluvium: Clay, brown, and sand- Gravel, medium, and clay- Gravel, medium, and claystone- Dalles Formation: Claystone, brown- 10S/12E-30bbd . Avex Miller, Jr. Alt 2,030 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 23 ft; unperforated. Water level 20 ft, 1965. Reported yield 4% gal/min with 36 ft drawdown in 1 hr 6 6 1,404 13 19 1,391 Alluvium: 2 21 1,389 Clay, brown, and sand- 2 2 2,028 Dalles Formation: 4 25 1,385 Sandstone, brown- 60 62 1,968 55 80 1,330 llS/12E-2ccc. Simtustus Park Campground. Alt 1,640 +10 ft. +10 ft . Drilled by Drilled by Bert Abrams, 1962. Casing: 6-in diam to 68 ft; 6-in. diam to 175 ft; unperforated. Water level 52 ft, 1973. Reported yield 15 1974. Reported yield gal/min with "no apparent" drawdown in 1% hr Alluvium: 3 3 1,467 Conglomerate (pumice)- 28 28 1,612 Dalles Formation: 37 40 1,430 Ash, red, cemented- 23 51 1,589 20 60 1,410 Basalt, vesicular- 17 68 1,572 15 75 1,395 70 5 25 145 150 175 1,325 1,320 1,295 10S/12E-28bdb . Gilbert Kalama. Alt 1,920 +10 ft. Drilled by George McClanahan Well Drilling, 1965. Casing: 6-in diam to 24 ft; unperforated. Water level 20 ft, 1965. Reported yield 6 gal/min with 28 ft drawdown in 1 hr Alluvium: Clay, brown, and sand- Gravel, coarse- Dalles Formation: 10 10 1, ,910 8 18 1, ,902 44 62 1, ,858 llS/12E-18dcc . Joe Estabrook. Alt 2,580 +10 ft. Drilled by Bert Abrams (?), 1958. Casing: 6-in diam to 12 ft. Water level 152 ft when drilled; later dropped to 260 ft. Reported yield 20 gal/min when drilled, but in 1973 piston pump produced several gallons per minute or less Soil. Basalt: Pumice- Basalt- Basalt, vesicular- Dalles Formation: Tuff. Basalt, gravel, sandstone, and conglomerate- Lava rock- Sandstone- 3 3 2,577 7 10 2,570 8 18 2,562 24 42 2,538 76 118 2,462 198 316 2,264 26 342 2,238 28 370 2,210 82 /Analyses by the U.S. Geological Survey/ (HVS) ou»a H CM sO vO px m >0 cn H ON 00 m 1 o m m 00 NO CM -1107 ijdaoepp am-jpog H H H CM r-4 r-4 ^4 (do) »injBiadm»x 00 m cn m 09 60 cn NO -4 m 0N l l r—4 m 50 1 1 1 1 cn m 62 63 i • 1 1 s p^ m 63 1 1 1 1 1 1 m m m m m m m m o oo 00 o cn o © (3 0 ) amieiadmax x 0 * H in m rx. o ON 1 o o 1 1 r—4 NO Px. i 1 1 X0 x* P". 1 1 1 1 1 r—4 r—4 •—4 i—s r-4 H f4 r-4 —4 r-4 H r-4 r—4 i-4 m *n CM vO cn vO 0N cn f-4 cn ON - m r*^ o NO NO © o On X0 xj CL px px. Px IX px r^. P*» 00 r^. p^ PN. 00 p*. p^ Pv 00 px. px. 00 fx. NO fx- px- (DoSZ 3® mo/eomnojo-pn) *0 rx. CM <* CM m CM CM sO nO cn m 98 , NO O 8 CO •—4 00 NO 96 3 93 00 X0 CM x 0 oo px. CM X0 1 1 cn 00 NO aouejonpuoo oujaadg —4 CM cn H CM H H H H r-4 CM r-4 r-4 r-4 r-4 CM r4 CM E(X>BD ®a ‘SBaupiBH CM o o CM m ON < P** P^ in 00 00 00 CM m CM «—4 >0 H vO vO cn >0 >0 ■0 m >0 CM *0 r-4 in x 0 in m x 0 ON fx. nO X 0 CM m r—4 00 0 N ON cn NO ^0 CM NO NO o ON P^ px. © On 3 CM © /y®PTT08 paAiossTa px x 0 •—4 CM CM CM H O CM 0N ON ON ON cn r—4 r-4 r-4 ON in r-4 o r-4 CM r—4 CM r4 *0 H r-4 r4 On px. 1 ^ oo ^4 3 O x .43 o (N) aifaiTU i i 1 1 o CM l l 18 O 01 18 79 O' H 08 cn 09 CM CM n- CO o P^ cn m 09 00 m + 93BJ3TN O H CM r—4 r-4 r-4 r4 r4 H CM o f4 CM r4 r-4 H CM r—4 r* cn o r-4 ON CM r4 cn cn O f-4 cn cn NO (d) apiJon TJ © r-4 r-4 0 ) O 00 CM 00 x 0 cn m NO Mf m 00 NO >0 cn o X 0 cn m m m p^ O' x4 —4 (13) apiJomS CM CM CM CM 16 r-4 CM r—4 —4 r-4 CM cn CM r4 NO r—4 cn r-4 CM X0 x 0 Px U m r^ sO 0 i O NO o NO r—4 r-4 CM NO r-4 r4 r—4 00 00 *0 NO NO X0 O' cn n § (^OS) aiBJins CM —4 H H H NO CM CM CM CM NO CM ^4 0 X 0 r-4 r-4 cn -< CM X0 CM cn 0 u (E03) aisuoqieo o o o o o O o o O O O O o O O o o o o o © O o t4 H r-4 •H ( C 03H) aisuoqiBofa nO 00 o o 0 N NO p**- 00 O m CM *0 ^0 3 in m CM o NO m px o H CM m h r—4 CM o r4 o H NO NO m O i-4 r- in CM r-4 00 oo On 00 NO NO r-4 r-4 r4 r-4 r-4 cn rH px 00 Px m m m cn p^ rx. *0 NO cn CO m O fx- CM CM CM o (y) mnis8B508 -0 cn cn cn H p*- f—4 r-4 r-4 r-4 1—4 r4 cn CM H CM CM CM 00 *0 p^ ON r-4 in 00 00 00 (®N) ran TP°S •—■4 m px CM m NO —4 in ON cn ON r-4 cn 00 r-4 NO 00 P^ ON cn CM -4 i-4 r-4 CM r-4 r—4 cn r-4 r-4 r-4 r4 CM ( 8 h) nmfsBUgBM CM x 0 X 0 «0 00 0N -0 m NO P». 00 00 NO 00 r4 00 o P^ x 0 O' NO nO O cn cn cn 00 px i-^ -0 NO m «0 r-4 cn CM NO NO in m x 0 O' px. NO H m 00 sj- o CM ON X 0 r4 (®3) umioi®3 cn px —4 CM 3 1 1 0 r4 40 a a g£ 1 r-4 x4 i s 0 *3 0 Us is I | 3 s s s 41 3 0Q & r4 < X x4 w CO M Us X < N-4 CO w •4 CO A 04 r4 U M H U V-4 u CO 51 j w O' u 2 O O : P*X 3 £ •3 0 1 0 0 <5 0 A 0 cn o A 0 cn s CM CM Px. CM cn cn rx U3 w U1 W U) W UJ U) UJ r-4 —4 r-4 CM o o r-4 -4 CM —4 —4 —4 r-4 r4 1-4 r-4 x- XX- x^ Xx. x-^ •x- CO CO CO CO CO CO CO CO CO NO NO NO NO p^ px px px px O 0 I 0 px —4 i S to) cn »—4 x^ x^, CO CO .O 3 £ s £ 0 3 O u X* w X0 3 8 3 X 3 3 S 0 o 0 U) CM u 3 cn i h) CM *0 U 3 3 f T UI W 83 !_/ Calculated values with bicarbonate recomputed as carbonate. Table 17.-- Chemical analyses of water from selected wells and springs --Continued 0 oo vO n«. NO r** m pH OO CM CO 00 00 oo m r*» CM 00 00 r- r—t 00 in r*. pH 00 -3 r>* NO r** O' r^. (3oS3 un/soquioaopu) aouBtjonpuoo ojj-poads CO o p-• CO NO CM CM pH 00 CM CM co 3 1,790 o o 3 »H o 3 pH H r-H CO m CM O' t—4 CO O' ON CM CO pH ON St NO CO CO O NO >3 00 CM NO m CM 00 00 pH E()D b 0 ® B ‘BSBUpjBH 3 3 O CO CO CM O' CM 3 1 CO o pH 3 pH O' r“H m NO CO pH m O' CM CM CM o CO pH NO pH NO NO NO m m ^SpTTOS p9A"[08 8JQ on O' 'O st St CO »H pH 00 CM st pH CO o o f—l 00 1,020 m •o- CM co CM CM CM *3 CM *3 NO CM O CM fH r>* NO CO 00 CO CM 00 CO NO CO CM pH CM CM st r>» pH (a) uojog ro o o CM O CM O 1 1 o NO m VO CM 1 1 1 1 O O O m o 1 1 3 1 1 1 1 1 1 1 1 1 • (sy) opussay o CM O O ON CM O CO o 00 pH o 3 co O CO 1 1 1 1 m o o f'* r“l o O' 8 CM «—• O 00 pH O 1 1 1 1 o o o m 8 1 1 (VOJ) BJBqdsoqg 0.12 o pH pH CM r-. m O' m CM m CM m CM n- 00 h <—< co NO pH sO *>3 NO 00 pH 1 1 00 CM pH CM pH co (N) B 4T«T“ + BasaapK 0.16 CM pH 00 sO H 00 m NO o o r>» 00 3 o CO 00 in f>. 00 CM O' »3 CM CM CM 00 1 1 r** m NO pH O' O' (I) aPT^onii pH o pH pH m o pH H CM CO CM r-* CM in r-* r" CM CO NO o sO -3 CO » NO On oo r*. pH CM m sO On NO r*. pH O' NO 00 •3 O' rs. 0) a CO E (Vqs) 35Bjpng co r>* pH o so o i—1 pH pH CO 3 CO O' CO 00 t-M O' NO H o St 00 pH O' O' oo m pH m NO 00 NO pH ■3 cd 00 •H (COD) 33BuoqaB0 o CM o o o o o CO O o o o o O o o o O o O •H £ ,(tODH) 33BUoqaBopg CO r*» 00 s> CO o so O' CM r-l CO sO CM CO o NO 3 o m NO 00 CO 00 sO •■M 00 co i—i O' r^. r—4 CM NO pH St m St NO pH oo oo pH m CM n* m pH m co pH O O pH 00 mnpssBjog pH pH m vO CO 1—1 m m O' - 00 CO co oo m o -3 NO co m >3 pH CM St O' NO NO sO NO *3 st (bn) mnppos 00 st O co pH st H co st O O pH O O 3 o CM CO o 00 CO CM m co O NO sO 3- r—< CM H ON CM oo CO co pH CM pH CM co pH (uw) bssubSubw o o o CO o o O o o m m o o o CM o H o o o CO o i—i o o o NO o o i i pH o pH o pH o ( B i) aoai 0.33 O o 00 st NO pH o NO NO o m O NO o m o o CM ON o n- o m CM o nO nO pH pH sO O NO o ( Z 0TS) B3 TTTS 00 CO CO m 3^ o oo CO st oo m oo m r» so NO H in oo oo CM St in St m CO pH r*^ r*. O' NO Date of col - lection CO n* o CM "■h. 5/ 9/74 6/ 8/73 9/11/73 5/17/73 5/14/73 3 r*. 3 CM T— 1 co r-. pH m O T3 o TJ 9/10/73 o TJ CO l-» CM pH St O TJ 0 TJ St r'- CM CM 4/11/73 O TJ o TJ Prin¬ cipal geo¬ logic source TJ H TJ H TO •*“) H tj T H TO 1 H X> •*-» H tj H T5 •n H XJ H XJ •*-» H XJ H 1 TJ H Tjd(?) TJ •'-) H u o H cd H TJ *p“I H TJ •*-» H Td/Tjd (s) Supjds (M) tt b m CO CO CO CO 3 CO CO CO CO 5 CO CO CO CO C/3 CO Name or (location) Buck Spring (South of Skookum Creek) Wire Corral Spring Charley Corral Spring Margaret Charley (Hot spring east of hatchery) Kahneeta Hot Spring (Hot spring west of Kahneeta) (Northeast of Eagle Butte) Ida McKinley Delbert Frank Harold Culpus Rattlesnake Spring Sanders Heath (South of Webster Flat) Olallie Lake Guard Station (South of Eagle Butte) Tohet Spring (Upper Dry Creek) Location number 8S/12E-29dbb 8S/13E-laaa 8S/13E-7cca 8S/13E-llbdb 8S/13E-17dbd 8S/13E-19bad 8S/13E-20acd 8S/13E-20bdb 8S/13E-30aaa 8S/13E-32bdd 8S/13E-33cab 8S/13E-35bbc s> Si Si o CM l U St pH CO 00 co X) s> o CM 1 w >0 pH CO 00 8S/14E-31cbb s TJ <3 1 Id 00 co O' 9S/12E-ldaa 9S12E-3cbb 9S/12E-10ccc 84 _1/ Calculated values with bicarbonate recomputed as carbonate. Table 17.-- Chemical analyses of water from selected wells and springs --Continued > u 3 t/5 O o to D 0) XL (0