State Water Board Resolution 68-16, Statement of Policy with Respect to Maintaining High Quality of Waters in California, which prohibits a Discharger from reducing the quality of surface or groundwater even though such a reduction of water quality may not directly impact beneficial uses associated with the water body; and State Water Board Resolution 88-63, which specifies that except under specific defined exceptions, all surface and groundwater of the State are to be protected as existing or potential sources of municipal and domestic supply.

The area of the Proposed Action falls under the jurisdiction of the Central Valley RWQCB. Proposed Project aspects that are regulated by the RWQCB include: Impacts to surface waters from the erosion of soils disturbed during construction of the power transmission line, roads, and well pads; Accidents and spills of material and fuels transported to either project and/or off-site for disposal; Emissions of contaminants to air and their deposition upon the land or water (fallout). Monitoring of groundwater and surface water quality; Drill site waste management including mud sumps, test pits, fuel storage, etc.; and Pipeline leaks and breaks.

The Project Applicant would be required to submit a Report of Waste Discharge, and the Project would need the approval of the Central Valley RWQCB prior to discharging fluids to the sumps. Additional permits that may be required by the Central Valley RWQCB include: (a) Construction Stormwater NPDES permit during construction; (b) General Industrial Stormwater NPDES permit during operation, and (c) Fuel Storage permit for a single above ground tank over 660 gallons, or for multiple above ground tanks over 1,320 gallons cumulative. A Fuel Storage permit would include requirements for the development of a Spill Prevention Control and Countermeasure Plan.

Underground Injection Control Program: Injection of spent geothermal fluids into injection wells is regulated by the U.S. Environmental Protection Agency (EPA) consistent with Underground Injection Control (UIC) Program requirements. The UIC Program of the EPA is charged with the mission of protecting underground sources of drinking water (USDWs) by regulating injection practices (40 CFR §§144 and 146). The injection wells for the Proposed Action would be classified as Class V geothermal injection wells (40 CFR 146.5(e)(12)).

The EPA’s UIC Program would focus on several areas of concern to verify and document that the Project injection wells will not endanger USDWs (Written Communication to Randall Sharp, USFS/BLM from Karl Kanbergs, Federal Activities Office, EPA; March 13, 1998). The major areas of injection well requirements for protection of water sources, include mechanical integrity, area of review, financial responsibility, injection pressure limitations, and confining zone and related geology review (40 CFR 146).

The BLM acts on behalf of the EPA for permitting, monitoring, and ensuring proper construction and maintenance of injection wells. The BLM also permits and monitors geothermal production wells. General guidance for well drilling, completion, testing, and abandonment of geothermal wells is provided in Geothermal Resource Operational (GRO) Order Nos. 1 through 3 (see Section 1.7.2). In addition, Draft GRO Order No. 5 requires that a Plan of Injection or Disposal (POI) be prepared by a geothermal project applicant prior to the injection or disposal of geothermal effluent or associated byproducts. The POO for Utilization and Disposal submitted to the BLM by CEGC indicates that a detailed POI will be prepared and submitted to the BLM after injection well drilling and testing has been partially completed (CEGC 1997a). The BLM would require the Project Applicant to meet standard injection well procedures and requirements which would be incorporated into the injection well permits issued by the BLM (Personal Communication — Rich Estabrook, Petroleum Engineer, BLM, Ukiah, California; March 24, 1998). Injection well monitoring requirements typical of those which would be required are provided as Exhibit 6 to this EIS/EIR.

Clean Water Act: The Clean Water Act is a 1977 amendment to the 1972 Federal Water Pollution Control Act which set the groundwork for regulating pollutant discharges into U.S. waters. The Clean Water Act makes discharging pollutants from a point source to navigable waters illegal without a permit. The Clean Water Act amendments of 1977 were aimed at toxic pollutants. The Clean Water Act allows the EPA to delegate administrative and enforcement aspects of the law to state agencies. In the area of the Proposed Action, the Central Valley RWQCB administers and enforces the Clean Water Act.

Section 404 of the Clean Water Act establishes the federal authority to regulate activities in wetlands. Under Section 404, jointly administered by the U.S. Army Corps of Engineers and the EPA, the discharge of material into waters of the United States, including wetlands, requires a permit from the Corps based on regulations developed in conjunction with EPA (Section 404(b)(1) guidelines).

Modoc National Forest Land and Resource Management Plan: The Modoc National Forest Land and Resource Management Plan (LRMP) (USFS 1991) provides direction for implementing the Forest’s management practices and activities (see Section 1.7). The LRMP management direction that is specifically applicable to this Hydrologic and Geothermal Resources analysis, and potentially relevant to the proposed Project, includes the Water, Riparian Areas, Minerals, Geology, and Soils resource guidance provided in the Forest Standards and Guidelines, Management Prescriptions, and Management Area Direction sections of the LRMP.

3.2.2 Affected Environment

3.2.2.1 Study Area

The local study area for hydrologic and geothermal resources is the Medicine Lake basin within the caldera of the Medicine Lake Highlands and the area extending to the south of Payne Springs, Blanche Lake, and Bullseye Lake. For both hydrology and geothermal resources, the regional study area is the area bounded by Tule Lake to the north, the east flank of Mt. Shasta to the west, the Pit River to the south, and Tionesta to the east. The major geologic structural features and geologic map relevant to this hydrologic assessment and the approximate boundaries of the regional study area are shown on Figure 3.2.1. 3.2.2.2 Study Methods This description of the affected environment was compiled from a variety of sources including Baseline Hydrogeology Evaluation Report for Telephone Flat Geothermal Project, Medicine Lake, California (Weiss 1997; provided as Appendix A); published literature and unpublished reports, including Comparative Isotope Hydrology Study of Groundwater Sources and Transport in Three Cascade Volcanoes of Northern California (Davisson and Rose 1997) and Preliminary Chemical and Isotopic Data for Waters from Springs and Wells on and near Medicine Lake Volcano, Cascade Range, Northern California (Mariner et al. 1998; provided as Appendix B); communications with scientists who have studied the hydrologic and geothermal resources of the Medicine Lake area: Bob Mariner (USGS), Ross Denton (Mesquite Group), Lee Davisson (Lawrence Livermore National Laboratory), and Joe Iovenitti (Weiss Associates); and a site visit to the Medicine Lake Highlands and to the Fall River Springs area.

The description of the affected environment that follows is divided into four parts: Geothermal Resources, Local Surface Water, Local Groundwater, and Regional Hydrology.

3.2.2.3 Geothermal Resources

Material reviewed for the description of the affected environment for geothermal resources included the Weiss (1997) baseline hydrogeology evaluation for the proposed Project, published data on the Medicine Lake volcano and the geothermal resource, and proprietary subsurface data on file with the BLM.

The area of the Proposed Action is located within the Glass Mountain Known Geothermal Resource Area (KGRA). The geothermal resource potential of the Glass Mountain KGRA has been explored since the early 1980's and may have an electricity potential as high as 500 MW over a 30-year period (USFS and BLM 1984) 1. An additional geothermal power project has been proposed at Four Mile Hill, approximately 5 miles (8 km) northwest of the proposed power plant site.

A geothermal resource may be defined as a concentration in the natural heat of the earth, close enough to the surface that it can be extracted and utilized economically. In order for a geothermal resource to be a viable energy source, the following are required: shallow concentration of heat energy; a working fluid (steam or water) to bring the heat near to the surface for utilization; a permeable subsurface geothermal reservoir; and a lithologic and/or hydrothermal alteration seal around the reservoir.

All of these conditions are met in the Telephone Flat Project geothermal system. This geothermal system is a liquid-dominated, possibly two-phase (boiling liquid and vapor) hydrothermal system related to shallow and recent silicic intrusions (Donnelly-Nolan 1988). Geothermal reservoir characteristics for the Proposed Action, as reported by CEGC, are provided in Chapter 2 of this EIS/EIR (see Section 2.2.4.2 and Table 2.2.3).

The only surface manifestation of the geothermal activity in the Medicine Lake Highlands area is a pair of fumaroles known as the Hot Spot located approximately 2.5 miles (4 km) northeast of the proposed power plant site at the north edge of Glass Mountain. Weiss (1997) referenced a U.S. Geological Survey (USGS) study, Mariner (1997), in which gases from this Hot Spot were sampled and analyzed and found to consist of steam and very dilute amounts of carbon dioxide. This gas vent may result from meteoric water infiltrating and being conductively heated by the rocks of the geothermal system until vaporization occurs and the heated water vapor escapes (Weiss 1997).

Twenty-four intermediate depth temperature gradient holes and four exploration wells have been drilled in and around the area of the Proposed Action (Figure 3.2.2) to measure the temperature gradient and identify the lithology in the coreholes. The temperature gradient holes were drilled by Unocal, Phillips Petroleum, and Occidental Geothermal between 1981 and 1984. In 1984, Phillips Petroleum and Occidental Geothermal drilled a deep exploration well, GMF 17A-6. Unocal drilled three additional deep exploration wells between 1985 and 1989, GMF 31-17, GMF 87-13, and GMF 68-8. Well GMF 31-17 was deepened in 1991. In 1993, CEGC acquired all the geothermal rights held by Unocal in the Medicine Lake Highlands.

The 24 temperature gradient holes range in depth from 600 to 4,009 feet below ground surface (bgs) (183 to 1,222 m bgs). The four exploration wells range in depth from 3,110 to 9,619 feet bgs (948 to 2,932 m bgs). Three of the four exploration wells are productive; GMF 17A-6 is not.

Rocks in contact with geothermal fluids may have anomalously low resistivities due to changes caused by the hot water such as clay alteration or increased salinity. Geophysical methods such as Schlumberger soundings measure the electronic resistivity of rocks and can identify potential geothermal resource areas. Zohdy and Bisdorf (1990) conducted Schlumberger soundings within the Medicine Lake basin. Their results show shallow, low resistivity (high conductivity) anomalies near Medicine Lake and along the west, southwest, and eastern rim of the Medicine Lake basin. These resistivity anomalies are interpreted to be a composite of the thermal anomaly and the shallow groundwater in the area.

Figure 3.2.3 shows the elevation of the 100° F (38° C) isotherm based on data from the temperature gradient holes and exploration wells. This isotherm has been chosen as representative of the top of the Telephone Flat geothermal system (Weiss 1997). The elevation of the 100 F isotherm in the area of the Proposed Action is about 5,900 feet (about 1,800 m) which is approximately 1,000 feet bgs (about 300 m bgs). The Weiss (1997) hydrology baseline report lists in tabular form the depth and elevation of the 100° F temperature data for the temperature gradient holes and the exploration wells. Lithologic logs from temperature gradient holes and deep exploration wells indicate that a thick (up to 1,400-foot (427-m)) unit made up of rhyolite-dacite flows occurs throughout the Medicine Lake Basin starting at depths of 1,450 to 2,000 feet bgs (442 to 610 m bgs). Intense clay alteration coincides with the rhyolite-dacite unit. Together, the rhyolite-dacite unit and the hydrothermal alteration are known informally as the “capping rhyolite” and form the impermeable cap rock that prevents the upward movement of the geothermal fluid and is a necessary feature of any economically feasible geothermal resource. Figure 3.2.4 provides a generalized lithologic profile for well GMF 31-17, which shows this “capping rhyolite” in the Project wellfield. The occurrence of clay alteration at the top of the geothermal reservoir is widespread throughout Medicine Lake Highlands, having also been identified at the Four Mile Hill Geothermal Project (BLM et al. 1998). At Four Mile Hill, an 800- to 1,100-foot (244 to 335-m) sequence of extensively altered lithic tuff was observed in two different temperature gradient wells approximately 2 miles (3.2 km) apart. In both holes, the tuff exhibited highly impermeable formation conditions.

Further evidence for the impermeable cap rock that acts as a barrier to movement of geothermal fluids upward is found from the temperature gradient observed in temperature gradient holes. The temperature profiles are steep through the cap rock, indicating highly conductive rocks. Figure 3.2.4 shows the temperature gradient (temperature increase per unit of increasing depth) measured in GMF 31-17, a deep well drilled in the Project wellfield. The upper portion of the temperature gradient curve, above the “capping rhyolite,” is steep, with little increase in temperature with increasing depth. Steep temperature gradients such as this indicate that fluids are moving vertically through the rock, mixing and keeping temperatures relatively uniform. However, in the “capping rhyolite,” the temperature gradient increases substantially. This substantial increase in temperature with increasing depth indicates that there is little or no vertical movement of water through this sequence of rock, and that heat is being transferred through the rock by conduction, rather than through the movement of water by convection. Below the “capping rhyolite,” the temperature gradient curve begins to steepen again, which indicates that the geothermal reservoir, in which heat is again transferred vertically through the movement of water by convection, has been penetrated. Similar temperature gradient profiles are seen in the other Project wells and in the Fourmile Hill Project well (BLM et al. 1998).

The geochemistry of the geothermal fluid in the area of the Proposed Action has been analyzed. Table 3.2.1 shows the water chemistry from well 87-13 sampled in 1989 and in 1991 (Personal Communication — Dale R. Schuster, CEGC, September 17, 1997). In Table 3.2.1, both the analytical results reported by the laboratory and the flash corrected results are shown. The samples were collected after steam had been flashed away. For the 10/13/91 sample, the steam fraction was reported at 19.8 percent. For this sample, the flash corrections were made by dividing each concentration by 1.198 to account for the concentration that would have occurred pre-flash. These analyses show that the geothermal reservoir groundwater is enriched in silica, sodium, potassium, chloride, sulfide, boron, arsenic, and other trace elements relative to the surface water and shallow groundwater in Medicine Lake Basin.

Stable isotope signatures of the geothermal fluids at Medicine Lake have been measured. Weiss (1977) reported data from CEGC provided in Table 3.2.2 from two geothermal wells within the proposed Project wellfield. These waters, on a plot of delta deuterium versus delta oxygen-18 ( D vs. 18O), show a shift in delta oxygen-18 values away from the meteoric water line toward primary magmatic waters. This delta oxygen-18 shift, which is common in geothermal waters worldwide, indicates intermingling and exchange between meteoric water and hot igneous rocks (Taylor 1979).

Other thermal features within the region surrounding Medicine Lake Highlands include Little Hot Springs located at the southeastern edge of the Whitehorse Mountains, approximately 25 miles (40 km) southeast of Medicine Lake. Little Hot Springs occurs along northwest-southeast trending Basin and Range style faulting (Leivas et al. 1981) and is not related to the geothermal system at Medicine Lake Highlands (Weiss 1997).

Table 3.2.1: Geochemistry of the Geothermal Water from Well 87-13

Parameter (units)	Laboratory Results 10/13/91 samplea	Flash-Corrected Results 10/13/91 sample	Flash-Corrected Results 11/6/89 sampleb	Laboratory Limits of Detection
pH	8.5	8.5	8.6	NR
Conductivity (µmhos/cm)	3,600	3,005	NR	1.0
Total Dissolved Solids (mg/l)	2,800	2,337	NR	10
Alkalinity (as CaCO3): Total (mg/l) Bicarbonate (mg/l) Carbonate (mg/l)	100 33 70	83 28 58	NR 49 NR	10 10 10
Bromide (mg/l)	ND	ND	NR	10
Chloride (mg/l)	1,300	1,085	1,012.2	1.0
Sulfate (mg/l)	55	46	46.9	1.0
Fluoride (mg/l)	0.89	0.74	NR	0.1
Sulfide (mg/l)	2.4	2.0	NR	1.0
Nitrate, as N (mg/l)	ND	ND	NR	0.03
Total Phosphorus, as P (mg/l)	1.8	1.5	NR	0.02
Aluminum (mg/l)	0.71	0.59	NR	0.1
Antimony (mg/l)	ND	ND	NR	0.1
Arsenic (mg/l)	0.72	0.60	NR	0.005
Beryllium (mg/l)	ND	ND	NR	0.02
Boron (mg/l)	12	10	NR	0.1
Cadmium (mg/l)	ND	ND	NR	0.02
Calcium (mg/l)	5.2	4.3	7.9	0.5
Chromium (mg/l)	ND	ND	NR	0.02
Cobalt (mg/l)	ND	ND	NR	0.05
Iron (mg/l)	0.43	0.36	NR	0.05
Lead (mg/l)	ND	ND	NR	0.002
Lithium (mg/l)	2.6	2.2	3.1	0.1
Magnesium (mg/l)	ND	ND	0.1	0.5
Manganese (mg/l)	ND	ND	NR	0.02
Mercury (mg/l)	ND	ND	NR	0.0005
Molybdenum (mg/l)	ND	ND	NR	0.05
Nickel (mg/l)	ND	ND	NR	0.05
Potassium (mg/l)	92	77	107.7	0.5
Selenium (mg/l)	ND	ND	NR	0.005
Silica (mg/l)	530	442	582.3	0.1
Sodium (mg/l)	530	442	632.0	0.5
Strontium (mg/l)	0.03	0.025	NR	0.1
Thallium (mg/l)	ND	ND	NR	0.2
Vanadium (mg/l)	ND	ND	NR	0.05
Zinc (mg/l)	0.033	0.028	NR	0.02
ND = NOT DETECTED NR = NOT REPORTED a CEGC (written communication -Dale R. Schuster, CEGC, September 17, 1997) b BLM et al. 1995

Table 3.2.2: Stable Isotope Data From the Telephone Flat Project Geothermal Reservoir Fluid

Sample Number (Assigned by Weiss 1997)	Delta Oxygen-18 (per mil) ( 18O)	Delta Deuterium (per mil) ( D)
ML-88-50	-9.03	-94.82
ML-88-51	-8.81	-97.07
ML-88-52	-8.71	-94.31
ML-88-53	-8.37	-96.08
Source: Weiss 1997

3.2.2.4 Local Surface Water

The Medicine Lake Highlands area is notable for its general lack of permanent surface water drainages. The volcanic rocks that make up the Highlands are very permeable causing surface water to infiltrate below the surface before it travels very far. Permanent surface water features within the Medicine Lake Basin include four lakes (Medicine Lake, Little Medicine Lake, Bullseye Lake, and Blanche Lake); six springs or spring groups (Paynes Springs I, II, and III; Schonchin Spring; Crystal Spring; and an unnamed spring or spring group); and two perennial streams emanating from springs (Figure 3.2.5). The perennial stream associated with Crystal Springs flows into Medicine Lake. Paynes Creek is a perennial stream resulting from Paynes Springs I and II which flows for approximately 1.5 miles (2.5 km) and then disappears beneath the surface. There are also a number of small seasonal lakes and streams that occur annually, resulting from snow melt. Table 3.2.3 lists the permanent surface water features in Medicine Lake Basin and their elevations. There are no permanent lakes, springs, or streams within the proposed Project wellfield. Seasonal lakes within the Project wellfield include one in Alcohol Crater, one northwest of Alcohol Crater, and one at the southwest edge of Glass Mountain. The closest permanent surface water feature to the Project wellfield is Blanche Lake, approximately 2,500 feet (762 m) south of the southernmost proposed well pad (16-18/87-13).

Table 3.2.3: Elevation and Uses of Surface Water Features in the Medicine Lake Highlands

Surface Water Feature	Elevation	Surface Water Usesc
Medicine Lake	6,676 ft (2,035 m)a	Domestic Use, Recreation, Fish Habitat
Little Medicine Lake	6,682 ft (2,037 m)a	Recreation, Fish Habitat
Bullseye Lake	6,742 ft (2,055 m)a	Recreation, Fish Habitat
Blanche Lake	6,735 ft (2,053 m)a	Recreation
Paynes Spring I	6,558 ft (1,999 m)b	Paynes Creek: Recreation, Fish Habitat
Paynes Spring II	6,471 ft (1,972 m)b	Paynes Creek: Recreation, Fish Habitat
Paynes Spring III	6,678 ft (2,035 m)b	Seep Only — No Identified Use
Schonchin Spring	6,820 ft (2,079 m)b	Domestic Use
Crystal Spring	6,860 ft (2,091 m)b	Crystal Spring Creek: Domestic Use, Recreation, Fish Habitat
Unnamed (private) Spring	6,700 ft (2,042 m)b	No Identified Use
a USGS Topographic Map, 7.5 Minute series, Medicine Lake Quadrangle California, Siskiyou County, 1988 Provisional Edition b Schneider and McFarland 1996 c USFS and BLM 1994

Water quality of lakes in the Medicine Lake Basin has been monitored by the USFS (Medicine Lake, 1971-1986), by CEGC (Medicine Lake, Little Medicine Lake, Bullseye Lake, and Blanche Lake, 1984), and by the USGS (Medicine Lake, Little Medicine Lake, Bullseye Lake and Blanche Lake, 1992). Table 3.2.4 presents water quality analyses for Medicine Lake. The water quality is very good, with a low concentration of total dissolved solids (TDS). The USGS (Schneider and McFarland 1996) reported that Medicine Lake temperatures in September 1992 ranged from 57° F (14° C) at the surface to approximately 39° F (4° C) at depths greater than 70 feet (21 m). Dissolved oxygen concentrations in Medicine Lake were a constant 8 mg/l to a depth of 40 feet (12 m), then increased to 10.5 mg/l, and dropped to 7 mg/l at 80 feet (24 m). The pH was relatively constant with depth, between 6 and 7 (pH units). Specific conductance was relatively constant with depth at approximately 21 microsiemens per centimeter (µS/cm). The USFS reported that Medicine Lake had elevated levels of fecal coliform at sampling points adjacent to campgrounds and the public beach in 1982 and 1983. This was attributed to leaky vault toilets that were later replaced and fecal coliform concentrations were lowered in the Lake (USFS 1984). Water quality in Little Medicine Lake, Bullseye Lake, and Blanche Lake is presented in Table 3.2.5. All of the lakes have good water quality with TDS concentrations of 12-24 mg/l. The USGS (Schneider and McFarland 1996) reported that Little Medicine Lake has a maximum depth of 25 feet (8 m), and had temperatures ranging from 58-60° F (14.5-15.5° C), dissolved oxygen concentrations ranging from 7.2-8.3 mg/l, and pH ranging from 7.2-7.5 (pH units). Blanche Lake has a maximum depth of 1.5 feet (0.5 m) and had temperatures ranging from 62-64° F (16.9-17.9° C), dissolved oxygen concentrations ranging from 7.6-8.0 mg/l, pH ranging from 5.9-6.7 (pH units), and specific conductance ranging from 14-15 µS/cm (Schneider and McFarland 1996). Bullseye Lake has a maximum depth of 8.2 feet (2.5 m) and had temperatures ranging from 56-58° F (13.6-14.6° C), dissolved oxygen concentrations ranging from 7.5-8.5 mg/l, pH ranging from 6.9-7.0 (pH units), and specific conductance consistently at 15 µS/cm (Schneider and McFarland, 1996).

Table 3.2.4: Medicine Lake Water Quality Data

Parameter	1971-1972	1982	1983	1983	1983	1984	1986
Temp °F (°C)	32 -66 (0-19)	NR	NR	NR	NR	NR	NR
Dissolved Oxygen (mg/l)	5.0-11	6.7-8.8	NR	NR	5.4-7.7	6.4-7.9	6.3-7.2
pH (pH units)	6.7-7.4	7.1-7.9	5.7	NR	6.7-7.3	6.5-7.4	6.3-6.9
Turbidity (JTU)	0.14-3.0	0.2-0.4	NR	NR	0.2-1.0	0.3-0.4	0.2-0.3
Total Phosphorus (mg/l)	0.07	0.009-0.032	NR	NR	0.005-0.028	0.004-0.026	<0.04
Alkalinity (mg/l)	<17	0.2-10.2	NR	NR	5.4-6.3	5.4-6.2	6-7
Fecal Coliform (MPN/100 ml)	0-2	<2.2-110	NR	NR	<2.2->16.0	<3-4	<2
Secchi Disc Depth ((inches (cm))	NR	234-342 (594-869)	NR	NR	234-414 (594-1,052)	270-306 (686-777)	353-378 (897-960)
Calcium (mg/l)	NR	NR	1.1	<1.0	NR	NR	NR
Magnesium (mg/l)	NR	NR	0.44	<1.0	NR	NR	NR
Sodium (mg/l)	NR	NR	0.9	<1.0	NR	NR	NR
Potassium (mg/l)	NR	NR	0.5	<1.0	NR	NR	NR
Carbonate (mg/l)	NR	NR	0	NR	NR	NR	NR
Bicarbonate (mg/l)	NR	NR	3.5	NR	NR	NR	NR
Chloride (mg/l)	NR	NR	<1.8	1.9	NR	NR	NR
Sulfate (mg/l)	NR	NR	<5.0	1.3	NR	NR	NR
Nitrite + Nitrate as N (mg/l)	NR	NR	<0.4	<0.2	NR	<0.02-0.03	<0.20-0.29
Iron (mg/l)	NR	NR	0.08	NR	NR	NR	NR
Manganese (mg/l)	NR	NR	<0.01	NR	NR	NR	NR
Copper (mg/l)	NR	NR	<0.01	NR	NR	NR	NR
Total Dissolved Solids (mg/l)	NR	NR	10	8	NR	NR	NR
Boron (mg/l)	NR	NR	<0.01	NR	NR	NR	NR
Silica (mg/l)	NR	NR	4	5.4	NR	NR	NR
Specific Conductivity (µmhos/cm)	NR	NR	21	15	NR	NR	NR
Delta Oxygen 18	NR	NR	-9.85	NR	NR	NR	NR
Delta Deuterium	NR	NR	-82	NR	NR	NR	NR
Source:	USFS 1982a	USFS 1982b	Cosens-Gallinatti 1984	Cosens-Gallinatti 1984	USFS 1983	USFS 1984	USFS 1986
NR = Not Reported JTU = Jackson Turbidity Units, a measure of turbidly based on the amount of light-scattering caused by the water Secchi Disc Depth = a measure of water clarity

Table 3.2.5: Water Quality of Smaller Lakes in the Medicine Lake Basin

Parameter	Little Medicine Lake	Bullseye Lake	Blanche Lake
pH (pH units)	6.2	5.7	4.2
Calcium (mg/l)	2.4	1.2	1.2
Magnesium (mg/l)	0.7	0.4	0.44
Sodium (mg/l)	1.5	1	0.8
Potassium (mg/l)	0.6	0.4	0.2
Carbonate (mg/l)	0	0	0
Bicarbonate (mg/l)	10.4	3.5	0
Chloride (mg/l)	<1.8	<1.8	<2.1
Sulfate (mg/l)	<5.0	<5.0	<5.0
Nitrite + Nitrate as N (mg/l)	0.9	2.2	2.7
Iron (mg/l)	0.11	<0.05	0.07
Manganese (mg/l)	<0.01	<0.01	<0.01
Copper (mg/l)	<0.01	<0.01	<0.01
Total Dissolved Solids (mg/l)	24	12	14
Boron (mg/l)	<0.01	<0.01	<0.01
Silica (mg/l)	8	6	6
Specific Conductivity (µmhos/cm)	29	20	24
Delta Oxygen 18 (per mil)	-11.96	-11.32	-9.96
Delta Deuterium (per mil)	-92	-87	-84
Source:	Cosens-Gallinatti 1984	Cosens-Gallinatti 1984	Cosens-Gallinatti 1984

Water quality analyses for Schonchin Spring, Crystal Spring, Paynes Spring I, and Paynes Spring II are shown in Table 3.2.6. Water quality analyses were collected by CEGC and by EMA/WESTEC (WESTEC 1997; provided as Appendix C). The springs have good water quality with TDS concentrations ranging from 43 to 88 mg/l. Stable isotope data, delta oxygen-18 ( 18O) and delta deuterium ( D), are presented for the springs, with data collected by CEGC, Lawrence Livermore Laboratory, and EMA. The oxygen and deuterium ratios fall on the meteoric water line on a plot of delta deuterium vs. delta oxygen-18 indicating that meteoric water is the source of water in these springs. Flow rates of springs in the Medicine Lake basin are presented in Table 3.2.7. Different locations are listed for Paynes Springs II and III by two different investigators, and different sampling locations below the springs are described for Paynes Springs I and II.

Table 3.2.6: Water Quality of Springs in the Medicine Lake Basin

Parameter	Schonchin Spring	Schonchin Spring	Crystal Spring	Crystal Spring	Paynes Spring #1	Paynes Spring #1	Paynes Spring #1	Paynes Spring #2	Paynes Spring #2	Paynes Spring #2	Paynes Springs
pH (pH units)	6.7	NR	6.6	NR	6.6	7.6	7.6	6.1	7.5	7.5	NR
Calcium (mg/l)	8.6	NR	3.9	NR	3.1	NA	5.1	4.6	NA	4.8	4.1
Magnesium (mg/l)	2	NR	1.1	NR	1	2.4	NA	1.5	1.8	NA	2.8
Sodium (mg/l)	3.1	NR	2.3	NR	2.1	NA	3.8	3.4	NA	2.8	3.8
Potassium (mg/l)	1	NR	0.8	NR	1	NA	1.2	1.8	NA	1.1	3
Carbonate (mg/l)	0	NR	0	NR	0	NA	NA	0	NA	NA	NR
Bicarbonate (mg/l)	41.6	NR	20.8	NR	17.3	NA	NA	23.4	NA	NA	NR
Chloride (mg/l)	<1.8	NR	<1.8	NR	<1.8	2.0	0.32	<1.8	2.0	0.26	0.5
Sulfate (mg/l)	<5.0	NR	<5.0	NR	<5.0	<1.0	0.74	6	<1.0	0.40	<1.0
Nitrate as N (mg/l)	<0.04	NR	<0.4	NR	<0.04	0.20	NA	2.2	0.27	NA	<0.2
Iron (mg/l)	<0.05	NR	<0.05	NR	<0.05	0.028	NA	<0.05	0.026	NA	NR
Manganese (mg/l)	<0.01	NR	<0.01	NR	<0.01	<0.010	NA	<0.010	<0.010	NA	NR
Copper (mg/l)	<0.01	NR	<0.01	NR	<0.01	<0.010	NA	<0.010	<0.010	NA	NR
Total Dissolved Solids (mg/l)	88	NR	57	NR	54	74	87	85	59	92	43
Boron (mg/l)	<0.01	NR	0.03	NR	<0.01	<0.10	<0.10	<0.10	<0.10	<0.10	NR
Aluminum (mg/l)	NR	NR	NR	NR	NR	<0.010	NA	NR	<0.010	NA	NR
Antimony (mg/l)	NR	NR	NR	NR	NR	<0.0050	NA	NR	<0.0050	NA	NR
Beryllium (mg/l)	NR	NR	NR	NR	NR	<0.0010	NA	NR	<0.0010	NA	NR
Nickel (mg/l)	NR	NR	NR	NR	NR	<0.040	NA	NR	<0.040	NA	NR
Arsenic (mg/l)	NR	NR	NR	NR	NR	<0.0050	<0.10	NR	<0.0050	<0.10	NR
Barium (mg/l)	NR	NR	NR	NR	NR	<0.10	NA	NR	<0.10	NA	NR
Cadmium (mg/l)	NR	NR	NR	NR	NR	<0.0010	NA	NR	<0.0010	NA	NR
Chromium (mg/l)	NR	NR	NR	NR	NR	<0.010	NA	NR	<0.010	NA	NR
Lead (mg/l)	NR	NR	NR	NR	NR	<0.0050	NA	NR	<0.0050	NA	NR
Selenium (mg/l)	NR	NR	NR	NR	NR	<0.0050	NA	NR	<0.0050	NA	NR
Silver (mg/l)	NR	NR	NR	NR	NR	<0.010	NA	NR	<0.0010	NA	NR
Thallium (mg/l)	NR	NR	NR	NR	NR	<0.0050	NA	NR	<0.0050	NA	NR
Zinc (mg/l)	NR	NR	NR	NR	NR	<0.010	NA	NR	<0.010	NA	NR
Mercury (mg/l)	NR	NR	NR	NR	NR	<0.00020	<0.00020	NR	<0.00020	<0.00020	NR
Fluoride (mg/l)	NR	NR	NR	NR	NR	0.27	NA	NR	0.22	NA	NR
Silica (mg/l)	32	NR	28	NR	29	43	35	42	30	32	42
Specific Conductivity (µmhos/cm)	77	NR	44	NR	40	74	63	60	64	53	63
Delta Oxygen 18 (per mil)	-13.55	-13.7	-13.88	-13.7	-13.48	-13.4	NA	-13.77	-13.5	NA	NR
Delta Deuterium (per mil)	-99	-97	-98	-98	-99	-97	NA	-102	-95	NA	NR
Source:	Cosens- Gallinatti 1984	Davisson and Rose 1997	Cosens- Gallinatti 1984	Davisson and Rose 1997	Cosens- Gallinatti 1984	WESTEC (8-8-97)	WESTEC (10-16-97)	Cosens-Gallinatti 1984	WESTEC (8-8-97)	WESTEC (10-16-97)	Weiss 1997
NA = Not Analyzed NR = Not Reported

Table 3.2.7: Flow Rates of Springs in Medicine Lake Basin

Spring Name	Location	Flow Rate (gpm)	Date	Comments	Source
Schonchin	T43N,R3E,S3cdc	Dry	9-15-92		Schneider and McFarland 1996
Private (Latunich)	T43N,R3E,S10acb	28.7	9-15-92	Measurement made approximately 600 ft (183 m) downstream and approximately 100 ft (30 m) from lake edge	Schneider and McFarland 1996
Crystal	T43N,R3E,S15abd	3.4	6-2-92		Schneider and McFarland 1996
Paynes Spring I	T43N,R4E,S19bca	75.4	9-16-92	Measurement made 600 ft (183 m) downstream on west fork of Paynes Creek	Schneider and McFarland 1996
Paynes Spring I	T43N,R4E,S19bca	48.1	8-8-97	Measurement made approximately 50 ft (15 m) from the source	WESTEC 1997
Paynes Spring I	T43N,R4E,S19bca	2.3	10-16-97	Measurement made approximately 50 ft (15 m) from the source	WESTEC 1997
Paynes Spring II	T43N,R4E,S19bdb	23.3	9-16-92	Measurement made in small channel about 15 ft (5 m) from orifice	Schneider and McFarland 1996
Paynes Spring II	T43N,R4E,S18cdc	>65.4	8-8-97	Measurement made approximately 50 ft (15 m) from the source	WESTEC 1997
Paynes Spring II	T43N,R4E,S18cdc	33.9	10-16-97	Measurement made approximately 50 ft (15 m) from the source	WESTEC 1997
Paynes Spring III	T43N,R4E,S18cdcc	Seeps only	9-16-92		Schneider and McFarland 1996
Paynes Spring III	T43N,R4E,S18cca	Seeps only	8-8-97		WESTEC 1997