RESULTS AND INTERPRETATION OF PRELIMINARY AQUIFER TESTS IN BOREHOLES UE-25c #1, UE-25C #2, AND UE-25c #3, YUCCA MOUNTAIN, NYE COUNTY, NEVADA by Arthur L. Geldon U.S. GEOLOGICAL SURVEY Water-Resources Investigations Report 94-4177 Prepared in cooperation with the U.S. DEPARTMENT OF ENERGY, NEVADA FIELD OFFICE, under Interagency Agreement DE-AI08-92NV10874 Denver, Colorado 1996
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RESULTS AND INTERPRETATION OF PRELIMINARY AQUIFER TESTS IN BOREHOLES UE-25c #1, UE-25C #2, AND UE-25c #3, YUCCA MOUNTAIN, NYE COUNTY, NEVADA
by Arthur L. Geldon
U.S. GEOLOGICAL SURVEY
Water-Resources Investigations Report 94-4177
Prepared in cooperation with the
U.S. DEPARTMENT OF ENERGY,
NEVADA FIELD OFFICE, under
Interagency Agreement DE-AI08-92NV10874
Denver, Colorado 1996
U.S. DEPARTMENT OF THE INTERIOR
BRUCE BABBITT, Secretary
U.S. GEOLOGICAL SURVEY
Gordon P. Eaton, Director
The use of trade, product, industry, or firm names is for descriptive purposes only and does not imply endorsement by the U.S. Government.
For additional information write to: Copies of this report can be purchased from:Chief, Earth Science Investigations U.S. Geological SurveyProgram USGS Information ServicesYucca Mountain Project Branch Open-File Reports SectionU.S. Geological Survey Box 25286, MS 517Box 25046, MS 421 Denver Federal CenterDenver Federal Center Denver, CO 80225Denver, CO 80225
CONTENTS
Abstract................................................................................................................................................................................. 1Introduction........................................................................................................................................................................... 1
Purpose and scope....................................................................................................................................................... 1Acknowledgments.................................................................................»^ 2
Physical setting ..................................................................................................................................................................... 2Borehole construction................................................................................................................................................. 2Site geology.....................................................................................................................................................^ 7
Site hydrology..................................................................................................................................................^ 9Matrix permeability..................................................................................................................................................... 9Heat-pulse flowmeter surveys..................................................................................................................................... 12Transmissive intervals................................................................................................................................................. 13
Calico Hills Aquifer.......................................................................................................................................... 13Prow Pass - Upper Bullfrog Aquifer................................................................................................................. 20Bullfrog Aquifer.....................................» 20TramAquifer.........................................^ 20
Fluid-injection tests............................................................................................................................................................... 20Falling-head tests ........................................................................................................................................................ 21Pressure-injection tests................................................................................................................................................ 24
Constant-flux tests.................................................................................................^^ 35Analytical methods..................................................................................................................................................... 39Pumping tests in borehole UE-25c #1......................................................................................................................... 42Pumping test in borehole UE-25c #2.......................................................................................................................... 43
Procedures and problems.................................................................................................................................. 43Test analyses..................................................................................................................................................... 44
First pumping test in borehole UE-25c #3.................................................................................................................. 48Procedures and problems.................................................................................................................................. 48Test analyses...................................................................................................................................................... 51
Injection test in borehole UE-25c #2.......................................................................................................................... 58Second pumping test in borehole UE-25c #3.............................................................................................................. 61
Procedures and problems.................................................................................................................................. 61Test analyses...................................................................................................................................................... 64
Summary and conclusions .................................................................................................................................................... 69Selected references......................................................................................................_^ 71Supplementary data............................................................................................................................................................... 73
PLATES
[In pocket]
1-3. Charts showing:1. Indicators of transmissive intervals in borehole UE-25c #1, Yucca Mountain, Nye County, Nevada2. Indicators of transmissive intervals in borehole UE-25c #2, Yucca Mountain, Nye County, Nevada3. Indicators of transmissive intervals in borehole UE-25c #3, Yucca Mountain, Nye County, Nevada
CONTENTS III
FIGURES
1. Map showing location of Yucca Mountain, boreholes UE-25c #1, UE-25c #2, and UE-25c #3, andnearby boreholes used for hydrologic investigations............................................................................................ 5
2. Map showing surface location and drift of boreholes UE-25c #1, UE-25c #2, and UE-25c #3........................... 63. Diagram showing relation between fractures and borehole diameter in an enlarged, rugose interval
of borehole UE-25c #2.......................................................................................................................................... 74-6. Plots showing:
4. Frequency distribution of fracture orientations in boreholes UE-25c #1, UE-25c #2, and UE-25c #3...... 105. Horizontal matrix permeability in the tuffs and lavas of Calico Hills and Crater Flat Tuff, east-
central Yucca Mountain area, as a function of depth within geologic units............................................... 116. Relation of vertical to horizontal matrix permeability in core samples from the tuffs and lavas
of Calico Hills and Crater Flat Tuff in the c-holes and nearby boreholes.................................................. 127. Hydrogeologic section of the c-hole complex....................................................................................................... 188. Sketch showing design configuration of falling-head tests in borehole UE-25c #1, October 1983...................... 23
9-15. Plots showing:9. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite,
homogeneous, isotropic, confined aquifer.................................................................................................. 2510. Falling-head tests and transmissivity values obtained in relation to geology, borehole UE-25c #1.......... 3311. Analyses of pressure-injection tests conducted in borehole UE-25c # 1, October 1983, assuming
an infinite, homogeneous, isotropic, confined aquifer................................................................................ 3612. Transmissivity and hydraulic conductivity distributions within a small radius of borehole UE-25c #1,
estimated from falling-head and pressure-injection tests........................................................................... 3813. Drawdown as a function of time in borehole UE-25c #2 during the pumping test in borehole
UE-25c #2, March 1984............................................................................................................................. 4514. Drawdown as a function of time in boreholes UE-25c #1 and UE-25p #1 during the pumping test in
borehole UE-25c #2, March 1984.............................................................................................................. 4515. Atmospheric pressure at borehole USW H-4 during the pumping test in borehole UE-25c #2,
March 1984........................................................._ 4516-29. Plots showing:
16. Analytical solution for drawdown data from borehole UE-25c #1 above the packers assuming afissure-block aquifer, pumping test in borehole UE-25c #2, March 1984.................................................. 46
17. Analytical solutions for drawdown and recovery data from borehole UE-25c #1 above the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25 c #1, March 1984............................................................................................................................ 48
18. Drawdown as a function of time during the pumping test in borehole UE-25c #3, May to June 1984:(A), borehole UE-25c #3; (B), borehole UE-25c #2 .................................................................................. 50
19. Drawdown as a function of time in borehole UE-25c #1 during the pumping test in boreholeUE-25c #3, May to June 1984: (A), above the packers; (B), between the packers................................... 51
20. Analytical solution for residual drawdown data from borehole UE-25c #3 assuming an infinite,homogeneous, isotropic, confined aquifer, pumping test in borehole UE-25c #3, May to June 1984....... 52
21. Analytical solution for drawdown data from borehole UE-25c #3 assuming an infinite, homogeneous, isotropic, confined aquifer with leakage from a confining unit without storage, pumping test in borehole UE-25c #3, May to June 1984..................................................................................................... 53
22. Analytical solution for drawdown data from borehole UE-25c #2 assuming a fissure-block aquifer,pumping test in borehole UE-25c #3, May to June 1984........................................................................... 53
23. Analytical solution for drawdown data from borehole UE-25c #2 assuming an infinite, homogeneous,anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, May to June 1984 ....................... 56
24. Analytical solution for drawdown data from borehole UE-25c #1 above the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, May to June 1984........................................................................................................................................ 57
25. Analytical solution for recovery data from borehole UE-25c #1 between the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, May to June 1984........................................................................................................................................ 57
IV CONTENTS
26. Water-level changes in borehole UE-25c #2 during and after injection of water between packerson October 30,1984................................................................................................................................... 59
27. Water-level changes in boreholes UE-25c #1 and UE-25c #3 in response to injection of water intoborehole UE-25c #2, October 30,1984...................................................................................................... 60
28. Atmospheric pressure at borehole USW H-4 during the pumping test in borehole UE-25c #3,October to December 1984......................................................................................................................... 62
29. Drawdown as a function of time in borehole UE-25c #3 during the pumping test in boreholeUE-25c #3, October to December 1984..................................................................................................... 62
30-35. Plots showing:30. Drawdown as a function of time in borehole UE-25c #1 during the pumping test in borehole
UE-25c #3, October to December 1984..................................................................................................... 6331. Drawdown as a function of time in borehole UE-25c #2 between the packers during the pumping
test in borehole UE-25c #3, October to December 1984, with residual drawdown from a preceding injection test subtracted.............................................................................................................................. 63
32. Analytical solution for drawdown data from borehole UE-25c #1 above the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, October to December 1984......................................................................................................................... 65
33. Analytical solution for recovery data from borehole UE-25c #1 between the packers assuming an infinite, homogeneous, isotropic, confined aquifer, pumping test in borehole UE-25c #3, October to December 1984........................................................................................................................................... 67
34. Analytical solution for recovery data from borehole UE-25c #2 between the packers assuming an infinite, homogeneous, isotropic, confined aquifer, pumping test in borehole UE-25c #3, October to December 1984........................................................................................................................................... 68
35. Analytical solution for drawdown data from borehole UE-25c #1 below the packers assuming aninfinite, homogeneous, isotropic, confined aquifer with leakage from a confining unit without storage, pumping test in borehole UE-25c #3, October to December 1984............................................................. 68
TABLES
1. Information collected at the c-hole complex for determination of rock hydrologic properties................................ 32. Distances between pumped wells and monitored intervals in observation wells during some pumping tests
conducted in 1984 in boreholes UE-25c #2 and UE-25c #3..................................................................................... 63. Stratigraphic column for the c-hole complex............................................................................................................ 84. Transmissive intervals in borehole UE-25c #1......................................................................................................... 145. Transmissive intervals in borehole UE-25c #2......................................................................................................... 156. Transmissive intervals in borehole UE-25c #3......................................................................................................... 167. Results of falling-head tests conducted in borehole UE-25c #1, October 6-12,1983............................................. 228. Results of pressure-injection tests conducted in borehole UE-25c #1, October 6-12,1983.................................... 349. Summary of analyses of 1984 constant-flux aquifer tests in boreholes UE-25c #1, UE-25c #2, and UE-25c #3.... 70
10. Summary of information from lithologic, television, acoustic televiewer, caliper, and temperature logsfor borehole UE-25c#l..........................................^ 74
11. Summary of information from lithologic, television, acoustic televiewer, caliper, and temperature logsfor borehole UE-25c^..................................................^ 89
12. Summary of information from lithologic, television, acoustic televiewer, caliper, and temperature logsfor borehole UE-25c #3............................................................................................................................................. 108
CONTENTS
CONVERSION FACTORS AND VERTICAL DATUM
Multiply inch-pound unit By To obtain metric unit
cubic foot per day (ft3/d)foot
foot per day (ft/d)foot squared per day (ft2/d)
gallon (gal)gallon per minute (gal/min)
inch (in.)inch of mercury (in. of mercury)
milemillidarcy (mD)
minute per square foot (mm/ft2)pound per square inch (lb/in.2)
reciprocal foot (ft" 1 )square foot (ft2)
2.832 X lO'2.3048.3048
9.290 X 10-23.78546.309 X 10'22.54
.34531.60939.87 X 10' 12
10.766.8953.28089.290 X 10'2
cubic meter per daymetermeter per daymeter squared per dayliterliter per secondcentimetermeter of waterkilometersquare centimeterminute per square meterKilopascalreciprocal metersquare meter
Degree Fahrenheit (°F) may be converted to degree Celsius (°C) by using the following equation:°C = 5/9(°F-32).
Sea level: Altitudes in this report are referenced to the National Geodetic Vertical Datum of 1929 (NGVD of 1929), a geodetic datum derived from a general adjustment of the first-order level nets of the United States and Canada, formerly called the Sea Level Datum of 1929.
VI CONTENTS
Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
By Arthur L. Geldon
Abstract
Pumping and injection tests conducted in 1983 and 1984 in boreholes UE-25c #1, UE-25c #2, and UE-25c #3 (the c-holes) at Yucca Mountain, Nevada, were analyzed with respect to information obtained from lithologic and borehole geophysical logs, core permeameter tests, and borehole flow surveys. The three closely spaced c-holes, each of which is about 3,000 feet deep, are completed mainly in nonwelded to densely welded, ash-flow tuff of the tuffs and lavas of Calico Hills and the Crater Flat Tuff of Miocene age. Below the water table, tectonic and cooling fractures pervade the tuffaceous rocks but are dis tributed mainly in 11 transmissive intervals, many of which also have matrix permeability. Although steep to vertical, south-striking (west dipping) fractures predominate in rocks penetrated by the c-holes, fractures in transmissive intervals gener ally are oriented diversely. From the water table, at depths between 1,312 and 1,320 feet, to a depth of 1,700 feet, transmissive intervals are uncon- fined; transmissive intervals between 1,800 and 2,700 feet respond to pumping as fissure-block or nonleaky, confined aquifers; below 2,700 feet, transmissive intervals are recharged by water released from faults that have offset and brecciated the rocks in these intervals. Miocene tuffaceous rocks and Paleozoic carbonate rocks at the c-hole complex appear to be connected hydraulically.
Heat-pulse flowmeter surveys indicate a change from generally small, downward to large, upward flow with depth, that is disrupted by pumping. Flow from unconfined to confined inter vals occurs in response to hydraulic gradients established during pumping tests. Diverse aquifer tests consistently indicate layered heterogeneity and the dependence of calculated hydrologic prop erties on the volume of aquifer being tested. For
the entire thickness of rocks penetrated by the test holes, cross-hole pumping and injection tests indicated transmissivity between 20,000 and 35,000 feet squared per day; storativity between 0.002 and 0.004; horizontal hydraulic conductivity between 30 and 40 feet per day; and vertical hydraulic conductivity between 2 and 5 feet per day.
INTRODUCTION
Information contained in this report is presented as part of ongoing investigations by the U.S. Geologi cal Survey (USGS) regarding the hydrologic and geo logic suitability of Yucca Mountain, Nevada, as a potential site for the storage of high-level nuclear waste in an underground mined geologic repository. This investigation was conducted in cooperation with the U.S. Department of Energy under Interagency Agree ment DE-AI08-78ET44802, as part of the Yucca Mountain Site Characterization Project.
Purpose and Scope
This report presents previously unpublished syn theses of geologic and hydrologic data from boreholes UE-25c #1, UE-25c #2, and UE-25c #3 (collectively called the c-holes) and descriptions, analyses, and interpretations of fluid-injection and withdrawal tests conducted in the c-holes. These tests were conducted between September 1983 and December 1984 to (1) help develop a conceptual model of the ground- water system at the c-hole complex; (2) provide a range in hydrologic properties for the rocks in tested intervals based on multiple analytical solutions applied to aqui fer test data; and (3) provide information for designing hydraulic-stress tests and tracer tests within constraints imposed by initial test analyses. Analysis and interpre tation of the preliminary aquifer tests at the c-holes were aided by published and unpublished data obtained between April 1985 and December 1992 that are listed
Abstract 1
in table 1. Interpretations presented in this report should be considered tentative and subject to change, as optimally designed hydraulic-stress and tracer tests are conducted and analyzed. This report updates some hydrogeologic information and corrects some errone ous information about aquifer tests in U.S. Geological Survey Water-Resources Investigations Report 92-4016 (Geldon, 1993).
Acknowledgments
The author is indebted to many people currently or formerly with the USGS and Fenix and Scisson, Inc., who assisted with data collection, pro cessing, and analysis, including but not limited to: Richard K. Waddell, Jr., James R. Erickson, Devin L. Galloway, Michael P. Chornack, Charles T. Warren, David H. Lobmeyer, Robert W Craig, John B. Czarnecki, Brent Anderson, Jack Kume, William J. Oatfield, Charles S. Washington, and Geoffrey Miller (USGS); Robin L. Reed, Byron W. Cork, Sandy Waddell, Eric P. Eshom, Jennifer B. Warner, Daniel O. Blout, Kirstin A. Johnson, Lynn D. Panish, Heather Huckins, Thomas M. Howard, Eric Larsen, and Russell G. Lahoud (Fenix and Scisson, Inc.).
PHYSICAL SETTING
Boreholes UE-25c #1, UE-25c #2, and UE-25c #3 are located in Nye County, Nevada, just east of the western boundary of the Nevada Test Site, approximately 90 miles northwest of Las Vegas. The c-holes are in the channel of an ephemeral stream that cuts through Bow Ridge parallel to and east of the main part of Yucca Mountain. The c-holes, other boreholes referred to in this report, and the potential high-level nuclear waste repository site are shown in figure 1. Yucca Mountain is situated in the arid Basin and Range physiographic province of the southwestern United States. Typical of the Basin and Range, the area around Yucca Mountain is characterized by narrow, predomi nantly northerly aligned mountain ranges separated by broad, alluvial basins (Frizzell and Shulters, 1990).
Borehole Construction
Boreholes UE-25c #1, UE-25c #2, and UE-25c #3 are 100 to 251 ft apart at the land surface (fig. 2). Lines connecting the boreholes delineate a tri angle with an area of 11,050 ft2. Because of borehole drift during drilling (fig. 2), interborehole distances at
depth vary substantially from distances at the surface. For example, average horizontal distances between intervals monitored in some of the pumping tests con ducted in the c-holes range from 92 to 280 ft (table 2). Cumulative borehole drift in a vertical plane for each of the c-holes was less than a foot. As a result, measured depths to features within the c-holes did not require a true-depth correction for the purposes of this report.
Borehole UE-25c #1 was completed in September 1983 (Fenix and Scisson, Inc., 1986). The top of the borehole is at an altitude of 3,709.28 ft (Grady O'Brien, U.S. Geological Survey, written com- mun., 1993). As indicated by television (TV) and cal- iper logs listed in table 1, casing and concrete extend 1,371 ft below the top of the borehole. The open part of the borehole was rotary-drilled with a 14.75-in.- diameter bit through the bottom of the concrete to a depth of 1,511 ft and a 9.875-in.-diameter bit from 1,511 to 2,990 ft. The borehole was cored with an 8.75-in.-diameter bit from 2,990 to 3,000 ft. Caliper logs indicate that the borehole walls are very irregular (plate 1). TV and caliper logs indicate that the bottom of the borehole has collapsed substantially since the borehole was completed. The bottom of the borehole was at a depth of 2,994 ft in September 1983,2,962 ft in November 1983, and 2,945 ft in December 1990.
Borehole UE-25c #2 was completed in February 1984 (Fenix and Scisson, Inc., 1986). The top of the borehole is at an altitude of 3,715.25 ft (Grady O'Brien, U.S. Geological Survey, written com- mun., 1993). As indicated by TV and caliper logs listed in table 1, casing and concrete extend 1,365 ft below the top of the borehole. The open part of the borehole was rotary-drilled with a 14.75-in.-diameter bit through the bottom of the concrete to a depth of 1,515 ft and a 9.875-in.-diameter bit from 1,515 to 3,000 ft. Caliper logs indicate that the borehole walls are very irregular (pi. 2). In figure 3, a close relation ship is shown between the location of open, near verti cal to vertical (dip 70°-84°), southerly and northwesterly striking fractures and an enlarged, rug ose section of borehole UE-25c #2. TV and acoustic televiewer logs in the c-holes indicate that prominent fractures with other orientations, partings at contacts between geologic units, and drilling-induced slough ing, also, are associated with enlargement and rugosity in the c-holes. TV and caliper logs indicate that the bottom of borehole UE-25c #2 has collapsed slightly since completion. The bottom of the borehole was at a depth of 2,999 ft in February 1984,2,990 ft in August 1984, and 2,986 ft in June 1992.
Borehole UE-25c #3 was completed in April 1984 (Fenix and Scisson, Inc., 1986). The top of the borehole is at an altitude of 3,715.25 ft
Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
Table 1. Information collected at the c-hole complex for determination of rock hydrologic properties1
Information Source Dates obtained
Caliper logs
Gyroscopic (borehole deviation) surveyResistivity logsTemperature logs (nonpumping)
Miscellaneous geophysical logsTracejector survey (pumping)Television logsAcoustic televiewer logLithologic logCore permeability analyses (9)Pumping tests (2)Falling-head (slug) tests (16)Pressure-injection tests (9)Heat-pulse flowmeter survey (nonpumping)Static water levels, atmospheric pressure, andbarometric efficiencyBorehole history
Caliper logs
Gyroscopic (borehole deviation) surveyResistivity logsTemperature logs (nonpumping)
Miscellaneous geophysical logs Tracejector survey (pumping) Television logs
Acoustic televiewer logs
Lithologic logCore permeability analyses (3)Pumping testConstant-flux injection testHeat-pulse flowmeter survey (nonpumping)Static water levels, atmospheric pressure and barometric efficiency Borehole history
Borehole UE-25c #1BirdwellAtlas Wireline ServicesUSGSEastmanBirdwellBirdwellUSGSNelson and others (1991)Gearhart-OwenWestechRichard K. Waddell (USGS, written commun., 1984)Richard E. Spengler (USGS, written commun., 1984)Holmes and Narver, Inc.USGS, assisted by REECoUSGS, assisted by TAM InternationalUSGS, assisted by TAM InternationalFrederick L. Paillet (USGS, written commun., 1992)Galloway and Rojstaczer (1988)
Fenix and Scisson, Inc. (1986)
Borehole UE-25c #2BirdwellBirdwellAtlas Wireline ServicesUSGSSperry-SunBirdwellBirdwellUSGSNelson and others (1991)Gearhart-OwenWestechBarbour Well Surveying CorporationRichard K. Waddell (USGS, written commun., 1984)USGSRichard E. Spengler (USGS, written commun., 1984)Alan L. Flint (USGS, written commun., 1993)USGS, assisted by REECoUSGS, assisted by REECoFrederick L. Paillet (USGS, written commun., 1992)Galloway and Rojstaczer (1988)
Fenix and Scisson, Inc. (1986)
09/18/8312/11/9012/10/9109/18/8309/20/8309/20/8312/09/91
08/21/83-11/20/8309/29/83
09/17/83-11/18/8310/31/83
2/8403/14/84
09/27/83-10/02/83 10/06/83-10/12/83 10/08/83-10/12/83
12/12/91 02/23/86-04/21/86
08/10/83-02/01/85
02/28/8408/23/8412/11/9012/14/9102/27/8402/28/8402/28/8412/14/91
01/27/84-02/29/8403/12/84
02/08/84-04/13/8406/02/9202/27/8412/14/91
03/84 12/92
03/07/84-03/18/8410/30/8412/16/91
02/23/86-04/21/86
01/09/84-06/27/85
PHYSICAL SETTING
Table 1. Information collected at the c-hole complex for determination of rock hydrologic properties1 -Continued
Information Source Dates obtained
Caliper logs
Gyroscopic (borehole deviation) surveyResistivity logsTemperature logs (nonpumping)
Miscellaneous geophysical logs Tracejector survey (pumping) Television logs
Acoustic televiewer logs
Lithologic logCore permeability analyses (8)Pumping tests
First testSecond test
Heat-pulse flowmeter survey (nonpumping) Static water levels, atmospheric pressure and barometric efficiency Borehole history
Borehole UE-25c #3BirdwellBirdwellAtlas Wireline ServicesUSGSSpeny-SunBirdwellBirdwellUSGSNelson and others (1991)Gearhart-OwenWestechBarbour Well Surveying CorporationRichard K. Waddell (USGS, written commun., 1984)USGSRichard E. Spengler (USGS, written commun., 1984)Alan L. Flint (USGS, written commun., 1993)
USGS, assisted by REECoUSGS, assisted by REECoFrederick L. Paillet (USGS, written commun., 1992)Galloway and Rojstaczer (1988)
Fenix and Scisson, Inc. (1986)
04/27/84 03/21/85 12/11/90 12/13/91 04/26/84 04/30/84 04/30/84 12/31/91
03/28/84-04/30/8405/07/8404/13/8406/02/9204/27/8412/13/91
05/8412/92
05/14/84-06/12/84 10/30/84-12/09/84
12/15/91 02/23/86-04/21/86
03/20/84-06/27/85
Core permeability analyses UE-25b#l(12) USW H-l (15) USW G-3 (22) USW G-4 (20)
Boreholes near the c-holes
Lobmeyer and others (1983)Rush and others (1983)Philip Nelson (USGS, written commun., 1992)Philip Nelson (USGS, written commun., 1992)
unknown unknown unknown unknown
Any use of trade names in this report is for descriptive purposes only and does not imply endorsement by the U.S. Geological Survey.
Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
37°00'116030' 116°22'30"
36°45'
UE-25c#1, UE-25c #2, UE-25c #3
Potential Repository Site
CRATER FLAT
NEVADA TEST SITE BOUNDARY
Amargosa Valley
AMARGOSA DESERT
\10 KILOMETERS
10 MILESI
Figure 1. Location of Yucca Mountain, boreholes UE-25c #1, UE-25c #2, and UE-25c #3, and nearby boreholes used for hydrologic investigations.
PHYSICAL SETTING
N757J50
N757JOO
N757.050
N757,000
N756,950
N756,900
N756.850
N756,800
SURFACE LOCATION OF BOREHOLE
DIRECTION OFBOREHOLE DRIFT
UE-25c #3
UE-25C #1
100 FEET
50 METERS
Figure 2. Surface location and drift of boreholes UE-25c #1, UE-25c #2, and UE-25c #3.
Table 2. Distances between pumped wells and monitored intervals in observation wells during some pumping tests conducted in 1984 in boreholes UE-25c #2 and UE-25c #3
Connected pointsMonitored Interval(feet below land
surface)
Thickness- weighted average distance
(feet)
Borehole UE-25c #2 test, March 1984UE-25c#l above packers to UE-25c #2 1,371-2,510 270 UE-25c #1 between packers to UE-25c #2 2,520-2,600 277
Borehole UE-25c #3 test, May-June 1984
UE-25c#l above packers to UE-25c #3 1,371-1,595 256 UE-25c#l between packers to UE-25c #3 1,605-1,680 259
Borehole UE-25c #3 test, October-December 1984UE-25c #1 above packers to UE-25c #3 1,371-2,514 267 UE-25c #1 between packers to UE-25c #3 2,524-2,594 280 UE-25c #1 below packers to UE-25c #3 2,603-3,000 280 UE-25c #2 between packers to UE-25c #3 2,364-2,475 92
Results and Interpretation of Preliminary Aquifer Tests In Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
16 15 14 13 12 11 11 12 13 14 15 16 17
BOREHOLE DIAMETER, IN INCHES, ON DECEMBER 11, 1992 CALIPER LOG
2,730
EXPLANATION
OPEN, NEAR VERTICAL, SOUTH-STRIKING (160°-195°) FRACTURE Dashed where extrapolated outside borehole
OPEN, VERTICAL, NORTHWEST-STRIKING (330°) FRACTURE
Figure 3. Relation between fractures and borehole diameter in an enlarged, rugose interval of borehole UE-25c #2.
(Grady O'Brien, U.S. Geological Survey, written com- mun., 1993). As indicated by TV and caliper logs listed in table 1, casing and concrete extend 1,368 ft below the top of the borehole. The open part of the borehole was rotary-drilled with a 14.75-in.-diameter bit through the bottom of the concrete to a depth of 1,514 ft and a 9.875-in.-diameter bit from 1,514 to 3,000 ft. Caliper logs indicate that the borehole walls are very irregular (pi. 3). TV and caliper logs indicate that the bottom of the borehole has collapsed substan tially since completion. The bottom of the borehole was at a depth of 3,000 ft in April 1984,2,976 ft in March 1985, and 2,954 ft in June 1992.
Site Geology
The c-holes are completed in Miocene tuf- faceous rocks that are covered by a thin veneer (0-80 ft) of Quaternary alluvium and underlain by dolomite of the Silurian Roberts Mountain Formation and Lone Mountain Dolomite (Carr and others, 1986; Geldon, 1993). Based on information obtained from borehole UE-25p #1, 2,028 ft southeast of borehole UE-25c #1, the Miocene rocks are estimated to be about 5,000 ft thick in the vicinity of the c-holes.
Northerly trending, high-angle faults, such as the Paintbrush Canyon and Bow Ridge Faults, have offset and tilted the Miocene rocks in the vicinity of the
PHYSICAL SETTING
c-holes (Scott and Bonk, 1984). The dip of the Miocene rocks increases in fault blocks from 5° to 10° on the crest of Yucca Mountain to 15° to 20° at the c-hole complex (Frizzell and Shulters, 1990; Geldon, 1993). According to Scott (1990), the high- angle faults merge listrically at depth with a detach ment fault that forms the contact between Miocene and Paleozoic rocks in the Yucca Mountain area. However, Carr (1990) considers the contact between the Miocene and Paleozoic rocks to be an unconformity, and the high-angle faults in the Yucca Mountain area to be col lapse faults bordering a caldera centered in Crater Flat (location shown in fig. 1).
As indicated in table 3, Miocene rocks pene trated by the c-holes include the Tiva Canyon and Topopah Spring Members of the Paintbrush Tuff, the tuffs and lavas of Calico Hills, and the Prow Pass, Bullfrog, and Tram Members of the Crater Flat Tuff. These geologic units predominantly consist of ash-flow tuff, that is devitrified to vitrophyric and nonwelded to
densely welded. Bedded tuff, consisting of ash-fall tuff and volcaniclastic rocks (reworked tuff), is interlayed with the ash-flow tuff at the base of formations and members. Unique to boreholes in the Yucca Mountain area, a tuff breccia occurs in the Tram Member in an interval where moderately welded ash-flow tuff is present in nearby boreholes (Geldon, 1993). Faults that intersect at the c-hole complex apparently have brecciated the upper nonwelded to partially welded part of the Tram Member and cut out the moderately welded part (Geldon, 1993). All of the geologic units at the c-hole complex have been altered partially to zeolite and clay minerals below the water table, which according to information from Robison and other (1988) and USGS files, occurs at depths of between 1,312 and 1,320 ft below the land surface (at altitudes of 2,394 to 2,396 ft above the NGVD of 1929). The water table is slightly above or below the contact between the Paintbrush Tuff and the tuffs and lavas of
Table 3. Stratigraphic column for the c-hole complex
[Summarized from lithologic logs prepared by Richard E. Spengler, USGS, written commun., 1984; dashed line in depth column indicates an unconformity]
Geologic unit Generalized descriptionDepth below land surface
(feet)
UE-25C #1 UE-25c #2 UE-25C #3
Alluvium Paintbrush Tuff
Tiva Canyon Member
Topopah Spring Member
Tuffs and lavas of Calico Hills
Crater Flat Tuff
Sand and gravel
Moderately to densely welded ash-flow tuff with thin basal bedded tuffModerately to densely welded ash-flow tuff with inter vals containing lithophysae; thin vitrophyre and non- welded tuff layers at the top and bottom Nonwelded ash-flow tuff Bedded tuff
Absent 0-70 0-80
0-315 70-290 80-290
315-1,332 290-1,316 290-1,300
1,332-1,593 1,593-1,691
1,316-1,570 1,570-1,672
1,300-1,560 1,560-1,629
Prow Pass Member
Bullfrog Member
Tram Member
Nonwelded to partially welded ash-flow tuffModerately welded ash-flow tuffPartially welded to nonwelded ash-flow tuffBedded tuffNonwelded to partially welded ash-flow tuffModerately to densely welded ash-flow tuffPartially welded to nonwelded ash-flow tuffBedded tuffNonwelded to partially welded ash-flow tuff
Indurated tuff brecciaPartially welded, lithic ash-flow tuff
1,692-1,8381,838-1,860
~ UJ6CT2, m ~
2,118-2,152~ 2T15T-2T260"
2,260-2,4802,480-2,6952,695-2,7162,716-2,775
2,775-2,975
2,975-3,000
1,673-1,8101,810-1,8401,840-2,1102,110-2,138
~2,l39^2,240 ~2,240-2,4602,460-2,6752,675-2,7192,719-2,775
2,775-2,935
2,935-3,000
1,630-1,7801,780-1,8301,830-2,0852,085-2,1122,112-2,2102,210-2,4302,430-2,6502,650-2,6702,670-2,804
2,804-3,000Not reached
Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
Calico Hills in individual boreholes (see tables in the Supplementary Data section at the end of this report).
The tuffaceous rocks at the c-hole complex are pervaded by tectonic and cooling fractures. Fracture orientations and frequency in the geologic units pene trated by the c-holes vary from unit to unit and among boreholes, but for the tuffs and lavas of Calico Hills and the Crater Flat Tuff, in general, fractures strike pre dominantly south-southeast to south-southwest (fig. 4) and dip 50° to 87° to the west-southwest or west-north west. Largely because of the Tram Member of the Crater Flat Tuff, the second most abundant fractures in the c-holes strike north-northwest to north-northeast and dip east-northeast to east-southeast. Many of the latter fractures are shallow-dipping or mineralized. The least common fractures generally strike to the east (between 70° and 110°) and west (between 250° and 290°), and many of these are shallow-dipping or miner alized. In contrast to boreholes UE-25c #1 and UE-25c #2, southwesterly, westerly, and northwest erly-striking fractures are more common in borehole UE-25c #3 than southeasterly, easterly, and northeast erly striking fractures. Borehole UE-25c #3 differs from the other two c-holes, also, in having a smaller proportion of steep to vertical, nonmineralized frac tures to mineralized or shallow, nonmineralized frac tures. Because of fault brecciation, fracture frequency is greatest in the Tram Member. The bedded zone of the tuffs and lavas of Calico Hills is also very fractured. On the average, moderately to densely welded zones of the Prow Pass and Bullfrog Members are more frac tured than bedded zones, which in turn, are more frac tured than nonwelded to partially welded zones (pis. 1-3).
SITE HYDROLOGY
The tuffaceous rocks penetrated by the c-holes are not uniformly permeable. Variations in fracture fre quency and openness and matrix permeability confine ground-water movement to relatively thin intervals in the tuffs and lavas of Calico Hills and the Crater Flat Tuff. In combination, laboratory analyses of core per meability, fracture (television and acoustic televiewer) logs, caliper logs, resistivity logs, temperature logs, tracejecter surveys during pumping tests, and heat- pulse flowmeter surveys identify the transmissive intervals.
Matrix Permeability
Permeameter tests were done on 20 samples of core from boreholes UE-25c #1, UE-25c #2, and UE-25c #3 (table 1) to determine horizontal and verti cal matrix permeability. These samples were insuffi cient to characterize the variation in matrix permeability with depth throughout the entire thickness of tuffaceous rocks penetrated by the c-holes. How ever, with the addition of permeability analyses for 69 samples of core from four boreholes within a three- mile radius of the c-hole complex (table 1), profiles of horizontal matrix permeability as a function of depth within geologic units (sample depth divided by the thickness of the geologic unit from which the sample was obtained) were prepared for the c-holes and nearby boreholes (fig. 5).
To construct the permeability profile shown in figure 5, it was assumed that permeability values would be the same at the same normalized depths within geo logic units at different locations. However, it was rec ognized that this assumption might be incorrect locally because of lateral changes in lithology. Some points shown in figure 5 that deviate substantially from the plotted permeability profile were ignored under the assumption that they represent either locally unusual lithology or a poorly correlated permeability value.
Horizontal matrix permeability as a function of depth for each of the c-holes was calculated from the permeability and percent of thickness values in figure 5 and depths of stratigraphic horizons listed in table 3. As indicated on plates 1-3, horizontal matrix perme ability in the tuffaceous rocks at the c-hole complex is estimated to range from 0.001 to 20 mD. With respect to matrix permeability, the tuffaceous rocks at the c-hole complex are slightly anisotropic (fig. 6). Matrix permeability is slightly larger in the horizontal direc tion than in the vertical direction. Expressed as a func tion of horizontal matrix permeability (kr\ vertical matrix permeability (fcz) can be found from the follow ing empirically derived equation (R2 = 0.71):
log* = 0.881og*r -0.36 (1)
Vertical matrix permeability in the tuffaceous rocks at the c-hole complex is estimated to range from 0.001 to 6mD.
SITE HYDROLOGY B
UE-25c #1P B T A C P B TiA C P B TiA C P B T A C P B TiA C P B TiA C P B TiA C.P B TiA
'340-20' 21-69 ' 70 -110 'ill - 159'l60 - 200 201 - 249'250 - 290'29l - 339'
UE-25c #3
70-110 111 - 159 160 - 200 201 - 249 250 - 290 291 - 339'
STRIKE AZIMUTH, IN DEGREES
200
190 -
UE-25C #2C P B T.A C P B T A C P B TiA C P B TiA C P B TIA C P B T A C P B TIA C P B TM
340-20 21-69 70 -110 111 - 159'l60 - 200'201 - 249'250 - 290'291 - 339 1
STRIKE AZIMUTH, IN DEGREES
EXPLANATION
"'// 'A PARTLY OR ENTIRELY MINERALIZED
NONMINERALIZED, SHALLOW (<50 DEGREE DIP)
NONMINERALIZED, STEEP TO VERTICAL
TUFFS AND LAVAS OF CALICO HILLS
PROW PASS MEMBER OF THE CRATER FLAT TUFF
BULLFROG MEMBER OF THE CRATER FLAT TUFF
TRAM MEMBER OF THE CRATER FLAT TUFF
ALL GEOLOGIC UNITS
Figure 4. Frequency distribution of fracture orientations in boreholes UE-25c #1, UE-25c #2, and UE-25c #3. (Based on TV and acoustic televiewer logs. Fractures identified in the c-holes are listed in the Supplementary Data section at the end of this report.)
10 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
CA
LIC
O H
ILL
S
UP
PE
R:
Nonw
eld
ed
PR
OW
PA
SS
UP
PE
R:
Nonw
eld
ed t
o
modera
tely
we
lde
d
LOW
ER
: P
art
ially
we
lde
d
to n
onw
eld
ed (
som
e m
od
era
tely
weld
ed)1
BU
LLF
RO
GU
PP
ER
: N
on
we
lde
d t
o part
ially
we
lde
d
MID
DLE
: M
od
era
tely
w
eld
ed (
som
e p
art
ially
w
eld
ed
)
LOW
ER
: P
artia
lly w
eld
ed
to
nonw
eld
ed (
som
e m
od
era
tely
weld
ed)
TR
AM
UP
PE
R:
Nonw
eld
ed t
o
part
ially
weld
ed
BO
RE
HO
LES
UE
-25b
#1
UE
-25c
#1
UE
-25c
#2
UE
-25c
#3
US
W G
-4
US
W G
-3
US
WH
-1
MID
DLE
: T
uff b
recc
ia
LOW
ER
: P
artia
lly t
o
mo
de
rate
ly w
eld
ed
lit
hic
tuff
0.00
010.
001
1 T
hin
bedd
ed i
nte
rvals
at t
he
bas
e o
f th
e P
row
Pas
s an
d B
ullf
rog
Me
mb
ers
are
om
itted.
One
sam
ple
of
bedd
ed t
uff
had
a p
erm
ea
bili
ty o
f 0.
26 m
illid
arc
ies
0.01
0.
1 1
MA
TR
IX P
ER
ME
AB
ILIT
Y,
IN M
ILLID
AR
CIE
S
10
Figu
re 5
. H
oriz
onta
l mat
rix p
erm
eabi
lity
in th
e tu
ffs a
nd la
vas
of C
alic
o H
ills a
nd C
rate
r Fl
at T
uff,
east
-cen
tral Y
ucca
M
ount
ain
area
, as
a fu
nctio
n of
dep
th w
ithin
geo
logi
c un
its (
base
d on
cor
e an
alys
es li
sted
in ta
ble
1).
100
10
0.1
0.01
0.001
0.0001
LINE OF EQUAL HORIZONTAL AND. VERTICAL MATRIX PERMEABILITY
REGRESSION LINE
O
O
O
O
BOREHOLES
A UE-25b#1
x UE-25c #1
4 UE-25c #2
O UE-25C #3
USW G-4
+ USW G-3
O USW H-1
0.0001 0.001 0.01 0.1 1
HORIZONTAL MATRIX PERMEABILITY, IN MILLIDARCIES
10 100
Figure 6. Relation of vertical to horizontal matrix permeability in core samples from the tuffs and lavas of Calico Hills and Crater Flat Tuff in the c-holes and nearby boreholes.
Heat-Pulse Flowmeter Surveys
Heat-pulse flowmeter surveys were conducted in each of the c-holes in December 1991 by Alfred E. Hess and Frederick L. Paillet of the USGS Borehole Geophysics Research Project to identify zones of intraborehole flow under natural hydraulic gradients (undisturbed by pumping or drilling). As described by Hess (1990), the method used involves lowering the flowmeter probe by cable to intervals of a borehole previously identified by fracture (television and acoustic televiewer) logs, caliper logs, and temper ature logs as possibly transmissive intervals. Measure ments are made with the probe above and below an
interval of interest. A packer is inflated above the probe to restrict the measurement to the depth of inter est. The flow measurement is made by releasing a heat pulse from an open grid of resistance wire and timing the movement of the heat pulse to sensors located at equal distances above and below the heat source. A positive deflection on a strip-chart recording of heat- pulse transit time indicates movement of the heat pulse to the upper sensor and, hence, upward intraborehole flow. A negative deflection on a strip-chart recorder indicates movement of the heat pulse to the lower sen sor and, hence, downward intraborehole flow. Heat- pulse transit time is converted to flow rate by an empir ically derived calibration equation for the probe.
12 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c *2, and UE-25c f 3, Yucca Mountain, Nye County, Nevada
Heat-pulse flowmeter surveys indicated dis tinctly different patterns of intraborehole flow in each of the c-holes (pis. 1-3). In borehole UE-25c #1, the flow fluctuated slightly but remained less than 0.09 gal/min and downward from 1,505 to about 2,520 ft. Below about 2,520 ft, the intraborehole flow became upward. The upward flow increased from 0 to 1.18 gal/min between about 2,520 and 2,735 ft, decreased to 0.91 gal/min between 2,735 and 2,765 ft, and became too small to measure reliably between 2,765 and 2,830 ft.
Similar to the pattern in borehole UE-25c #1, flow in borehole UE-25c #2 was downward in the top of the borehole and upward in the bottom of the bore hole. However, downward and upward flow in bore hole UE-25c #2 remained small (less than 0.15 gal/min) throughout the entire surveyed part of the borehole, and the change from downward to upward flow was 230 ft lower than in borehole UE-25c #1.
In contrast to the situation in boreholes UE-25c #1 and UE-25c #2, the flow in borehole UE-25c #3 was upward throughout the entire surveyed part of the borehole, although it is possible that small downward flow might be occurring above the upper most measuring depth. The flow in borehole UE-25c #3 decreased from 0.10 to 0.05 gal/min between 1,505 and 1,650 ft, increased gradually to 0.08 gal/min between 1,650 and 2,275 ft, increased sharply to 4.0 gal/min between 2,275 and 2,550 ft, and decreased from 4.0 to 1.7 gal/min between 2,800 ft and the bottom of the borehole.
As described in the next section, changes in flow in the c-holes generally coincide with zones of moder ately to very fractured rock. Faults, partings, and inter vals with relatively large matrix permeability, also influence intraborehole flow.
Transmissive Intervals
The best indicators of transmissivity are aquifer tests and numerical modeling. However, both tech niques require some knowledge of hydrogeologic con ditions in advance of use for the most reliable calculation of hydrologic properties. Diverse labora tory and geophysical data obtained at the c-hole com plex from 1983-1992 were used to determine transmissive intervals in and between the c-holes in order to improve the analysis and interpretation of pre liminary aquifer tests conducted at the c-hole complex. For example, knowing that ground-water flow was occurring in only 50 ft of a packed-off interval 500-ft thick instead of the entire interval, substantially would change the calculation of hydraulic conductivity from
a transmissivity value determined by a pumping test. The analytical solution used to calculate transmissivity from drawdown, residual drawdown, or recovery data, and hence the numerical value obtained, would be expected to differ substantially if pre-test analysis showed that the source of ground water in a borehole was a fracture zone, an unfractured interval with large matrix permeability, a fault, or gravity drainage from the water table. In this study, the following criteria were used to identify transmissive intervals:
1. Gains and losses in intraborehole flow detected during heat-pulse flowmeter surveys;
2. Gains in discharge detected by tracejector surveys during pumping tests;
3. Inflections in nonpumping temperature gradients (caused by inflow, outflow, upflow, or down- flow);
4. Relatively low resistivity associated with moder ate to intense fracturing, relatively large matrix permeability, or partings (indicating that the resistivity is related to water and not weather ing, mineralization, or other factors); and
5. Borehole enlargement associated with fracturezones, an indicator of the openness of individ ual fractures, or the presence of cavities created by fracture intersections.
Transmissive intervals in each of the c-holes and their characteristics are listed in tables 4-6. Figure 7, a hydrogeologic section of the c-holes, drawn along lines shown in figure 2, extrapolates transmissive intervals between the c-holes. For purposes of discussion in this report, the c-hole transmissive intervals informally were grouped into four aquifers that are separated by three confining units. The aquifers cannot be consid ered as formal hydrogeologic units because (1) the aquifers are defined largely by the extent of fracturing within them; (2) fractures are spatially related to faults at the c-hole complex; and (3) in different areas, faults and related fractures can be expected to penetrate geo logic units differently than at the c-hole complex.
Calico Hills Aquifer
The Calico Hills aquifer extends from the water table, at depths between 1,312 and 1,320 ft to about 1,700 ft below land surface and is unconfined. It con sists of three relatively thin zones of moderately to very fractured rock separated by unfractured to sparsely fractured rock, much of which contains large matrix permeability (fig. 7). Fractures, some of which are
SITE HYDROLOGY 13
_*
Tabl
e 4.
Tra
nsm
issi
ve in
terv
als
in b
oreh
ole
UE
-25c
#1
Results
and
Interpr
Nye
County, Nevad 0
$ S o 3
o 3 3 § a) > C 3- H 9 3 3 g- 8 c
m 10 0 * c
m g" o *
[Fea
ture
s oi
scus
se
Dep
th
belo
w la
nd
surf
ace
(fee
t)1,
406-
1,51
6
1,52
1-1,
593
1,62
3-1,
639
1,69
1-1,
692
1,80
3-1,
846
1,86
0-1,
861
1,91
9-1,
925
1,96
3-1,
975
2,05
0-2,
156
2,21
5-2,
260
2,39
2-2,
457
2,46
3-2,
560
2,56
0-2,
604
A br
iefly
in th
is ta
ble
are
show
n in
det
ail o
n pl
ate
1J
Cha
ract
eris
tics
Poor
vis
ibili
ty b
ut b
elie
ved
to b
e sp
arse
ly to
mod
erat
ely
frac
ture
d. K
now
n fr
ac
ture
s sh
allo
w-n
ear v
ertic
al, n
orth
, sou
th, s
outh
east
, and
wes
t-stri
king
Ver
y fr
actu
red
to 1
,544
ft, l
arge
mat
rix p
erm
eabi
lity
belo
w; f
ract
ures
are
ste
ep-v
er
tical
, nor
th, e
ast,
sout
heas
t, so
uth,
and
wes
t-stri
king
Ver
y fr
actu
red;
fra
ctur
es a
re n
ear v
ertic
al-v
ertic
al, s
outh
-stri
king
Ope
n pa
rting
at C
alic
o H
ills-
Cra
ter F
lat c
onta
ct
Ver
y fr
actu
red,
larg
e m
atrix
per
mea
bilit
y; fr
actu
res
are
stee
p-ve
rtica
l, m
ostly
nor
th,
sout
h, s
outh
east
, and
sou
thw
est-s
triki
ngO
pen
parti
ng b
etw
een
mod
erat
ely
wel
ded
and
parti
ally
wel
ded
to n
onw
elde
d zo
nes
of P
row
Pas
s M
embe
rV
ery
frac
ture
d; f
ract
ures
are
ope
n, s
hallo
w-s
teep
, nor
th, e
ast,
and
sout
h-st
rikin
gM
oder
atel
y fr
actu
red;
fra
ctur
es a
re o
pen,
sha
llow
, nor
th-s
triki
ngPo
or v
isib
ility
but
bel
ieve
d to
be
spar
sely
to v
ery
frac
ture
d; k
now
n fr
actu
res
are
shal
low
-ver
tical
, mos
tly s
outh
and
nor
thea
st-s
triki
ng.
Inte
rval
s w
ith la
rge
mat
rixpe
rmea
bilit
y an
d an
ope
n pa
rting
at t
he P
row
Pas
s-B
ullfr
og c
onta
ctV
ery
frac
ture
d to
2,2
43 ft
, lar
ge m
atrix
per
mea
bilit
y be
low
; fra
ctur
es, s
ome
ofw
hich
are
ope
n, a
re s
hallo
w-v
ertic
al, n
orth
, sou
thea
st, a
nd s
outh
-stri
king
Spar
sely
to v
ery
frac
ture
d, w
ith la
rge
mat
rix p
erm
eabi
lity
belo
w 2
,415
ft;
frac
ture
sar
e ne
ar v
ertic
al- v
ertic
al, s
outh
and
eas
t-stri
king
Ver
y fr
actu
red
rock
sep
arat
ed b
y th
in in
terv
als
of u
nfra
ctur
ed ro
ck; f
ract
ures
, man
yof
whi
ch a
re o
pen
are
stee
p-ve
rtica
l, so
uth,
eas
t, an
d so
uthe
ast-s
triki
ng
Mod
erat
ely
to v
ery
frac
ture
d; fr
actu
res
are
open
, sha
llow
-ste
ep, n
orth
and
nor
th-
Intr
abor
ehol
e flo
w
(gal
lons
per
min
ute)
>0.0
9 do
wn
0.02
out
0.01
out
0.02
in a
nd d
own
0.02
out
0.02
in a
nd d
own
0.01
out
0.01
in a
nd d
own
0.01
out
0.03
in a
nd d
own
0.1 2
out
(cha
ngin
gfr
om d
own
to u
p at
2,52
0 ft)
0.76
out
Pum
ping
di
s
char
ge
(per
cent
)0 0 0 0 0 0 0 0 0 0 0 0 64
Supp
ortin
g in
form
atio
n
Low
resi
stiv
ity
Low
resi
stiv
ity, c
onca
ve te
mpe
ratu
regr
adie
nt in
flect
ion
Low
resi
stiv
ityLo
w re
sist
ivity
, con
vex
tem
pera
ture
grad
ient
infle
ctio
nB
oreh
ole
enla
rgem
ent
Abr
upt r
esis
tivity
dec
reas
e
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
Ver
y lo
w re
sist
ivity
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent,
pron
ounc
ed c
onca
ve te
mpe
ratu
re g
ra
dien
t inf
lect
ion
Ver
y lo
w re
sist
ivity
, con
vex
tem
pera
-
0 o.
c
east
-str
ikin
g an
d ne
ar v
ertic
al o
r ver
tical
, eas
t-st
riki
ng
2,65
6-2,
715
Mod
erat
ely
frac
ture
d, la
rge
mat
rix p
erm
eabi
lity;
fra
ctur
es a
re s
hallo
w-s
teep
, nor
th-
strik
ing
2,72
9-2,
752
Ver
y fr
actu
red;
fra
ctur
es, s
ome
of w
hich
are
ope
n, a
re s
hallo
w-v
ertic
al a
nd
dive
rsel
y or
ient
ed
0.38
out
0
0.29
in to
max
imum
0
upw
ard
flow
of 1
.18
ture
gra
dien
t inf
lect
ion,
bor
ehol
een
larg
emen
tLo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t
Ver
y lo
w re
sist
ivity
, con
cave
tem
pera
tu
re g
radi
ent i
nfle
ctio
n, b
oreh
ole
enla
rgem
ent
2,75
9-2,
790
2,79
0-2,
840
2,89
0-2,
915
2,92
1-2,
941
2,96
0-2,
980
Ver
y fr
actu
red;
fra
ctur
es, s
ome
of w
hich
are
ope
n, a
re s
hallo
w-s
teep
, mos
tly s
outh
and
sout
hwes
t-stri
king
. Tw
o of
the
frac
ture
s com
pris
e th
e Pa
intb
rush
Can
yon
Faul
tzo
neV
ery
frac
ture
d; f
ract
ures
, som
e of
whi
ch a
re o
pen,
are
ste
ep- v
ertic
al a
nd d
iver
sely
orie
nted
Ver
y fr
actu
red;
fra
ctur
es a
re n
ear v
ertic
al-v
ertic
al, d
iver
sely
orie
nted
Ver
y fr
actu
red;
fra
ctur
es a
re s
hallo
w-v
ertic
al, d
iver
sely
ori
ente
dM
oder
atel
y fr
actu
red(
?):
unce
rtain
bec
ause
inte
rval
con
ceal
ed b
y bo
reho
leco
llaps
e
<0.9
1 in
and
up
Smal
l up
Smal
l up(
?)
Smal
l up(
?)Sm
all u
p(?)
25 0 11 0 0
Con
vex
tem
pera
ture
gra
dien
t inf
lec
tion,
ext
ensi
ve b
oreh
ole
enla
rgem
ent
Bor
ehol
e en
larg
emen
t
Con
cave
tem
pera
ture
gra
dien
t inf
lec
tion,
bor
ehol
e en
larg
emen
tC
onve
x te
mpe
ratu
re g
radi
ent i
nfle
ctio
nLo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t
Tab
le 5
. T
rans
mis
sive
int
erva
ls in
bor
ehol
e U
E-2
5c #
2
[Fea
ture
s disc
usse
d br
iefly
in th
is ta
ble
are
show
n in
det
ail o
n pl
ate
2]
Dep
thbe
low
land
surf
ace
(feet
)
Cha
ract
eris
tics
Intr
abor
ehol
eflo
w(g
allo
ns p
er
min
ute)
Pum
p
ing
dis
ch
arge
(p
er
cent
)
Sup
port
ing
info
rmat
ion
o 3J
O 5 S
1,44
1-1,
570
Poor
vis
ibili
ty to
1,5
14 ft
, but
bel
ieve
d to
be
spar
sely
to m
oder
atel
y fr
ac
ture
d to
1,5
52 ft
. La
rge
mat
rix p
erm
eabi
lity
belo
w 1
,539
ft.
Kno
wn
frac
tu
res
are
verti
cal,
north
wes
t, no
rth, a
nd n
orth
east
-stri
king
; tw
o ar
e op
en
1,62
4-1,
634
Ver
y fr
actu
red;
fra
ctur
es a
re s
hallo
w, n
orth
and
nor
thea
st-s
triki
ng1,
644-
1,65
3 V
ery
frac
ture
d; fr
actu
res
are
shal
low
-ver
tical
, div
erse
ly o
rient
ed, o
pen
at
inte
rsec
tions
1,67
2-1,
673
Ope
n pa
rting
at C
alic
o H
ills-
Cra
ter F
lat c
onta
ct1,
812-
1,87
0 V
ery
frac
ture
d, w
ith la
rge
mat
rix p
erm
eabi
lity;
fra
ctur
es a
re n
ear v
ertic
al-
verti
cal,
sout
h an
d so
uthe
ast-s
triki
ng
1,94
8-1,
968
Mod
erat
ely
frac
ture
d(?)
. N
o kn
own
frac
ture
s be
caus
e of
poo
r vis
ibili
ty2,
045-
2,09
3 Po
or v
isib
ility
; cou
ld b
e sp
arse
ly to
mod
erat
ely
frac
ture
d, a
lthou
gh n
o fr
ac
ture
s w
ere
dete
cted
. In
terv
al k
now
n to
hav
e la
rge
mat
rix p
erm
eabi
lity
2,10
7-2,
122
Poor
vis
ibili
ty, b
ut b
elie
ved
to b
e m
oder
atel
y fr
actu
red.
Kno
wn
to h
ave
larg
e m
atrix
per
mea
bilit
y2,
138-
2,13
9 O
pen
parti
ng a
t Pro
w P
ass-
Bul
lfrog
con
tact
2,25
2-2,
267
Ver
y fr
actu
red;
fra
ctur
es, o
ne o
f whi
ch is
ope
n, a
re n
ear
verti
cal-v
ertic
al,
sout
h-st
rikin
g2,
380-
2,41
6 V
ery
frac
ture
d, w
ith la
rge
mat
rix p
erm
eabi
lity;
fra
ctur
es, a
bout
a th
ird o
f w
hich
are
ope
n, a
re s
teep
-ver
tical
, mos
tly n
orth
and
sou
th-s
triki
ng (
also
no
rthea
st, e
ast,
sout
heas
t, an
d so
uthw
est-s
triki
ng)
2,43
7-2,
499
Ver
y fr
actu
red
rock
with
thin
inte
rval
s of
unf
ract
ured
rock
; fra
ctur
es m
ostly
ar
e op
en, s
teep
-ver
tical
, sou
th, s
outh
east
, sou
thw
est,
and
north
wes
t-stri
king
2,69
1-2,
694
Ver
y fr
actu
red;
inte
rval
con
tain
s a
sing
le p
artly
min
eral
ized
, ver
tical
, sou
th-
strik
ing
frac
ture
, ind
icat
ed o
n lit
holo
gic
log
to b
e a
faul
t2,
707-
2,72
6 V
ery
frac
ture
d; fr
actu
res
mos
tly a
re o
pen,
ste
ep-v
ertic
al, s
outh
east
, sou
th,
and
sout
hwes
t-stri
king
2,74
9-2,
789
Ver
y fr
actu
red;
fra
ctur
es, t
hree
of w
hich
are
ope
n, a
re s
teep
-ver
tical
, nor
th
and
sout
h-st
rikin
g
2,78
9-2,
797
Ver
y fr
actu
red;
frac
ture
s m
ostly
are
sha
llow
-ste
ep, s
outh
-stri
king
; thr
eeop
en fr
actu
res
at 2
,793
-2,7
95 f
t com
pris
e th
e Pa
intb
rush
Can
yon
Faul
t zon
e
2,89
1-2,
942
Ver
y fr
actu
red;
fra
ctur
es, f
our o
f whi
ch a
re o
pen,
are
ste
ep-v
ertic
al,
dive
rsel
y or
ient
ed
2,94
2-2,
961
Spar
sely
fra
ctur
ed; i
nter
val k
now
n to
con
tain
two
shal
low
, sou
th-s
triki
ngfr
actu
res,
one
of w
hich
is o
pen
>0.0
4 do
wn
0.01
in
and
dow
n
0.10
in a
nd
dow
n to
max
i m
um d
ownw
ard-
flo
w o
f 0.1
50.
01 o
ut
0.01
out
0.01
out
0.04
out
0.02
out
Smal
l los
s(?)
>0.0
3 ou
t
0.08
out
(cha
ng
ing
from
dow
n
war
d to
upw
ard
at 2
,750
ft)
>0.0
5 in
to m
ax
imum
upw
ard
flow
Smal
l up(
?)
Smal
l up(
?)
0 Lo
w re
sist
ivity
; con
vex
tem
pera
ture
gra
dien
tin
flect
ion
at a
bout
1,4
65 f
t, an
d co
ncav
e te
mpe
ra
ture
gra
dien
t inf
lect
ion
at a
bout
1,5
20 ft
; bor
ehol
e en
larg
emen
t and
rugo
sity
0
Ver
y lo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t 0
Ver
y lo
w re
sist
ivity
, con
vex
tem
pera
ture
gra
dien
tin
flect
ion,
bor
ehol
e en
larg
emen
t 0
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
0 D
ecre
ase
to lo
w re
sist
ivity
con
cave
tem
pera
ture
gr
adie
nt in
flect
ion
0 Lo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t0
Gen
eral
ly lo
w re
sist
ivity
, con
vex
tem
pera
ture
gra
di
ent i
nfle
ctio
n, s
ubst
antia
l bor
ehol
e en
larg
emen
t0
Gen
eral
ly lo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t an
d ru
gosi
ty7
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
0 Lo
w re
sist
ivity
79
Res
istiv
ity tr
ough
, maj
or c
onve
x te
mpe
ratu
re g
ra
dien
t inf
lect
ion,
bor
ehol
e en
larg
emen
t
14
Dec
reas
e to
low
resi
stiv
ity, c
onca
ve te
mpe
ratu
re
grad
ient
infle
ctio
n; m
inor
bor
ehol
e en
larg
emen
t 0
Low
resi
stiv
ity
0 Lo
w re
sist
ivity
, maj
or c
onca
ve te
mpe
ratu
re g
radi
en
t inf
lect
ion,
maj
or b
oreh
ole
enla
rgem
ent
0 Lo
w re
sist
ivity
, con
vex
tem
pera
ture
gra
dien
t in
flect
ion,
bor
ehol
e en
larg
emen
t and
rugo
sity
Low
resi
stiv
ity
0 Lo
w re
sist
ivity
, con
cave
tem
pera
ture
gra
dien
tin
flect
ion
0 Lo
w re
sist
ivity
I II
Tabl
e 6.
Tra
nsm
issi
ve in
terv
als
in b
oreh
ole
UE
-25c
#3
[Fea
ture
s di
scus
sed
brie
fly in
this
sec
tion
are
show
n in
det
ail o
n pl
ate
3]
o I I 3 3 I
Dep
thbe
low
land
surf
ace
(feet
)
Cha
ract
eris
tics
intr
abor
ehol
e flo
w(g
allo
ns p
erm
inut
e)
Pum
p
ing
dis
ch
arge
(p
er
cent
)
Supp
ortin
g in
form
atio
n
o_ 9 m C m m ; a m
1,41
4-1,
483
Spar
sely
to m
oder
atel
y fr
actu
red.
Kno
wn
frac
ture
s ar
e st
eep-
near
ver
tical
, nor
th a
nd
Smal
l dow
n(?)
0
north
wes
t-stri
king
. U
nfra
ctur
ed ro
ck a
ppar
ently
tran
smits
wat
er1,
483-
1,52
2 M
oder
atel
y to
ver
y fr
actu
red;
larg
e m
atrix
per
mea
bilit
y; fr
actu
res,
mos
tly o
pen
to
>0.1
0 ou
t (an
y 0
1,51
0 ft,
are
sha
llow
-ver
tical
, nor
th, s
outh
, and
sout
hwes
t-stri
king
. W
ater
app
aren
tly
dow
nwar
d flo
w
is tr
ansm
itted
by
frac
ture
s an
d m
atrix
an
d al
l rem
aini
ngup
war
d flo
w lo
st)
1,52
2-1,
586
Spar
sely
to m
oder
atel
y fr
actu
red,
larg
e m
atrix
per
mea
bilit
y; f
ract
ures
are
sha
llow
- 0.
04 in
and
up
0 ve
rtica
l, no
rthea
st, e
ast,
and
sout
h-st
rikin
g. W
ater
app
aren
tly tr
ansm
itted
by
frac
tu
res
and
mat
rix1,
615-
1,64
0 V
ery
frac
ture
d, la
rge
mat
rix p
erm
eabi
lity
belo
w 1
,629
ft, o
pen
parti
ng a
t Cal
ico
0.01
in
and
up
0 H
ills-
Cra
ter F
lat c
onta
ct; f
ract
ures
, mos
tly o
pen
1,62
2-1,
625
ft, a
re s
hallo
w-n
ear
verti
cal,
dive
rsel
y or
ient
ed.
Mos
t flo
w p
roba
bly
is th
roug
h op
en fr
actu
res
and
part
in
g1,
640-
1,67
4 Sp
arse
ly f
ract
ured
to 1
,666
ft, m
oder
atel
y fr
actu
red
belo
w; l
arge
mat
rix p
erm
eabi
l- Sm
all g
ain(
?)
0 ity
; fra
ctur
es a
re n
ear v
ertic
al, e
ast,
sout
h, a
nd s
outh
wes
t-stri
king
. W
ater
app
aren
tly
trans
mitt
ed b
y fr
actu
res
and
mat
rix1,
846-
1,86
5 M
oder
atel
y fr
actu
red,
larg
e m
atrix
per
mea
bilit
y; f
ract
ures
are
nea
r ver
tical
-ver
tical
Sm
all l
oss(
?)
0 ea
st, s
outh
east
, and
sou
th-s
triki
ng.
Wat
er a
ppar
ently
tran
smitt
ed b
y fr
actu
res
and
mat
rix1,
865-
1,95
0 Sp
arse
ly to
mod
erat
ely
frac
ture
d(?)
: N
o fr
actu
res
dete
cted
, but
mat
rix p
erm
eabi
lity
Smal
l los
s(?)
0
is to
o sm
all f
or u
nfra
ctur
ed ro
ck to
be
trans
mis
sive
2,05
0-2,
132
Spar
sely
frac
ture
d to
2,1
16 ft
, ver
y fr
actu
red
belo
w; l
arge
mat
rix p
erm
eabi
lity
<0.0
1 ou
t 0
thro
ugho
ut.
Frac
ture
s ar
e sh
allo
w-n
ear v
ertic
al, w
est a
nd s
outh
-stri
king
. W
ater
ap
pare
ntly
tran
smitt
ed b
y m
atrix
abo
ve 2
,116
ft, f
ract
ures
and
mat
rix b
elow
2,20
0-2,
215
Mod
erat
ely
frac
ture
d(?)
, lar
ge m
atrix
per
mea
bilit
y; a
lthou
gh n
o fr
actu
res
dete
cted
, 0.
02 o
ut
0 sh
arp
peak
on
calip
er lo
g im
plie
s pr
esen
ce o
f one
or m
ore.
Wat
er p
roba
bly
trans
mit
te
d by
fra
ctur
es a
nd m
atrix
2,37
4-2,
3 81
V
ery
frac
ture
d, la
rge
mat
rix p
erm
eabi
lity;
frac
ture
s, o
ne o
f whi
ch is
ope
n, a
re m
ostly
1.
72 o
ut
17
near
ver
tical
-ver
tical
, sou
thea
st-s
triki
ng2,
421-
2,47
8 V
ery
frac
ture
d; f
ract
ures
are
ope
n, n
ear v
ertic
al-v
ertic
al, s
outh
-stri
king
1.
7 ou
t 55
2,50
3-2,
527
Ver
y fr
actu
red;
fra
ctur
es, t
wo
of w
hich
are
ope
n, a
re v
ertic
al, s
outh
-stri
king
0.
5 ou
t 3
2,53
5-2,
665
Spar
sely
to m
oder
atel
y fr
actu
red(
?), w
ith la
rge
mat
rix p
erm
eabi
lity
belo
w
Smal
l los
s(?)
0
2,61
0 ft.
Inte
rval
kno
wn
to c
onta
in a
n op
en, s
hallo
w, n
orth
-stri
king
frac
ture
and
a
near
ver
tical
sou
th-s
triki
ng fr
actu
re; o
ther
frac
ture
s im
plie
d by
sha
rp c
alip
er p
eaks
. W
ater
pro
babl
y tra
nsm
itted
thro
ugh
open
frac
ture
s an
d m
atrix
Low
resi
stiv
ity; b
oreh
ole
enla
rgem
ent
Low
resi
stiv
ity, c
onca
ve te
mpe
ratu
re
grad
ient
infle
ctio
n, b
oreh
ole
enla
rge
m
ent
Low
resi
stiv
ity, c
onve
x te
mpe
ratu
re
grad
ient
refle
ctio
n
Ver
y lo
w re
sist
ivity
, bor
ehol
e en
larg
e
men
t to
abou
t 32
inch
es
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
Low
resi
stiv
ity, m
inor
bor
ehol
e en
larg
emen
t
Low
resi
stiv
ity, c
onca
ve te
mpe
ratu
regr
adie
nt in
flect
ion
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
Low
resi
stiv
ity, c
onca
ve te
mpe
ratu
re
grad
ient
infle
ctio
n, b
oreh
ole
enla
rge
m
ent
Con
vex
tem
pera
ture
gra
dien
t inf
lec
tio
n, b
oreh
ole
enla
rgem
ent
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
to 2
,450
ftLo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t Lo
w re
sist
ivity
, bor
ehol
e en
larg
emen
t
Tabl
e 6.
Tra
nsm
issi
ve in
terv
als
in b
oreh
ole
UE
-25c
#3
-Con
tinue
d
Dep
th
belo
w la
nd
surf
ace
(fee
t)
2,68
5-2,
755
2,75
8-2,
851
2,88
4-2,
887
2,89
9-2,
910
2,92
3-2,
945
2,95
0-3,
000
Cha
ract
eris
tics
Mod
erat
ely
to v
ery
frac
ture
d; f
ract
ures
, tw
o of
whi
ch a
re o
pen,
are
sha
llow
-ste
ep,
north
east
, sou
thw
est,
wes
t, no
rthw
est,
and
north
-stri
king
4
Ver
y fr
actu
red
rock
, inc
ludi
ng th
e Pa
intb
rush
Can
yon
Faul
t zon
e at
2,8
20-2
,825
ft,
sepa
rate
d by
thin
inte
rval
s of
unf
ract
ured
rock
; fra
ctur
es f
our o
f whi
ch a
re o
pen,
are
sh
allo
w-v
ertic
al, m
ostly
nor
th, s
outh
, and
sou
thw
est-s
triki
ngV
ery
frac
ture
d; f
ract
ures
are
sha
llow
-ste
ep, n
orth
and
nor
thw
est-s
triki
ngV
ery
frac
ture
d; f
ract
ures
are
sha
llow
-ste
ep, m
ostly
wes
t, no
rthw
est,
and
north
- st
rikin
gM
oder
atel
y fr
actu
red;
fra
ctur
es a
re s
hallo
w-v
ertic
al, m
ostly
nor
th a
nd w
est-s
triki
ng
Mod
erat
ely
frac
ture
d(?)
; ext
ent o
f fra
ctur
ing
unce
rtain
bec
ause
inte
rval
is c
once
aled
by
cab
le a
nd b
oreh
ole
colla
pse
Intr
abor
ehol
e flo
w
(gal
lons
per
m
inut
e)
Estim
ated
sm
all
gain
to m
axim
um
upw
ard
flow
of
>4.0
2.0
in a
nd u
p
0.1
in a
nd u
p0.
1 in
and
up
0.1
in a
nd u
p
1 .7
in a
nd u
p
Pum
p-
Ing
dis
ch
arge
(p
er
cent
)
0 25 0 0 0 0
Supp
ortin
g In
form
atio
n
Low
resi
stiv
ity, b
oreh
ole
enla
rgem
ent
arou
nd o
pen
frac
ture
s at
2,6
85 a
nd
2,70
3 ft
Low
resi
stiv
ity, c
onve
x te
mpe
ratu
re
grad
ient
infle
ctio
n, b
oreh
ole
enla
rge
m
ent t
o ab
out 2
2 in
ches
bel
ow 2
,830
ftLo
w re
sist
ivity
, bor
ehol
e en
larg
emen
tC
onca
ve te
mpe
ratu
re g
radi
ent i
nfle
c
tion
Low
resi
stiv
ity, c
onve
x te
mpe
ratu
re
grad
ient
infle
ctio
nLo
w re
sist
ivity
(0 3D
O I
FEET BELOW LAND SURFACE 1
1,300
1,400
1,500
1,600
1,700
1,800
1,900
2,000
2,100
2,200
2,300
2,400
2,500
2,600
2,700
2,800
2,900
3,000
UE-25C #3
BEND IN SECTION
UE-25C #1 UE-25C #2
CALICO HILLS AQUIFER
UPPER PROW PASS CONFINING UNIT
PROW PASS-UPPER BULLFROG AQUIFER
MIDDLE BULLFROG CONFINING UNIT
LOWER BULLFROG CONFINING UNIT
1 Depths in boreholes adjusted for topography by adding 5 feet to depths in borehole UE-25c #1, which is 5 feet lower than the other 2 boreholes
0 50 100 FEETI ,
50 METERS
Figure 7A. Hydrogeologic section of the c-hole complex.
18 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
EXPLANATION
PAINTBRUSH TUFF, TOPOPAH SPRING MEMBER
TUFFS AND LAVAS OF CALICO HILLS
NONWELDED
BEDDED
CRATER FLAT TUFF
PROW PASS MEMBER
NONWELDED TO PARTIALLY WELDED
MODERATELY WELDED
PARTIALLY WELDED TO NONWELDED
BEDDED
BULLFROG MEMBER
NONWELDED TO PARTIALLY WELDED
MODERATELY TO DENSELY WELDED
PARTIALLY WELDED TO NONWELDED
BEDDED
TRAM MEMBER
NONWELDED TO PARTIALLY WELDED
TUFF BRECCIA
PARTIALLY WELDED
TRANSMISSIVE INTERVAL Dark gray where moderately to very fractured; light gray where sparsely to moderately fractured (?) and largely dependent on matrix permeability for transmissivity. Roman numeral referenced in text
NONTRANSMISSIVE ROCK Unfractured to very fractured
PUMP-TEST PRODUCTION ZONE
J. BOREHOLE
T WATER TABLE ON JUNE 2, 1992
CONFORMABLE GEOLOGIC CONTACT
DISCONFORMABLE GEOLOGIC CONTACT, WITH OPEN PARTING, EXCEPT IN TRAM MEMBER
BOUNDARY OF TRANSMISSIVE INTERVAL
1 FAULT Arrows indicate relative direction of movement
DIRECTION OF NONPUMPEDINTRABOREHOLE FLOW
Figure 7B. Hydrogeologic section of the c-hole complex.
SITE HYDROLOGY 19
open, are shallow to vertical and diversely oriented. The upper part of the aquifer (transmissive interval I) is characterized by small to moderate downflows from the water table. In the middle part of the aquifer (trans missive intervals II and III), all downward flow in bore hole UE-25c #3, all remaining upward flow from lower in borehole UE-25c #3, and about a third of the down- wardflow in borehole UE-25c #1 are lost through frac tures and the rock matrix; some of this water flows into borehole UE-25c #2. At the bottom of the aquifer, small upflows and downflows enter the c-holes through a parting at the contact between the tuffs and lavas of Calico Hills and the Crater Flat Tuff.
Prow Pass - Upper Bullfrog Aquifer
The Prow Pass - upper Bullfrog aquifer extends from about 1,800 ft to about 2,270 ft below land surface and probably either is unconfirmed or is a fissure-block aquifer. It consists of four relatively thin zones of mod erately (?) to very fractured rock separated by thin to thick intervals of unfractured to sparsely fractured rock, some of which contain large matrix permeability (fig. 7). Fractures, some of which are open, are shallow to vertical and diversely oriented, although many are north- or south-striking. A parting at the contact between the Prow Pass and Bullfrog Members of the Crater Flat Tuff occurs near the bottom of the aquifer. In the upper part of the aquifer (transmissive intervals IV and V), a small outflow from borehole UE-25c #3 is transmitted toward borehole UE-25c #1, and a small outflow from borehole UE-25c #1 is transmitted toward borehole UE-25c #2. Lower in this part of the aquifer, these inflows leave boreholes UE-25c #1 and UE-25c #2 through fractures. In the middle part of the aquifer (transmissive interval VI), small outflows from boreholes UE-25c #2 and UE-25c #3 are transmitted by fractures, the rock matrix, and the parting at the Prow Pass - Bullfrog contact toward borehole UE-25c #1. At the bottom of the aquifer (transmissive interval VII), small outflows to fractures occur in all of the c-holes. Seven percent of the discharge from borehole UE-25c #2 during a pumping test in March 1984 came from this aquifer.
Bullfrog Aquifer
The Bullfrog aquifer extends from about 2,370 to 2,660 ft below land surface and is confined by more than 100 ft of overlying unfractured to sparsely frac tured, moderately to densely welded tuff (fig. 7). The aquifer consists mostly of moderately to very fractured rock with thin intervals of unfractured to sparsely frac tured rock, but the lower 50 ft of the aquifer in borehole
UE-25c #3 is sparsely to moderately fractured. The upper part of the aquifer (transmissive interval VIII) contains large matrix permeability. Fractures, most of which are open, are shallow to vertical, and diversely oriented. In the upper part of the aquifer, small to large outflows from boreholes UE-25c #2 and UE-25c #3 are transmitted toward borehole UE-25c #1. In the lower part of the aquifer (transmissive interval IX), all down ward flow and all remaining upward flow from lower in borehole UE-25c #1 are lost through fractures; small to large outflows from boreholes UE-25c #2 and UE-25c #3 occur, as well. Sixty-four percent of the discharge from a pumping test in borehole UE-25c #1 in September 1983,93 percent of the discharge from a pumping test in borehole UE-25c #2 in March 1984, and 75 percent of the discharge from a pumping test in borehole UE-25c #3 in May-June 1984 came from this aquifer.
Tram Aquifer
The Tram aquifer extends from about 2,660 ft below land surface to the bottom of the c-holes and is confined. However, leakage occurs from two faults that transect this aquifer. The aquifer consists almost entirely of moderately to very fractured rock (fig. 7). Fractures, many of which are open, are shallow to ver tical and diversely oriented. At the top of the aquifer (transmissive interval X), all downward flow and all remaining upward flow from lower in the borehole are lost from borehole UE-25c #2 and are transmitted toward boreholes UE-25c #1 and UE-25c #3. In the lower part of the aquifer (transmissive interval XI), small to large upward flows enter the c-holes. Thirty- six percent of the discharge from a pumping test in borehole UE-25c #1 in September 1983 and 25 percent of the discharge from a pumping test in borehole UE-25c #3 in May-June 1984 came from this aquifer.
FLUID-INJECTION TESTS
Twenty-six fluid-injection tests were conducted in the c-holes in 1983 and 1984. In October 1983, 16 falling-head (slug) tests and nine pressure-injection tests were conducted in borehole UE-25c #1. In October 1984, a constant-head injection test was con ducted in borehole UE-25c #2 using boreholes UE-25c #1 and UE-25c #3 as observation wells. The constant-head test, soon after it began, developed into a constant-flux test and is discussed later in this report with pumping tests conducted in the c-holes.
20 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
Falling-Head Tests
Falling-head tests conducted in borehole UE-25c #1 are listed in table 7, which indicates that test intervals were successively reduced from 160 to 40 to 22 ft, except near the top and bottom of the borehole, where test interval thicknesses were determined partly by the bottom of the concrete and the bottom of the borehole. As shown in figure 8, tests intervals were isolated by TAM International inflatable packers, mon itored primarily by contractor-supplied Kuster and Speny-Sun pressure and temperature gauges above, between, and below the packers, and monitored sec ondarily by a USGS-supplied Bell and Howell pres sure-transducer suspended inside the 2.26-in.-inside diameter plastic riser pipe above the packer string. For all tests except test 1, the transducer was set at 1,370 ft below the top of the riser pipe; for test 1, it was set at 1,330 ft below the top of the pipe.
According to Devin L. Galloway (USGS, oral commun., 1993), the contractor-supplied gauges, with pressure ranges of 0 to 2,150 lb/in.2 and 0 to 5,000 lb/in.2 (Tarn International, written commun., 1983), were insensitive to small changes in head that are common to aquifer tests. Moreover, because of a recording interval of 2 min, these gauges missed the initial head in some tests, and in very permeable inter vals, the gauges missed most or all of the head recov ery. The USGS-supplied pressure transducer, with a pressure range of 0 to 500 lb/in.2 and a minimum recording interval of eight seconds, was considered more reliable for data collection and analysis than the contractor-supplied gauges. Consequently, only the pressure-transducer data for the falling-head tests were analyzed.
An additional problem with the design of the falling-head tests was the large column of water injected into borehole UE-25c #1 during the tests. As indicated in table 7, initial injected heads in these tests ranged from 592 to 1,022 ft above the static water level, averaging about 700 ft. Galloway (USGS, written commun., 1986) reported that calculations for a repre sentative test conducted in a permeable zone indicate that a head loss of 35 to 40 percent probably occurred during the falling-head tests as a result of friction between the injected water as it descended and the riser pipe. Although early-time recovery data could have been affected by any initial head loss to friction, later recovery data probably would not have been affected. Consequently, the later-time recovery data were emphasized in analyzing these tests.
The commonly used method for analyzing falling-head tests, in a confined aquifer, is that of Cooper and others (1967), which assumes radial flow
to a fully penetrating well in a homogeneous, isotropic, compressible aquifer. Reed (1980) presents type curves of the well function for the analytical solution of Cooper and others (1967). As pointed out by Cooper and others (1967), matching data curves with the type curves can provide a good determination of transmis- sivity, whereas the determination of storativity is not reliable because of the similar shape of the type curves. Barker and Black (1983) indicate that the solution of Cooper and others (1967) can be applied successfully to formations with very low storativity and to fractured rock, provided that there is no exchange of water between fractures and the rock matrix and that fracture apertures are not changed by the pressure of the injected water column. However, Barker and Black (1983) state that even where water is derived from frac tures and the rock matrix, a situation commonly termed a "dual-porosity" aquifer, transmissivity determined by the method of Cooper and others (1967) will be under estimated by a factor of no more than 2-3. This poten tial error generally would be considered insignificant in a complicated hydrogeologic environment, such as the c-hole complex, where one might expect transmissivity calculations to be within an order of magnitude of actual values. Barker and Black (1983) cautioned against using the method of Cooper and others (1967) to determine storativity in a dual-porosity aquifer, because the method can underestimate storativity by a factor of as large as 0.000001. Because of large poten tial error, storativity was not determined from the falling-head tests in borehole UE-25c #1.
In the solution of Cooper and others (1967), values of the ratio of injected head at time t to initial injected head (H/H0) are plotted against time elapsed since the injection of fluid occurred. A match between the data curve and a type curve plot of H/H0 as a func
tion of 6 = Tt/rc2 gives a value of a = rs2/rc2 x S, 6, and time, where,
T = transmissivity (L2/T);rc = radius of casing (plastic riser pipe in
UE-25c #1) in which water level fluctuates (L);
rs = radius of open hole (L);t = time (T); andS = storativity (dimensionless).
Transmissivity is found by picking a match point where 6=1 and solving the equation:
(2)
On the basis of the solution of Cooper and others (1967), falling-head tests in borehole UE-25c #1 indi cated transmissivity values for tested intervals that
FLUID-INJECTION TESTS 21
I! ft ? Q
.Z
3
» -3 jr § a I 3 g 2 .0 i 1 5" CD
O 3 8 c io C m IS
) » a» E.
Test
num
be
r 1 2 3 4 6 7 10 12 15 16 17 18 19 20 21 26
> i
i<7ouuo
in
ic
ani
Tes
t Int
erva
lde
pth
(fee
t)
1,37
1-1,
515
1,68
5-1,
845
1,86
5-2,
025
2,05
0-2,
210
2,61
0-2,
770
2,78
0-2,
995
1,80
5-1,
845
1,90
0-1,
940
2,55
5-2,
595
2,74
6-2,
786
2,81
8-2,
858
2,88
0-2,
920
2,93
0-2,
995
2,44
5-2,
467
2,47
6-2,
498
2,60
7-2,
995
III^
-|I9
CIV
J 19919
V/V
/I I
VJU
Vsl
9V
I II
I U
V/I
91 I
V/1
9
V/l
_-£
.v^V
y
W I,
\^V
sl\
SW
9l
\J
!£.,
1 W
*J
Geo
logi
c de
scri
ptio
n of
test
Int
erva
l
Unf
ract
ured
to s
pars
ely
frac
ture
d, n
onw
elde
d an
d be
dded
tuff
with
thin
inte
rval
s th
at a
rem
oder
atel
y fr
actu
red
Unf
ract
ured
to v
ery
frac
ture
d, n
onw
elde
d to
mod
erat
ely
wel
ded
tuff
Unf
ract
ured
to v
ery
frac
ture
d, n
onw
elde
d to
par
tially
wel
ded
tuff
Unf
ract
ured
to v
ery
frac
ture
d, b
edde
d an
d no
nwel
ded
to p
artia
lly w
elde
d tu
ffU
nfra
ctur
ed to
ver
y fr
actu
red,
non
wel
ded
to p
artia
lly w
elde
d tu
ffV
ery
frac
ture
d tu
ff b
recc
ia a
nd tu
ff w
ithin
Unf
ract
ured
inte
rval
sV
ery
frac
ture
d, n
onw
elde
d to
mod
erat
ely
wel
ded
tuff
Unf
ract
ured
and
ver
y fr
actu
red,
non
wel
ded
to p
artia
lly w
elde
d tu
ffM
oder
atel
y to
ver
y fr
actu
red,
non
wel
ded
to p
artia
lly w
elde
d tu
ffV
ery
frac
ture
d, n
onw
elde
d to
par
tially
wel
ded
tuff
and
tuff
bre
ccia
Unf
ract
ured
and
ver
y fr
actu
red
tuff
bre
ccia
Ver
y fr
actu
red
tuff
bre
ccia
Unf
ract
ured
and
ver
y fr
actu
red
tuff
bre
ccia
and
par
tially
wel
ded
tuff
Mod
erat
ely
to v
ery
frac
ture
d, m
oder
atel
y to
den
sely
wel
ded
tuff
Ver
y fr
actu
red,
par
tially
to d
ense
ly w
elde
d tu
ffM
ostly
mod
erat
ely
to v
ery
frac
ture
d, n
onw
elde
d to
par
tially
wel
ded
tuff
and
tuff
bre
ccia
Stat
icw
ater
leve
l(f
eet
belo
wla
ndsu
rfac
e)
1,31
4
1,31
31,
313
1,31
31,
314
1,31
21,
314
1,31
21,
314
1,31
31,
314
1,31
31,
314
1,31
31,
314
1,31
4
initi
alhe
adab
ove
stat
icw
ater
leve
l(f
eet)
649
638
699
728
656
750
705
666
784
592
792
822
1,02
268
366
686
9
Dur
atio
n4
*4
Of
reco
very
(min
utes
)
41 84 243
422
100 13 111
281 2.
7512 70 41 11
6 87 35 12.5
Tran
s-m
lssl
vlty
(fee
tsq
uare
per d
ay)
20 10 0.8
10 8 40 4 0.3
80 20 10 20 5 9 10 50
Hyd
raul
icco
nduc
tiv
ity(f
eet p
erda
y)
0.1
0.07
0.00
50.
080.
050.
20.
10.
008
2 0.5
0.3
0.5
0.08
0.4
0.6
0.1
I s 8 I I
Logging truck with Fluke digital and analog recorders
Valve Cable-Rig floor Ground
Riser pipe
Casing
Concrete
Inflated packer
Inflated packer
Injected water
Static water level
Pressure transducer
Open hole
Recorder carrier and guages
Recorder carrier and guages
Test interval, pipe slotted
Recorder carrier and guages
NOT TO SCALE
Figure 8. Design configuration of falling-head tests in borehole UE-25c #1, October 1983.
FLUID-INJECTION TESTS 23
ranged from 0.3 to 80 ft2/d (table 7). Assuming that head is dissipated uniformly throughout tested inter vals, and not through preferred pathways, such as frac tures and partings, then dividing transmissivity by test interval thickness provides estimates of hydraulic con ductivity for the tested intervals. Estimated values of hydraulic conductivity from the falling-head tests, range from 0.005 to 2 ft/d (table 7 and fig. 9).
Values of transmissivity and hydraulic conduc tivity calculated using the method of Cooper and others (1967) are considered reasonable because:
1. In all tests, there was fair to good agreementbetween data curves and type curves. There was no systematic improvement in curve matching for intervals with less fracturing and, presumably, more dependence on matrix flow (fig. 10). Therefore, one can conclude that the presence of fractures in a test interval generally did not invalidate the fundamental assumption of radial flow through a homogeneous, isotro- pic aquifer.
2. In the three sections of the borehole where multi ple tests were conducted, 1,685 to 1,845 ft, 1,865 to 2,025 ft, and 2,607 to 2,995 ft, tests of successively smaller intervals produced suc cessively smaller values of transmissivity, the sum of which did not exceed the transmissivity of the larger test interval (fig. 10). Transmis sivity is additive and should increase with increasing test-interval thickness.
One problem common to all of the falling-head tests conducted in borehole UE-25c #1 is the small to large divergence between the late-time recovery data and the tail of the type curve to which the data curve was matched (fig. 9). Analytical solutions invoking different conceptual flow models than that of Cooper and others (1967) were tried to provide more precise determinations of transmissivity (Devin L. Galloway, USGS, written commun., 1986). A linear flow model, which simulates flow in and perpendicular to fracture planes, produced a poorer solution because type curves are much flatter than those of Cooper and others (1967). Imposing a linear or radial constant-head boundary at some variable distance from borehole UE-25c #1, simulating radial flow through a borehole skin (although not justified by the drilling technique), or considering spherical flow through the test interval, all produced type curves and tails steeper than those of Cooper and others (1967), but less steep than the data curves. None of the alternative analytical solutions were considered substantially more accurate or con
ceptually more realistic than the method of Cooper and others (1967). Consequently, calculations using only the method of Cooper and others (1967) are presented in this report.
Pressure-Injection Tests
Pressure-injection tests conducted in borehole UE-25c #1 are listed in table 8, which indicates that test intervals were 22,40, or 160 ft. Some of the tests were planned for intervals thought to have small permeabil ity (Devin L. Galloway, USGS, oral commun., 1993), but most of the tests were changed from falling-head tests after a few minutes of extremely slow gravity drainage (USGS, unpublished log book for borehole UE-25c #1). Four of the tests could not be analyzed because of apparent mechanical problems and insuffi cient or unreliable data.
The pressure-injection tests were designed simi larly to the falling-head tests (fig. 8), except that a valve in the water line was closed during the pressure- injection tests to isolate the test interval from atmo spheric pressure. With the system pressurized (shut in), the pressure transducer used in the falling-head tests would have no hydraulic connection to the test interval and, therefore, could not be used (see fig. 8). The Sperry-Sun gauge, which provided digital output at two-minute intervals, produced the primary record for the pressure-injection tests. The procedure for the pressure-injection tests (Neuzil, 1982) consisted of the following steps:
1. The valve in the water line was opened, and a slug of water was released into the borehole;
2. The test interval was shut in by closing the valve in the water line;
3. Pressure decay in the test interval was monitored until pressure was constant or nearly constant;
4. The control valve was opened briefly, and another slug of water was released into the borehole;
5. The control valve was closed, again shutting in the test interval;
6. Pressure in the test interval again was allowed to decay to a constant or nearly constant level; and
7. The control valve was opened, and pressure on the system was released.
The pressure-injection tests were analyzed by the method of Bredehoeft and Papadopulos (1980), as
24 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
0.8
0.6
0.4
X X
O Z P O
DC ^UJ u_t O< uu
§1
0.2 -
00.01
0.8
0.6
0.4
0.2
TEST1
1,371 - 1,515 feet
cc=10- 1 °
0.1 100
EXPLANATION
o DATA POINT REPRESENTING THE RATIO OF HEAD WITH TIME SINCE FLUID INJECTION TO INITIAL HEAD
TYPE CURVE MATCHED TO DATA POINTS
I = TIME AT Tt'rc2 =1.0, IN MINUTES
T = TRANSMISSIVITY, IN FEET SQUARED PER DAY
t = TIME, IN MINUTES
rc = RADIUS OF ftlSER PIPE, IN FEET
a = A DIMENSIONLESS PARAMETER RELATED TO STORATIVITY
i i i i i i r
TEST 21,685- 1,845 feet
0.01 0.1 100
TIME IN MINUTES, SINCE INJECTION
Figure 9A. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
FLUID-INJECTION TESTS 25
0.8
0.6
0.4
X 0.2
O 2I- O0 P^ O
=10-1
EXPLANATION
o DATA POINT REPRESENTING THE RATIO OF HEAD WITH TIME SINCE FLUID INJECTION TO INITIAL HEAD
TYPE CURVE MATCHED TO DATA POINTS
I =TIME AT Tt/rc2 =1.0, IN MINUTES
T = TRANSMISSIVITY, IN FEET SQUARED PER DAY
t = TIME, IN MINUTES
rc = RADIUS OF 6lSER PIPE, IN FEET
a = A DIMENSIONLESS PARAMETER RELATED TO STORATIVITY
0.01 0.1 10
t O< LU
0.01 1 10
TIME IN MINUTES, SINCE INJECTION
TESTS 1,865-2,025 feet
100 1,000
100 1,000
Figure 9B. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
26 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
0.8
0.6
0.4
II
IIZo zP O0 =
i > *-
t o< LLJ
< QQ <
0.2
TEST 62,610-2,770 feet
0.01
0.8
0.6
0.4
0.2
0.01
0.1
a=lO-10
a=10- 10EXPLANATION
o DATA POINT REPRESENTING THE RATIO OF HEAD WITH TIME SINCE FLUID INJECTION TO INITIAL HEAD
TYPE CURVE MATCHED TO DATA POINTS
I = TIME AT Tt/rc2 =1.0, IN MINUTES
T = TRANSMISSIVITY, IN FEET SQUARED PER DAY
t = TIME, IN MINUTES
rc = RADIUS OF ftlSER PIPE, IN FEET
a = A DIMENSIONLESS PARAMETER RELATED TO STORATIVITY
10 100
TEST 7
2,780 - 2,995 feet
0.1 1
TIME IN MINUTES, SINCE INJECTION
10 100
Figure 9C. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
FLUID-INJECTION TESTS 27
0.01
100
1 10
TIME IN MINUTES, SINCE INJECTION
100 1,000
Figure 9D. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
28 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
0.8
CE £:UJ u_t o< LU
0.01
100
1
TIME IN MINUTES, SINCE INJECTION
10 100
Figure 9E. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
FLUID-INJECTION TESTS 29
0.01
TEST 172,818-2,858 feet
1
TIME IN MINUTES, SINCE INJECTION
10 100
Figure 9F. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
30 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25C #1, UE-25C #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
100
0.01 0.1 1
TIME IN MINUTES, SINCE INJECTION
100
Figure 9G. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
FLUID-INJECTION TESTS 31
100
0.1
TIME IN MINUTES, SINCE INJECTION
10 100
Figure 9H. Analyses of falling-head tests in borehole UE-25c #1, October 1983, assuming an infinite, homogeneous, isotropic, confined aquifer (symbols on plots explained in text).
32 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
FRAPTI IRF TEST INTERVAL AND STRATIGRAPHY ^NF<T CALCULATED TRANSMISSIVITY,
zui\itt> |N FEET SQUARED PER DAY
1,300 -
1,400 -
1,500 -
1,600 -
1,700 -
1,800 -
LULU"- 1,900 -
LU 0< 2,000 - CC D W Q 2,100 -
O 2,200 -
LU QQ
£ 2,300 -LUQ
2,400 -
2,500 -
2,600 -
2,700 -
2,800 -
2,900 -
3 nnn
BOTTOM OF CONCRETE CAS
CRATER FLAT TUFF TUFFS AND LAVAS
) J Ut- UALIUU MILLb
BULLFROG MEMBER ( PROW PASS MEMBER (
TRAM MEMBER
NONWELDED
BEDDED
^^^S~^ S^*^S~^^S1~^ S^^ S~**-S' N^*"-. f
NONWELDED TO PARTIALLY WELDED
MODERATELY WELDED
PARTIALLY WELDED TO NONWELDED
BEDDEDs **~s-^-S-^^ s~* s~*^s~*^s-^~s ^-s~
NONWELDED TO PARTIALLY WELDED
MODERATELY TO DENSELY WELDED
PARTIALLY WELDED TO NONWELDED
BEDDED
NONWELDED TO PARTIALLY WELDED
TUFF BRECCIA
NG
H
BY//////S
'////////
i^M '///////,
y///////,
m%.
i_,i~
-
;PARTIALLY WELDED 1
20
10
i 5 i
U.o
10
9
=_ __!
80
8
i- - ' 20 [
- 50
10 |
40 20 |
5i
EXPLANATION
UNFRACTUREDTO SPARSELY FRACTURED
MODERATELY FRACTURED
VERY FRACTURED
GEOLOGIC CONTACT
GEOLOGIC CONTACT WITH OPEN PARTING
FALLING HEAD TEST Solid if good match between data and type curves; dashed if fair match
Figure 10. Falling-head tests and transmissivity values obtained in relation to geology, borehole UE-25c#1.
FLUID-INJECTION TESTS 33
ada
Tab
le 8
. R
esul
ts o
f pr
essu
re-in
ject
ion
test
s co
nduc
ted
in b
oreh
ole
UE
-25c
#1
, Oct
ober
6-1
2,
1983
[n.a
., te
st n
ot a
nalyz
ed b
ecau
se o
f ins
uffic
ient
or u
nrel
iabl
e da
ta; n
.s.,
no s
olut
ion
dete
rmin
ed]
2. I 1 g 2 g I H | 5" 00 o § 1 (0 c s » c "71 to js n & C "71 to VI o
Tes
t nu
mbe
r
5 8 9 11 13 14 22 23 25
Tes
t int
erva
l de
pth
(fee
t)
2,27
0-2,
430
1,52
5-1,
565
1,63
4-1,
674
1,87
0-1,
910
1,94
0-1,
980
2,21
5-2,
255
2,49
8-2,
520
2,57
5-2,
597
2,50
8-2,
530
Geo
logi
c de
scrip
tion
of te
st in
terv
al
Unf
ract
ured
, mod
erat
ely
to d
ense
ly, w
elde
d tu
ff w
ith th
infr
actu
red
inte
rval
sU
nfra
ctur
ed a
nd v
ery
frac
ture
d, n
onw
elde
d tu
ffSp
arse
ly fr
actu
red,
bed
ded
tuff
Ver
y fr
actu
red,
non
wel
ded
to p
artia
lly w
elde
d tu
ffU
nfra
ctur
ed to
ver
y fr
actu
red,
non
wel
ded
to p
artia
llyw
elde
d tu
ffU
nfra
ctur
ed a
nd v
ery
frac
ture
d, n
onw
elde
d to
par
tially
wel
ded
tuff
Unf
ract
ured
and
ver
y fr
actu
red,
non
wel
ded
to p
artia
llyw
elde
d tu
ffU
nfra
ctur
ed to
ver
y fr
actu
red,
non
wel
ded
to p
artia
llyw
elde
d tu
ffSp
arse
ly to
mod
erat
ely
frac
ture
d, n
onw
elde
d to
par
tially
wel
ded
tuff
Rec
orde
d he
ad
(pou
nds
per
squa
re
inch
)
n.a.
388.
6555
2.97
n.a.
567.
31
550.
17
n.a.
922.
52
n.a.
Ant
eced
ent
head
(p
ound
s pe
r squ
are
inch
)
n.a.
142.
2839
7.35
n.a.
315.
09
389.
36
n.a.
544.
63
n.a.
Res
idua
l he
ad
(pou
nds
per
squa
re
inch
)
n.a.
246.
3715
5.62
n.a.
252.
22
160.
81
n.a.
377.
89
n.a.
Dur
atio
n of
pr
essu
re
deca
y (m
inut
es)
n.a. 96 98 n.a. 78 34 n.a. 96 n.a.
Tran
s-
mis
sitiv
lty
(fee
t sq
uare
d pe
r day
)
n.a.
n.s. 1
n.a. 6 10 n.a. 10 n.a.
Hyd
raul
ic
cond
uctiv
ity
(fee
t per
da
y)
n.a.
n.s. 0.03
n.a. 0.
2
0.3
n.a. 0.
4
n.a.
«
modified by Neuzil (1982). Assumptions of this method are the same as those discussed previously for the falling-head tests. In this method, pressure decay at the end of the first shut-in period is extrapolated to establish unambiguously an antecedent pressure trend before the second shut-in period. Antecedent pressure is subtracted from pressures recorded during the sec ond shut-in period, and the residual pressure decay is analyzed. If a, as defined previously, is less than or equal to 0.1, then transmissivity is calculated from equation 2 (Cooper and others, 1967). If a is between 0.1 and 10, the product of transmissivity and storativ- ity, TS, can be calculated from the following equations (Bredehoeft and Papadopulos, 1980; Neuzil, 1982):
2nr TSt s
(3)
and
AV/V\v'obsAP
(4)
where,
pw = density of water (M/L3); g = gravitational acceleration (L/T2); Vw = volume of water in pressurized interval (L3); AV = injected volume of water (L3); and AP = pressure pulse resulting from injected
volume of water (M/L2).
At values of a greater than 0.1, transmissivity can be calculated if the storativity can be determined inde pendently.
The five pressure-injection tests that could be analyzed, all had in common a downward bulge in the middle-time data on a semi-log plot of head recovery as a function of time. This bulge made it impossible to match the data curve for test 8 to any type curve. For test 9, a questionable match was made between the data and type curves. For tests 13,14, and 23, the bulge was small enough that a fairly reliable match could be made between data curves and type curves (fig. 11).
The reason for the downward bulge in the data curves is unknown. It could be an artifact of the coarse recording interval of the Sperry-Sun gauge (two min utes), or it could indicate a problem in the mechanical set-up. A transmissivity value obtained from test 13 that is substantially larger than would be expected from a falling-head test conducted in an interval that includes the one in which test 13 was run seems to indi cate that pressures applied could have opened fracture apertures in some pressure-injection tests. This would
violate one of the fundamental assumptions of the test method, that fracture apertures are independent of pres sure, and would invalidate the results of any tests thus affected. The transmissivity value obtained from test 13 was considered invalid because of possible "hydrofracturing".
Only tests 9,14, and 23 were considered to have produced reasonable values of transmissivity and hydraulic conductivity. Transmissivity values in tests 9,14, and 23 ranged from 1 to 10 ft2/d, and hydraulic conductivity values in these tests ranged from 0.03 to 0.4 ft/d (table 8).
The results of the falling head and pressure injec tion tests were combined to extrapolate the hydraulic conductivity distribution within a small radius of bore hole UE-25c #1. As shown in figure 12, hydraulic con ductivity in the vicinity of borehole UE-25c #1 was estimated to range from 0.005 to 0.6 ft/d. The average hydraulic conductivity in the horizontal direction was estimated to be 0.2 ft/d, whereas the average hydraulic conductivity in the vertical direction was estimated to be 0.02 ft/d.
On the basis of the hydraulic conductivity distri bution, the transmissivity distribution within a small radius of borehole UE-25c #1 was estimated for aqui fers and the entire thickness of rocks in the open part of the borehole (fig. 12). The Calico Hills aquifer was estimated to have a transmissivity of 22 ft2/d; the Prow Pass-upper Bullfrog aquifer was estimated to have a transmissivity of 34 ft2/d; the Bullfrog aquifer was estimated to have a transmissivity of 152 ft2/d; and the Tram aquifer was estimated to have a transmissivity of 44 ft2. The composite transmissivity of rocks below casing and concrete in borehole UE-25c #1 was esti mated to be 261 ft2. As discussed later in the report, the composite transmissivity value obtained from fluid- injection tests in borehole UE-25c #1 virtually is iden tical to the composite transmissivity value obtained by pumping borehole UE-25c #3.
CONSTANT-FLUX TESTS
Five pumping tests and a constant-flux injection test were conducted in the c-holes between September 1983 and December 1984. With the completion of each additional borehole at the c-hole complex, the monitoring network for these constant-flux tests was expanded, the conceptual model of ground-water flow at the c-hole complex was refined, and test compo nents, such as the rate of flux, the duration of fluid injection or withdrawal, and the length of time that recovery was monitored, were changed in accordance with information learned from previous tests. The design of these tests, problems encountered, possible
CONSTANT-FLUX TESTS 35
0.8
0.6
0.4
0.2
0.1
to< LU
I- << QQ << ^LU ^
nRO.o
0.6
0.4
0.2
0.1
EXPLANATION
o DATA POINT REPRESENTING THE RATIO OF HEAD WITH TIME SINCE FLUID INJECTION TO INITIAL HEAD
TYPE CURVE MATCHED TO DATA POINTS
I = TIME ATTt/rc2 =1.0, IN MINUTES
T = TRANSMISSIVITY, IN FEET SQUARED PER DAY
t = TIME, IN MINUTES
rc = RADIUS OF ftlSER PIPE, IN FEET
a = A DIMENSIONLESS PARAMETER RELATED TO STORATIVITY
0=10-""
10
TEST 91,634- 1,674 feet
100
TEST 131,940-1,980 feet
1 10
TIME, IN MINUTES, SINCE INJECTION
100
Figure 11 A. Analyses of pressure-injection tests conducted in borehole UE-25c #1, October 1983, assuming an infinite, homo geneous, isotropic, confined aquifer (symbols on plots are explained in the text).
36 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
0.8 -
TEST 142,215-2,255 feet
EXPLANATION
o DATA POINT REPRESENTING THE RATIO OF HEAD WITH TIME SINCE FLUID INJECTION TO INITIAL HEAD
TYPE CURVE MATCHED TO DATA POINTS
I =TIME ATTt/rc2 =1.0, IN MINUTES
T = TRANSMISSIVITY, IN FEET SQUARED PER DAY
t -= TIME, IN MINUTES
rr = RADIUS OF filSER PIPE, IN FEET
a = A DIMENSIONLESS PARAMETER RELATED TO STORATIVITY
TEST 232,575 - 2,597 feet
0.2 -
100
1 10
TIME, IN MINUTES, SINCE INJECTION
100
Figure 11 B. Analyses of pressure-injection tests conducted in borehole UE-25c #1, October 1983, assuming an infinite, homo geneous, isotropic, confined aquifer (symbols on plots are explained in the text).
CONSTANT-FLUX TESTS 37
LLJ O
1,200
1,300
1,400
1,500
1,600
1,700
1,800
1,900
2,000
2,100
2,200
2,300
2,400
2,500
2,600
2,700
2,800
2,900
j nnn
AQUIFER
; , BOTTOM
CALICOHILLS
-
~ PROW PASS- UPPER
r BULLFROG
- BULLFROG
; TRAM
HYDRAULIC CONDUCTIVITY (FEET PER DAY)
OF CONCRETE ANC
0.1
0.03
0.05
0.1
0.008
0.003
0.08
0.3
0.005
0.005
0.4
0.6
2 ,0.4
0.04
0.06
0.08
0.1
TRANSMISSIVITY (FEET SQUARED
PER DAY)
CASING ;
22 !
6 ;
34
1 ;
152
2 !
44 ;
Figure 12. Transmissivity and hydraulic conductivity distribu tions within a small radius of borehole UE-25c #1, estimated from falling-head and pressure-injection tests.
38 Results and Interpretation off Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
ground-water flow models that explain hydraulic head changes with time during the tests, and ranges in hydrologic properties calculated on the basis of analy tical solutions for different possible ground-water flow models are presented in this section of the report. For a general discussion of the principles of aquifer tests, the reader is referred to Lohman (1979) and Driscoll (1986).
Analytical Methods
Constant-flux tests conducted at Yucca Moun tain, including tests conducted in the c-holes discussed later in this section, rarely produce a transient response characteristic of an infinite, homogeneous, isotropic, confined aquifer the exponential-integral curve of Theis (1935). As indicated by Robison and Craig (1991), plots of the log of water-level change as a func tion of the log of time typically result in a two-humped curve or a curve that flattens out. Additionally, the early-time data are characterized by borehole storage effects (Gringarten, 1982), and the late-time data com monly contain oscillations that Galloway and Rojstaczer (1988) attributed to Earth tides and changes in atmospheric pressure. In this report, constant-flux tests in the c-holes are interpreted with respect to four analytical ground-water models: (1) An infinite, homogeneous, isotropic, confined aquifer (Theis, 1935; Cooper and Jacob, 1946); (2) a leaky, homoge neous, isotropic, confined aquifer (Cooper, 1963); (3) a fissure-block (dual-porosity) aquifer (Streltsova-Adams, 1978); and (4) an infinite, homoge neous, anisotropic, unconfined aquifer (Neuman, 1975). The four analytical models used were selected because of their applicability to hydrogeologic charac teristics of the c-hole complex discussed previously in this report.
Under the assumption of an infinite, homoge neous, isotropic, confined aquifer, water-level changes in observation wells are plotted as a function of time on log-log paper and matched to the exponential-integral type curve of Theis (1935). The following equations are used to calculate hydrologic properties:
T=
and
4ns
= T/b
_ 4Tt\l
(5)
(6)
(7)
where,
T = transmissivity (L2/T); Q = rate of injection or withdrawal (L3/T);
W(\i) = well function for an infinite, homogeneous,isotropic, confined aquifer (also called theexponential integral);
\i = a dimensionless parameter defined byequation 7;
Kr = horizontal hydraulic conductivity (L/T); b = thickness of transmissive intervals (L); S = storativity (dimensionless); t = time since injection or withdrawal started or
stopped (T) corresponding to fi; s = water-level change (L) corresponding to
; andr = distance from the pumped well to an
observation well (L).Under the same assumptions applicable to equa
tions 5, 6, and 7, the transmissivity of rocks in the pumped well can be analyzed by plotting residual drawdown as a function of the log of the ratio of time since injection or withdrawal started to time since injection or withdrawal stopped and solving the follow ing equation (Theis, 1935):
T =_ 2.3 Q t
d(8)
where:
AJ ' = the residual water-level change (L) over one log
cycle of the ratio of time since injection or withdrawal started to time since injection or withdrawal stopped; and all other variables are defined as in equation 5.
Flattening of a plot of the log of drawdown in the pumped well or an observation well as a function of the log of time can be interpreted to indicate induced recharge from an aquifer boundary, as a hydraulic gra dient develops between the boundary and the aquifer in response to pumping. This situation is analogous to leakage from a confining unit without storage during pumping. Analysis of drawdown in an aquifer with leakage from a confining unit without storage, accord ing to Cooper (1963), is done by plotting the log of drawdown as a function of the log of the ratio of time since pumping started to the distance squared from the pumped well, matching the data curve to one of a fam ily of type curves, and solving the following equations:
T= QxL(\i,v) 4ns (9)
CONSTANT-FLUX TESTS 39
C .._ 4Tt /r
and
v = <x
(10)
(ID
where,
L(ii,v)= well function of an infinite, homogeneous, isotropic, confined aquifer with leakage from a confining unit without storage;
K' = vertical hydraulic conductivity of theconfining unit (L/T);
b' = thickness of the confining unit (L); and v = a dimensionless parameter defined by
equation 11; and all other variables are as defined previously.
The fissure-block model of ground-water flow can be analyzed either by straight-line techniques (Robison and Craig, 1991) or by curve-matching (Streltsova-Adams, 1978). If a pumping test proceeds long enough, a plot of drawdown in an observation well as a function of the log of time since pumping started is characterized by three segments. The first and third segments have twice the slope of the second segment, which is relatively flat. The third segment is analyzed using the following equations (Cooper and Jacob, 1946):
and
2.25 TtS = o
(12)
(13)
where,
As, = drawdown (L) over one log cycle of time;
t0 = time at point of zero drawdown (T); and r = distance from pumped well to observation
well (L); and all other variables are asdefined previously.
If the test is terminated before the third segment is obtained, the second segment is analyzed with the denominator of equation 12 multiplied by 2.
In the curve-matching technique of Streltsova- Adams (1978), the log of drawdown in an observation well as a function of the log of time is plotted and matched to a type curve with a shape determined by the ratio of total storativity to fracture storativity (T|), and
by the ratio of the distance from the pumped well to the parameter B, which is defined by the following equa tion:
D TTT (14)
where,
T H
= transmissivity (L2/T);= the distance from the center of a block to a
bounding fracture, equivalent to half the average distance between fractures (L); and
Kb = hydraulic conductivity of the blocks (L/T).
Matching the data curve to the type curve gives the transmissivity of the aquifer; matching the data curve to the early-time part of the type curve gives the frac ture storativity; substituting the fracture storativity and T| into equation 17 below, gives the block storativity; rearranging equation 14 and solving for Kb gives the block hydraulic conductivity; and dividing transmis sivity by the thickness of transmissive intervals in the test interval gives the average fracture hydraulic con ductivity. The analytical equations are:
r=4ns
Sb = -1)
and
K - Kf~ b
(15)
(16)
(17)
(18)
(19)
where,
W(Q) = well function of a fissure-block aquifer; s = drawdown in fractures (L) corresponding to
W(0);Sf = fracture storativity (dimensionless); 0 = a dimensionless parameter defined by
equation 16; t = time since pumping started (T)
corresponding to 0; Kf = hydraulic conductivity of the fractures
(L/T); Sb = block storativity (dimensionless); and all
other variables are as defined previously.
40 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
Because the type curves are very similar, esti mating r/B in advance of curve-matching is recom mended. In analyzing the c-hole pumping tests, values of r/B were estimated using the fracture data in the Supplementary Data section of this report, values of matrix permeability shown on pis. 1-3, and values of transmissivity estimated from plots of drawdown or recovery during aquifer tests as a function of the log of time. Hydraulic conductivity (K), in feet per day, was estimated from matrix permeability (k), in millidarcies by the following equation:
where,
K = (20)
where,
\i = the dynamic viscosity of water(in centipoise); and
p w and g are defined as in equation 3.The final analytical model considered in this
report is an infinite, homogeneous, anisotropic, uncon- fined aquifer (Neuman, 1975). The method of analysis requires plotting the log of drawdown or recovery in either the pumped well or an observation well as a function of the log of the ratio of time since pumping started or stopped to distance squared from the pumped well and matching the data curve to a type curve that consists of two relatively steep segments (Type A and Type B curves) separated by a relatively flat transi tional segment. The shape of the transitional curve is related to the anisotropy of the aquifer. Matching the data curve to either the early-time or late-time part of a type curve gives the transmissivity; matching the data curve to the early-time part of a type curve gives the storativity; and matching the data curve to the late-time part of a type curve gives the specific yield. Hydro- logic properties are calculated using the following equations:
r =
= well function for an unconfinedaquifer;
s - drawdown (L) corresponding toW(|iAf JIB.B);
\LA = a dimensionless parameter defined byequation 22;
\LB = a dimensionless parameter defined byequation 23;
t = time since pumping started (T)corresponding to \1A or J1B ;
fi = a dimensionless parameter defined byequation 24;
Sy = specific yield (dimensionless); Kz = vertical hydraulic conductivity (L/T); and
all other variables are as defined previously. To calculate hydrologic properties using the
unconfined aquifer solution of Neuman (1975) first requires estimating the parameter 6, which, in turn, requires estimates of vertical hydraulic conductivity (KJ and horizontal hydraulic conductivity (K,). Initial estimates of IQ and Kj were obtained from values of interval hydraulic conductivity determined from the previously discussed fluid-injection tests in borehole UE-25c #1. The values of hydraulic conductivity determined from the fluid injection tests were inserted into equations given by Freeze and Cherry (1979) for determining average values of vertical and horizontal hydraulic conductivity in rocks with layered hydraulic conductivity. The equations used were:
K = (25)
K.i = i
and
4ns (21) (26)
S =
S =y
r
4Tt\LB
and
K r
Kb'
(22)
(23)
(24)
where:
K{ = hydraulic conductivity of a layer (L/T);fe, = thickness of a layer (L);b = total thickness of layers (L); andn = the number of layers.
In observation wells with packers emplaced to isolate selected intervals, the proportion of discharge contributed from above, between, and below the pack ers in an observation well had to be estimated to solve equations 5,9,15, and 21. The results of heat-pulse flowmeter surveys conducted in the c-holes, that are
CONSTANT-FLUX TESTS 41
shown on plates 1-3, were used to proportionalize dis charge.
Pumping tests with residual head changes from preceding tests or significant recovery (more than about 10 percent of drawdown) caused by a pump fail ure during the test were analyzed applying the principle that the effects of superimposed cycles of fluid injec tion or withdrawal and recovery are additive. The fol lowing equations were used during analysis of a pumping test to separate total recorded drawdown into component parts:
s = ST-SA
rl =S l~ ST
and
(28)
(29)
(30)
where
ST = total recorded drawdown (L);s = drawdown caused by continuous pumping
(L); SA = residual drawdown from a previous aquifer
test (L); Sj = drawdown caused by continuous pumping
or pumping prior to a pump failure (L); s2 = drawdown caused by pumping following a
period during which a pump failure occurred(L);
rj = water-level recovery after shutting off apump following continuous pumping orduring a pump failure (L); and
r2 = water-level recovery following pumpinginterrupted by a pump failure (L).
Values of SA, slt s2, and r7 were estimated beyond the time each was recorded by extrapolation of the slope of the recorded data on a plot of water-level change as a function of the log of time.
Where depths to water were recorded in piezom eters open to the surface, and a recording barometer was operated during an aquifer test, recorded draw down data were corrected for atmospheric pressure changes based on values of barometric efficiency obtained by Galloway and Rojstaczer (1988) from simultaneous records of water levels in the c-holes and borehole UE-25p #1 and atmospheric pressure during 1986. Above packers emplaced between depths of about 2,400 to 2,600 ft, and in open boreholes, a baro metric efficiency of 0.8 was used for the c-holes. Between packers emplaced between 2,400 and 2,600 ft
and below the packers, a barometric efficiency of 0.85 was used for the c-holes. In borehole UE-25p #1 below a packer emplaced 4,255 ft below the land sur face to isolate the Miocene tuffaceous rocks from the Paleozoic carbonate rocks, a barometric efficiency of 0.75 was used. Oscillations in recorded drawdown caused by Earth tides were handled by a visual best-fit match of type curves to curves of drawdown or recov ery through the oscillations.
(27) Pumping Tests in Borehole UE-25c #1
Two unsuccessful pumping tests were conducted in borehole UE-25c #1 in September and October 1983, immediately after completion of the borehole. During each test, borehole UE-25p #1, 2,028 ft south east of the pumped well, was monitored to determine whether the Miocene tuffaceous rocks, and the Paleo zoic carbonate rocks are connected hydraulically in the vicinity of the c-holes. Atmospheric pressure at bore hole UE-25c #1 was recorded on a Validyne digital barometer.
Borehole UE-25c #1 was open during the pump ing tests in the tuffs and lavas of Calico Hills and the Crater Flat Tuff, from the bottom of concrete at a depth of 1,371 ft, to the bottom of the borehole at a depth of 2,995 ft (USGS logbook for borehole UE-25c #1, unpublished). A Centrilift submersible pump was emplaced in the borehole from 1,399 to 1,477 ft below land surface, with the pump intake at 1,416 ft below land surface (Fenix and Scisson, Inc., written com- mun., 1983). A 5.5-in.-outside-diameter riser pipe extended from the pump to the wellhead, where it was coupled to a 6-in.-diameter, steel discharge pipe with an in-line flowmeter and end-line orifice plate and manometer (USGS logbook for borehole UE-25c #1, unpublished). Depth to water in the borehole was mon itored with a Bell and Howell pressure transducer with a recording range of 0 to 50 lb/in.2, that was connected at the surface to a Fluke data logger (USGS logbook for borehole UE-25c #1, unpublished). The calibrated depth of the transducer was 1,423 ft below land surface (110 ft below the static water level in the borehole).
Borehole UE-25p #1 is part of a water-level monitoring network at Yucca Mountain and is perma nently configured to record hydraulic head in the Paleozoic rocks near the c-hole complex (Robison and others, 1988). Borehole UE-25p #1 is cased and grouted through the tuffaceous rocks to a depth of 4,256 ft below land surface (175 ft below the contact between the Miocene and Paleozoic rocks in the bore hole). Hydraulic head in the Paleozoic rocks is recorded with a pressure transducer suspended inside a
42 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
I.9-in.-outside-diameter plastic piezometer tube. Dur ing the pumping tests in borehole UE-25c #1, a Bell and Howell pressure transducer with a recording range of 0 to 10 lb/in.2, that was connected at the surface to a Fluke data logger, was used in the borehole (USGS log book for borehole UE-25c #1, unpublished). The cali brated depth of the transducer was 1,198 ft below land surface, and 7.5 ft below the static water level in the piezometer tube (USGS records, unpublished).
Following several periods of pumping lasting from 10 minutes to 11.5 hours, during which the dis charge rate was varied between 242 and 500 gal/min, equipment to be used in the pumping tests was evalu ated, borehole UE-25c #1 was flushed of drilling debris, and a pumping test was started in borehole UE-25c #1 on September 27,1983. The pump was off for 22 hours prior to the test, and the water level was static when the test began. At an average discharge rate of 234 gal/min, a volume of 1,192,969 gal of water was withdrawn from the pumped well during the test (USGS records, unpublished). Pumping lowered the water level in borehole UE-25c #1 about 100 ft to the pump intake in about 12 minutes, where it remained until pumping ceased on September 30,1983,3.5 days after the test began (USGS records, unpublished). After the pump was shut off, the water level in borehole UE-25c #1 rose abruptly, and residual draw down was negligible 10.3 minutes after pumping ended (USGS records, unpublished).
A second pumping test in borehole UE-25c #1 took place 11 hours after the first pumping test on October 1,1983 (USGS logbook for borehole UE-25c #1, unpublished). During the first 12 minutes of the test, pumping at an average rate of 216 gal/min again lowered the water level in the pumped well to the pump intake (USGS records, unpublished). AfterII.8 hours, the pump failed for about 10 minutes, and the water level in the pumped well recovered 83 per cent (USGS records, unpublished). After the pump was restarted, the water level again decreased rapidly to the pump intake. Pumping continued at an average rate of 213 gal/min for another 19.6 hours until on October 2, the pump was shut off, and the water level in the pumped well again recovered rapidly (USGS records, unpublished).
The pumping tests conducted in borehole UE-25c #1 generally were a failure. Drawdown and recovery in borehole UE-25c #1 could not be analyzed quantitatively, because the depth to water during most of each pumping test was controlled by the depth of the pump intake and not the hydrologic properties of the rocks being tested. Clearly, a smaller capacity pump should have been used for these tests. Both pumping tests in borehole UE-25c #1 were too short to produce
any discernible effect on the water level in borehole UE-25p #1. Thus, neither test could be used to deter mine whether the Miocene and Paleozoic rocks are connected hydraulically in the vicinity of the c-holes.
Pumping Test in Borehole UE-25c #2
A pumping test was conducted in borehole UE-25c #2 in March 1984, several days after comple tion of the borehole. During the test, water levels in the pumped well, in borehole UE-25c #1, 251 ft north- northeast of the pumped well, and in borehole UE-25p #1,1,971 ft east-southeast of the pumped well, were monitored. Atmospheric pressure during the test was recorded on a Validyne digital barometer located at borehole USW H-4,7,466 ft northwest of borehole UE-25c #2.
Procedures and Problems
Borehole UE-25c #2 was open during the pump ing test in the tuffs and lavas of Calico Hills and the Crater Flat Tuff, from the bottom of concrete, at a depth of 1,365 ft, to the bottom of the borehole, at a depth of 2,999 ft (USGS logbook for borehole UE-25c #2, unpublished). A Centrilift submersible pump was emplaced in the borehole from 1,420 to 1,485 ft below land surface, with the pump intake at 1,447 ft below land surface (Fenix and Scisson, Inc., written com- mun., 1984). A 5.5-in.-outside-diameter riser pipe extended from the pump to the wellhead, where it was coupled to a 6-in.-diameter, steel discharge pipe with an in-line flowmeter and end-line orifice plate and manometer (USGS logbook for borehole UE-25c #2, unpublished). Depth to water in the borehole was mon itored with a Bell and Howell pressure transducer with a recording range of 0 to 25 lb/in.2, that was suspended inside a 2.4-in.-diameter access tube and connected at the surface to a Fluke data logger (USGS logbook for borehole UE-25c #2, unpublished). The calibrated depth of the transducer was 1,369 ft below the top of the access tube, 50 ft below the static water level inside the tube (USGS records, unpublished).
Borehole UE-25c #1 was monitored above and between straddle packers suspended on a 2.9-in.- outside-diameter plastic tube between depths of 2,510 and 2,610 ft (Fenix and Scisson, Inc., written commun., 1984). From the bottom of concrete to the top of the packers, borehole UE-25c #1 was open from the Calico Hills aquifer to the top of the Bullfrog aquifer (fig. 7). Between the packers, at depths of 2,520 to 2,600 ft, borehole UE-25c #1 was open in the lower part of the Bullfrog aquifer. Depth to water above the packers was
CONSTANT-FLUX TESTS 43
monitored with a Bell and Howell pressure transducer with a recording range of 0 to 10 lb/in.2, that was con nected at the surface to a Fluke data logger (USGS log book for borehole UE-25c #2, unpublished). The calibrated depth of the transducer to monitor the inter val above the packers was 1,355 ft below the top of cas ing, 20 ft below the static water level in the borehole. Depth to water between the packers was monitored with a Bell and Howell pressure transducer with a recording range of 0 to 25 lb/in.2, that was suspended inside the tube on which the packers were hung and connected at the surface to a Fluke data logger (USGS logbook for borehole UE-25c #2, unpublished). The calibrated depth of the transducer to monitor the inter val between the packers was 1,369 ft below the top of tubing, 50 ft below the static water level inside the tube.
In borehole UE-25p #1, depth to water inside the piezometer tube that was open to the Paleozoic rocks was monitored with a Bell and Howell vented pressure transducer with a recording range of 0 to 15 lb/in.2, that was connected at the surface to a Fluke data logger (USGS logbook for borehole UE-25c #2, unpublished). The calibrated depth of the transducer was 1,205 ft below the top of the piezometer tube, 15 ft below the static water level inside the tube.
Five days prior to the pumping test in borehole UE-25c #2, the borehole was cleaned of debris by repeated cycles of pumping and recovery over a period of five hours. Discharges during this procedure ranged from 321 to 335 gal/min (USGS logbook for borehole UE-25c #2, unpublished). On March 7, 1984, from 0350 to 0423, several attempts were made to begin a pumping test in borehole UE-25c #2, but the longest the pump remained operative during this time was 23 minutes (USGS logbook for borehole UE-25c #2, unpublished).
After complete water-level recovery (USGS records, unpublished) and several modifications to the equipment, a pumping test in borehole UE-25c #2 was started successfully at 1742 on March 7,1984 (USGS logbook for borehole UE-25c #2, unpublished). Pump ing continued until 1029 on March 14,1984 (a period of about 6.7 days). Discharge during the pumping test stabilized within minutes of the pump being started at an average rate of 245 gal/min, and a volume of 2,361,386 gal of water was withdrawn during the test (USGS records, unpublished).
The pumping in borehole UE-25c #2 caused the water level in the pumped well to decrease 8 ft during the first minute of the test; shutting off the pump at the end of the test caused an equally abrupt increase in the water level (fig. 13). Complete recovery to the pre-test static water level in the pumped well occurred 1,165 minutes after pumping ceased. The pumping in
borehole UE-25c #2 drew down water levels in bore hole UE-25c #1 about 1.2 ft above the packers and about 1.4 ft between the packers (fig. 14). Considering the changes in atmospheric pressure during the test (fig. 15), water-level recovery in borehole UE-25c #1, about 3.7 days after pumping ceased, was about 79 per cent complete above the packers and 100 percent com plete between the packers. The pumping in borehole UE-25c #2 apparently caused the water level in bore hole UE-25p #1 to decrease after about 1,000 minutes (fig. 14), indicating that the Miocene tuffaceous rocks and Paleozoic carbonate rocks at the c-hole complex are connected hydraulically. Corrected for changes in atmospheric pressure, the water level in borehole UE-25p #1 decreased 1.4 ft while the pump was on and another 0.5 ft in the 3.7 days that water levels were monitored after the pump was shut off.
Test Analyses
Despite oscillations, drawdown and recovery data from borehole UE-25c #1 above the packers could be interpreted to conform to the analytical solution of either Streltsova-Adams (1978) for a fissure-block aquifer or Neuman (1975) for an unconfined, anisotro- pic aquifer. For both solutions, tuffaceous rocks above the packers were estimated from a heat-pulse flow- meter survey done in December 1991 to contribute 12.5 percent of the discharge from the entire thickness of rocks below casing and concrete in borehole UE-25c#l.
Aquifer-test analysis using the fissure-block solution of Streltsova-Adams (1978) was guided by an estimate of r/B = 0.09 that was obtained from the fol lowing: (1) Half the average distance between frac tures in the interval above the packers = 2.6 ft; (2) log mean matrix hydraulic conductivity in the interval above the packers = 0.0009 ft/d; and (3) a first approx imation-estimate of transmissivity from the slope of the late-time data on a plot of drawdown as a function of the log of time during the pumping test = 3,200 ft2/d. The parameter r/B was calculated as follows:
ITxH210ft = 0.09
3.200/r /dx 2.6ft 0.0009/r/d
Fit to the type curve for r| = 10 and r/B = 0.3, the drawdown data from borehole UE-25c #1 above the packers (fig. 16) indicated the following values of transmissivity (7), fracture storativity (Sy), block stor- ativity (Sb), fracture hydraulic conductivity (Kj), and block hydraulic conductivity (Kb):
44 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
oQ
IQC Q
10
11
12
13
1 I I T
10 11 12
MARCH
13 14 15 16
Figure 13. Drawdown as a function of time in borehole UE-25c #2 during the pumping test in borehole UE-25c #2, March 1984.
-0.5
- 0.5
1.0
1.5
2.0
UE-25c #1, ABOVE PACKERS
UE-25c#1, BETWEEN PACKERS
UE-25p#1
Figure 14. Drawdown as a function of time in boreholes UE-25c #1 and UE-25p #1 during the pumping test in borehole UE-25c #2, March 1984.
28.6
28.5
£ 28.4
28.3
28.2
28.1
28.0
10 11 12 13 14 15 16 17 18
MARCH
19
Figure 15. Atmospheric pressure at borehole USW H-4 during the pumping test in borehole UE-25c #2, March 1984.
10 11 12 13 14 15 16 17 18 19
MARCH
CONSTANT-FLUX TESTS 45
10
1 -
0.1 -
0.01
MATCH POINT
DRAWDOWN DATA
TYPE CURVE MATCHED TO DATA
0.1 10 100
TIME SINCE PUMPING STARTED, IN MINUTES
1,000 10,000
Figure 16. Analytical solution for drawdown data from borehole UE-25c #1 above the packers assuming a fissure-block aquifer, pumping test in borehole UE-25c #2, March 1984.
T =QxW(Q) (0.125x245ga//romx 192.5ft /djxl 2
^ (47IX0.135/0 xlgal/min ~4ns= 3,500ft /d
c _ 4Tt _ 4 x 3 » 500/if /dx 1.35mm _ no, - -T ^ ~ "-r6 (270/0 x 1 x 1, 44Qmin/d
= Sfx (11-1) = 0.0002 x (10-1) = 0.002
r/B = 0.3
__ _ 3,500ft /dx 2.6ft _
B2 (900ft) 2
46 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
Aquifer-test analysis using the unconfined aquifer solution of Neuman (1975) was guided by an estimate of the parameter 6, as follows:
K.
K = 1 ' 139z (40/0.6 + 25/0.4 + 40/0.3 + 209/0.1 + 190/0.08 + 120/0.05 + 145/0.03 + 105/0.008 + 190/0.005 + 75/0.003)
K = 0.0\3ft/d
K =rY +1 £j b
i= 1
_ (40 x 0.6 + 25 x 0.4 + 40 x 0.3 + 209 x 0.1 + 190 x 0.08 + 120 x 0.05 + 145 x 0.03 + 105 x 0.008 + 190 x 0.005 + 75 x 0.003)r ~ 1, 139
Kr = 0.083/r/d
Assuming b is the thickness of transmissive intervals above the packers:2 2
P = -Ll = 0-013/r/Jx (270/Q = Q04
Kb2 0.083/r/d x (524/r) 2
Fit to the type curve for 6 = 0.06, the drawdown and recovery data from borehole UE-25c #1 above thepackers (fig. 17) indicated the following values of transmissivity (7), storativity (S), specific yield (Sy), horizontalhydraulic conductivity, vertical hydraulic conductivity, and anisotropy (K/Kr).
Drawdown Recover
T -[ 0.125 x 245gal/min x 192.5ft3 /d j x 1 [ 0.125 x 245gal/min x 192.5ft3 /d] x 1
~ 4n x 0.1 6/f x Igal/min ~ 4itx0.16/fx \gal/min
T = 2, 900ft2 /d T = 2, 900f 2/d
r» _ ^* r. _ ______ £*
+t £r r
2 2c _ 4x2,900/f /Jx 1.5mm xl _ 4x2,900/r /d x 2mm x 1* ~ T ~ 2
(270/0 X 1, 440min/«/ (270/0 xl,440min/d5 = 0.0002 S = 0.0002
y ~ 2 y ~ ~T~r r
2 25 = 4x2, 900/f / d x 35>m'n x 1 _ _ 4x2. 900/r / d x 25mm x 1
y (270/0 xl,440min/</ ( 270/0 2 x 1, 440m in/dS = 0.004 S = 0.003y y
CONSTANT-FLUX TESTS 47
Assuming b is the thickness of transmissive intervals:
_ K - Krb $ _ 6ft /dx (524/Q 2 x 0.06 _ . ft/ , - - - ijt/a(270//)
K /K = 1/6 = 0.2z r
First Pumping Test in Borehole UE-25c #3
A pumping test was conducted in borehole UE-25c #3 from May to June 1984, primarily to deter mine the composite transmissivity of the tuffaceous rocks penetrated by borehole UE-25c #3 and the trans missivity of the tuffs and lavas of Calico Hills at the c-hole complex. During the test, water levels were monitored in the pumped well, in borehole UE-25c #2 (100 ft southeast of the pumped well) in borehole UE-25c #1 (224 ft northeast of the pumped well) and in
borehole UE-25p #1 (2,067 ft southeast of the pumped well). No barometric record during this pumping test was found in USGS files.
Procedures and Problems
The pumped well, borehole UE-25c #3, was open in the tuffs and lavas of Calico Hills and the Crater Flat Tuff, from the bottom of concrete, at a depth of 1,368 ft, to the bottom of the borehole, at a depth of 3,000 ft (Fenix and Scisson, Inc., written commun., 1984). A Centrilift submersible pump was emplaced in the borehole from 1,439 to 1,484 ft below land surface, with the pump intake at 1,454 ft below land surface (Fenix and Scisson, written commun., 1984). A 5.5-in.-outside-diameter riser pipe extended from the pump to the wellhead, where it was coupled to a 6-in.-diameter, steel discharge pipe with an in-line flowmeter and an end-line orifice plate and manometer (USGS logbook for borehole UE-25c #3, unpublished). Depth to water in the pumped well was monitored with a Bell and Howell pressure transducer with a recording range of 0 to 50 lb/in.2, that was suspended inside a
10 10TIME SINCE PUMPING STOPPED, IN MINUTES
100 1,000 10,000 100,000
LUo
0.1
0.01
x RECOVERY DATA
DRAWDOWN DATA
TYPE CURVE MATCHED TO DATA
MATCH POINTS
Early-time drawdown
Late-time drawdown
Early-time recovery
Late-time recovery
0.1 10 100
TIME SINCE PUMPING STARTED, IN MINUTES
1,000 10,000
Figure 17. Analytical solutions for drawdown and recovery data from borehole UE-25c #1 above the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #1, March 1984.
48 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
2.4-in.-diameter access tube and connected at the sur face to a Fluke data logger (USGS logbook for bore hole UE-25c #3, unpublished). The calibrated depth of the transducer was 1,420 ft below the top of the access tube, 100 ft below the static water level inside the tube (USGS records, unpublished).
Borehole UE-25c #2 was open in the tuffs and lavas of Calico Hills and the Crater Flat Tuff, from the bottom of concrete, at a depth of 1,365 ft, to the bottom of the borehole, at a depth of about 2,990 ft (USGS log book for borehole UE-25c #3, unpublished). Depth to water in the borehole was monitored with a Bell and Howell pressure transducer with a recording range of 0 to 25 lb/in.2, that was connected at the surface to a Fluke data logger. The calibrated depth of the trans ducer was 1,340 ft below the top of the casing, 20 ft below the static water level in the borehole (USGS records, unpublished).
Borehole UE-25c #1 was monitored above, between, and below straddle packers (Fenix and Scisson, Inc., written commun., 1984). Above the packers, between depths of 1,371 and 1,595 ft, the borehole was open in the nonwelded, upper part of the tuffs and lavas of Calico Hills. Between the packers, from 1,605 to 1,680 ft, the borehole was open in the bedded, lower part of the tuffs and lavas of Calico Hills. Below the packers, between depths of 1,690 and 2,962 ft, the borehole was open in the Crater Flat Tuff. Hydraulic heads above, between, and below the pack ers were monitored with GRC temperature- compensated pressure transducers with a recording range of 0 to 2,500 lb/in.2 (USGS records, unpub lished). The packers and instrumentation were sus pended on 2.9-in.-outside-diameter plastic tubing. The transducers were connected at the surface by water proofed cable to a Hewlett-Packard (HP-85) data log ger (USGS logbook for borehole UE-25c #3, unpublished). After installation of equipment and prior to testing, borehole UE-25c #1 was shut in to minimize barometric effects on water-level changes (USGS log book for borehole UE-25c #3, unpublished).
Borehole UE-25p #1, as in previous tests, was monitored to record hydraulic head in the Paleozoic rocks in the vicinity of the c-holes. Depth to water inside a piezometer tube was monitored with a pressure transducer with a recording range of 0 to 15 lb/in.2, that was connected at the surface to a Fluke data logger. The calibrated depth of the transducer was 1,190 ft below the top of the piezometer tube, 9 ft below the static water level inside the tube (USGS records, unpublished).
Without prior development, pumping began in borehole UE-25c #3 at 2257 on May 4,1984, and con tinued until 1002 on May 14, 1984, a period of about
9.5 days (USGS logbook for borehole UE-25c #3, unpublished). The test was interrupted by a pump fail ure on May 9,1984 (6,520 min into the test), that lasted 163 minutes. Prior to the pump failure, the discharge averaged 420 gal/min, but it took 25 hours for the dis charge to stabilize. After the pump was restarted, the discharge quickly stabilized at an average rate of 414 gal/min. For the entire pumping period, the aver age discharge rate was 418 gal/min, and a volume of 5,623,928 gallons of water was withdrawn (USGS log book for borehole UE-25c #3, unpublished).
In addition to the pump failure, the first pumping test in borehole UE-25c #3 was hampered by several other mechanical problems. Diurnal fluctuations of 1 to 4 mv in the system power supply, coupled with Earth tides, caused daily fluctuations of water levels in some of the boreholes. On the average, the water level in borehole UE-25c #2 was 0.35 ft higher at 0600 than at 1700 during and after the period in which the pump was operating; the water level in borehole UE-25c #3 fluctuated 1.5 ft between 0600 and 1700 after the pump was shut off. The transducer in borehole UE-25c #1 below the packers was inoperative during the entire pumping test. Finally, intermittent failure of data log ging equipment resulted in gaps of as much as seven days in recorded drawdown and recovery in each of the c-holes.
As in the pumping test in borehole UE-25c #2, turning the pump on and off during the pumping test in borehole UE-25c #3 caused rapid, large changes in the water level in the pumped well (fig. 18 A). Ten minutes after pumping began, the water level in borehole UE-25c #3 had decreased 61 ft; during the pumping failure, the water level in this borehole recovered to within three percent of the static level; when the pump was shut off on May 14, 1984, the water level in the pumped well rose 67 ft in ten minutes. Maximum drawdown in the pumped well during this test was about 72 ft (USGS records, unpublished).
The drawdown in boreholes UE-25c #2 and UE-25c #1 caused by pumping borehole UE-25c #3 was much slower and smaller than in the pumped well. The maximum drawdown in borehole UE-25c #2 was about 1.7 ft (fig. 18B), the maximum drawdown in borehole UE-25c #1 above the packers was about 18 ft (fig. 19A), and the maximum drawdown in borehole UE-25c #1 between the packers was about 11 ft (fig. 19B). The pumping did not cause a change in the water level in borehole UE-25 p#l that could be distin guished from water-level fluctuations related to Earth tides, atmospheric pressure changes, variations in the discharge rate, and mechanical problems (USGS records, unpublished). The pump failure caused an 86 percent water-level recovery in borehole
CONSTANT-FLUX TESTS 49
UE-25c #2, about one percent recovery in borehole UE-25c #1 between the packers, and no discernible recovery in borehole UE-25c #1 above the packers (figs. 18 and 19). On June 12,28.9 days after the pump was shut off, recovery in borehole UE-25c #2 was
100 percent complete, recovery in borehole UE-25c #1 between the packers was 20 percent complete, and no recovery had occurred in borehole UE-25c #1 above the packers.
-5
0 510 15 20 25 30 35 40 45 50 55
in 60UJ 65
Z 70
2 75
O -0.5 Q
0.5
1.0
1.5
2.0
RECOVERYDURINGPUMP
FAILURE
I I I I I I I I T \ I I 1 I I I I I V
RECOVERY DURING PUMP FAILURE
B
4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24
MAY
Figure 18. Drawdown as a function of time during the pump ing test in borehole UE-25c #3, May to June 1984: (A), Bore hole UE-25C #3; (B), Borehole UE-25c #2 (data from unpublished USGS records).
50 Results and Interpretation of Preliminary Aquifer Tests In Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
O -5 Q
IDC Q
I T T 1 \ i i i r \ I I T \ II T \ I I I
B -
10
15
.RECOVERY DURING PUMP FAILURE
I I I I I I4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 31 1 2 3 4 5 6 7 8 9 10 11 12 13
MAY JUNE
Figure 19. Drawdown as a function of time in borehole UE-25c #1 during the pumping test in borehole UE-25c #3, May to June 1984: (A), above the packers; (B), between the packers (data from unpublished USGS records).
Test Analyses
The first pumping test in borehole UE-25c #3 provided analyzable data sets from boreholes UE-25c #3, UE-25c #2, UE-25c #1 above the packers, and UE-25c #1 between the packers. Because of the variable discharge rate during the first 25 hours of the test, more weight was given in analyses to data obtained later in the pumping phase and during the recovery phase of the test. Based on atmospheric cor rections of less than 0.25 ft that were applied during the pumping test in borehole UE-25c #2, it is believed that failure to obtain a barometric record during the first pumping test in borehole UE-25c #3 potentially would have affected only analyses of data from monitored
intervals where drawdown or recovery did not exceed two feet. Thus, only analyses of data from borehole UE-25c #2 and recovery data from borehole UE-25c #1 between the packers might have been improved by cor recting for atmospheric pressure change.
Analyses of the data from the pumped well, bore hole UE-25c #3, by two methods indicated nearly iden tical values of transmissivity and hydraulic conductivity. Under the assumption of an infinite, homogeneous, isotropic, confined aquifer (Theis, 1935), a plot of residual drawdown as a function of the log of the ratio of time since the pump was restarted to time since pumping stopped (fig. 20) indicated the fol lowing:
CONSTANT-FLUX TESTS 51
T = = 2.3 x 4l4gal/min x 192.5ft /d = 2Qf 2 ' 4nx (60.0- 5.6/0 7
DATAPOINT
BEST-FIT STRAIGHT LINE SOLUTION
10 100 1,000 10,000 100,000
TIME SINCE PUMPING STARTED
TIME SINCE PUMPING STOPPED
Figure 20. Analytical solution for residual drawdown data from borehole UE-25c #3 assuming an infinite, homogeneous, isotropic, confined aquifer, pumping test in borehole UE-25c #3, May to June 1984.
Assuming b = the thickness of transmissive intervals (table 6):
= T/b = = 0.3ft/d
Flattening of a log-log plot of drawdown as a function of time since pumping started implies that a recharge boundary exists very close to borehole UE-25c #3. Hence, the solution of Cooper (1963) was applied to the drawdown data. Fit to the type curve for v = 0.1, the drawdown data from borehole UE-25c #3 after the pump was restarted (fig. 21) indicated the fol lowing values of transmissivity and horizontal hydrau lic conductivity:
= QxL(u,v) = 4l4gal/minx 192.5ft4ns 4nx2lftxlgal/min
If b is assumed to equal the total thickness of transmis sive intervals in the borehole,
The drawdown and recovery data obtained from borehole UE-25c #2 could be interpreted to conform to the analytical solution of either Streltsova-Adams (1978) for a fissure-block aquifer or Neuman (1975) for an unconfined, anisotropic aquifer. For both analy ses, the distance between boreholes UE-25c #2 and UE-25c #3 (r) was considered to be the average dis tance between the open sections of the boreholes. Tak ing into account the drift of both boreholes, the average interborehole distance was determined from gyro scopic surveys to be 95 ft.
For the analytical solution of Streltsova-Adams (1978), the parameter r/B was estimated as follows:
1. Half the average distance between fractures in transmissive intervals (from Supplementary Data section) = 1.7ft
2.
3.
Log-mean matrix hydraulic conductivity (from pi. 2) = 0.0004 ft/d
Transmissivity (from the slope of late-time data on a plot of recovery as a function of time during this pumping test) = 25,000 ft2/d
fTxH95ft
25,000ft /dx 1.1 ft 0.0004ft/d
= 0.009
Fit to the type curve for i\ = 10 and r/B = 0.05, the drawdown data from borehole UE-25c #2 after the pump was restarted (fig. 22) indicated the following values of transmissivity (7), fracture storativity (Sj), block storativity (Sfc), fracture hydraulic conductivity (Kf), and block hydraulic conductivity (Kb):
T =4ns
= 4l4gal/minxl92.5ft/dxl = 4nx 0.22ft x 1 gal/ min
_ 4Tt _ 4x29,000ft /dxQ.49min _ nrvuA, - - - - U.UW
re (95/0 xlxl,440min/d
5^ = S,x (Tl-1) = 0.004x (10-1) = 0.04
4 = 0.05
K =r 899/f
= Q.3ft/dJ
52 Results and Interpretation of Preliminary Aquifer Tests In Boreholes UE-25c #1, UE-25c *2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
10
1 -
0.1
MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
0.1 1 10 100 1,000
TIME SINCE PUMPING STARTED/RADIUS SQUARED, IN MINUTES PER SQUARE FOOT
10,000
Figure 21. Analytical solution for drawdown data from borehole UE-25c #3 assuming an infinite, homogeneous, isotropic, confined aquifer with leakage from a confining unit without storage, pumping test in borehole UE-25c #3, May to June 1984.
10
0.1
0.010.1
DATA POINT
TYPE CURVE MATCHED TO DATA
10 100
TIME SINCE PUMPING STARTED, IN MINUTES
1,000 10,000
Figure 22. Analytical solution for drawdown data from borehole UE-25c #2 assuming a fissure-block aquifer, pumping test in borehole UE-25C #3, May to June 1984.
CONSTANT-FLUX TESTS 53
=
(1,900/0
For the analytical solution of Neuman (1975), it was assumed that the vertical hydraulic-conductivity profile determined by injection tests in borehole
UE-25c #1 applied, also, in UE-25c #2. Consequently, values of vertical hydraulic conductivity (ATZ), horizon tal hydraulic conductivity (ATr), and the parameter 6 in the first pumping test in UE-25c #3 were estimated for borehole UE-25c #2 as follows:
K.
K = 1,625z (70/2 + 55/0.6 + 135/0.4 + 80/0.2 + 250/0.08 + 345/0.05 + 145/0.03 + 175/0.01 + 105/0.008 + 190/0.005 + 75/0.003)
K = 0.0l5ft/d
K =
V K.b.£j i ii= 1
_ (70 x 2 + 55x 0.6 + 135 x 0.4 + 80 x 0.2 + 250 x 0.08 + 345 x 0.05 + 145 x 0.03 + 175 x 0.01 + 105 x 0.008 + 190 x 0.005 + 75 x 0.00! r T625
= 0.18/f/d
54 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
Assuming b = the thickness of transmissive intervals in borehole UE-25c #2:
B =Kb2 0.18/f/</x (544/r) 2
(95/Q = 0<003
Fit to the type curve for 6 = 0.004, the drawdown data from borehole UE-25c #2 after the pump was restarted (fig. 23) indicated the following values of transmissiv- ity (7), storativity (5), specific yield (Sy), horizontal hydraulic conductivity, vertical hydraulic conductiv ity, and anisotropy (K/Kr):
T =4ns
'n * 192.5ft /dx 1 _4n x 0.27ft x Igal/min
_ 4 x 23, 000/r/</ x 0.6mm x 1 _ - - - -
r (95/r) x 1, 440min/</
T =
_ o -
_ 4 x 23,000/r /d x 9.7mm x 1 _ OQ7
/ ( 95/r) 2 x 1, 440min/d
Assuming b = thickness of transmissive intervals:
T2 IUU14*
= T/b =
(544/Q x 0.004
= 5/r/rf
/K = z r 4Qft/d
= 0.1
Both the drawdown data from borehole UE-25c #1 above the packers and the recovery data from borehole UE-25c #1 between the packers unam biguously conform to type curves of Neuman (1975) for an unconfined, anisotropic aquifer (figs. 24 and 25). From a heat-pulse flowmeter survey done in December 1991, it was estimated that tuffaceous rocks above the packers contribute four percent of the discharge from the entire thickness of rocks below casing and concrete in borehole UE-25c #1, and tuffaceous rocks between the packers contribute 0.5 percent of this discharge. Therefore, for the interval above the packers the fol-
lowing values of transmissivity (7) and specific yield (Sy) were calculated:
T =4ns
[o.Q4 x 4lSgal/min x 192.5ft3 /d] x 1 2
_V ~"
(4n x 4.5/0 x Igal/min
_ 4 x 60ft /d x 480mm x 1 _ nnni - ^ ~ UlUU1 r (256/r) x\440min/d
For the interval between the packers, the following values of transmissivity and specific yield were calcu lated:
Q x
4ns
{ 0.005 x 418*a//mm x 192.5/f3/</ )xl 71________________________ / _ AQft /
(4nx 0.74/0 x Igal/min J
_ 4 x 40/r /d x 1,100mm x 1y - = U.UU2
r (259/f) x 1,440min/</
From the drawdown data and thickness of transmis sive intervals above the packers,
B = K
K /KZ
x K /K = 4.0 z r
2 2 4.0 x (182/Q
(256/0
Fracture data from between the packers were insufficient to calculate unequivocally the thickness of transmissive intervals between the packers. Therefore, average values of horizontal hydraulic conductivity (Kr) and vertical hydraulic conductivity (Kz) were cal culated for the Calico Hills aquifer (the intervals above and between the packers in borehole UE-25c #1) by assuming that the value of anisotropy (K/Kr) obtained above the packers applies, also, to the interval between the packers.
Adding the transmissivity values for the intervals above and between the packers gives a composite transmissivity of 100 ft2/d for the Calico Hills aquifer. Dividing this transmissivity value by the known thick ness of transmissive intervals above and between the packers, 198 ft, gives a horizontal hydraulic conductiv ity value of 0.5 ft/d for the Calico Hills aquifer. If K/Kr - 2, then the vertical hydraulic conductivity of the Calico Hills aquifer = 2 Kr = 2 x 0.5 ft/d = 1 ft/d.
CONSTANT-FLUX TESTS 55
10
oQ
0.1
0.010.1
EARLY-TIME DATA MATCH POINT
LATE-TIME DATA MATCH POINT
_L_L
DATA POINT
TYPE CURVE MATCHED TO DATA
10 100
TIME SINCE PUMPING STARTED, IN MINUTES
1,000 10,000
Figure 23. Analytical solution for drawdown data from borehole UE-25c #2 assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, May to June 1984.
56 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
100
10
0.01
MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
10 100 1,000 10,000
TIME SINCE PUMPING STARTED, IN MINUTES
100,000
Figure 24. Analytical solution for drawdown data from borehole UE-25c #1 above the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, May to June 1984.
10
0.1
0.01
MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
100 1,000 10,000 100,000
TIME SINCE PUMPING STOPPED, IN MINUTES
Figure 25. Analytical solution for recovery data from borehole UE-25c #1 between the packers assuming an infinite, homogeneous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, May to June 1984.
CONSTANT-FLUX TESTS 57
Injection Test in Borehole UE-25c #2
An injection test was conducted in borehole UE-25c #2 from 1351 to 1520 on October 30,1984, to ascertain hydrologic properties of an interval in bore hole UE-25c #2 that was thought to contain very per meable rock (the Bullfrog aquifer). The injection test was conducted using monitoring equipment installed for a pumping test in borehole UE-25c #3 that began 156 minutes after the injection test ended.
In the injection well, borehole UE-25c #2, strad dle packers were installed on a 2.9-in-diameter plastic tube to isolate the Bullfrog aquifer (Fenix and Scisson, Inc., written commun., 1984). The interval between the packers extended from 2,364 to 2,475 ft below the land surface. Above the packers, from 1,365 to 2,355 ft below the land surface, the borehole was open in the Calico Hills aquifer, the Prow Pass-upper Bull frog aquifer, and confining units between and below the two aquifers. Below the packers, from 2,484 to 2,990 ft below land surface, the borehole was open in the Tram aquifer and the overlying confining unit. Hydraulic heads above, between, and below the pack ers were monitored with GRC temperature-compen sated, pressure transducers with recording ranges of 0 to 2,500 and 0 to 5,000 lb/in.2, that were connected at the surface to a HP-85 data logger (USGS logbook for thec-holes, 1984-1985, unpublished). During the test, water was injected between the packers from a Baker tank to maintain a constant pressure head of 778 ft (USGS records, unpublished). Because the injection rate quickly stabilized at 167 gal/min (USGS logbook for the c-holes, 1984-1985, unpublished), what was intended to be a constant-head test was converted to a constant-flux test, and the effects of this flux were mon itored in borehole UE-25c #1, UE-25c #2, and UE-25c #3 (Devin L. Galloway, USGS, oral commun., 1993).
Borehole UE-25c #1 was monitored above, between, and below straddle packers hung on a 2.9-in.-diameter plastic tube (Fenix and Scisson, Inc., written commun., 1984). Above the packers, from 1,371 to 2,514 ft below land surface, the borehole was open from the Calico Hills aquifer to the top of the Bullfrog aquifer. Between the packers, from 2,524 to 2,594 ft below land surface, the borehole was open in the Bullfrog aquifer. Below the packers, from 2,603 to 2,962 ft below land surface, the borehole was open in the Tram aquifer and overlying confining unit. Hydraulic heads in borehole UE-25c #1 were moni tored with GRC temperature-compensated, pressure transducers with recording ranges of 0 to 2,500 and 0 to 5,000 lb/in.2, that were connected at the surface to a HP-85 data logger (USGS logbook for the c-holes,
1984-1985, unpublished). Before the test began, bore hole UE-25c #1 was shut in to minimize barometric effects.
Borehole UE-25c #3 was open in the tuffs and lavas of Calico Hills and the Crater Flat Tuff, from the bottom of concrete, at a depth of 1,368 ft, to the bottom of the borehole, at a depth of 2,976 ft. The pump instal lation was the same as it was in the May-June 1984 pumping test in borehole UE-25c #3. Depth to water in the borehole was monitored with a Bell and Howell pressure transducer with a recording range of 0 to 50 lb/in.2, that was suspended inside a 2.4-in.- diameter access tube and connected at the surface to a Fluke data logger (USGS logbook for the c-holes, 1984-1985, unpublished). The calibrated depth of the transducer was 1,320 ft below the top of the access tube, 100 ft below the static water level inside the tube (USGS records, unpublished).
Injection of water between the packers in bore hole UE-25c #2 caused the water level to rise about 4.0 ft in borehole UE-25c #2 above the packers (fig. 26), 0.7 ft in borehole UE-25c #1 between the packers, 0.1 ft in borehole UE-25c #1 above and below the packers, and 0.4 ft in borehole UE-25c #3 (fig. 27). After injection ended, water-level recovery to pre-test static levels was complete in all monitored intervals in boreholes UE-25c #1 and UE-25c #3 within 90 min utes. However, in borehole UE-25c #2, water level recovery above the packers was only 69 percent com plete when a pumping test began in borehole UE-25c #3,156 minutes after injection ended. As indi cated in figure 26, residual drawdown from the injec tion test is estimated to have had an effect on the water level in borehole UE-25c #2 above the packers for the first 515 minutes of the pumping test. Possibly because injection changed fracture apertures in the injection interval, the hydraulic head between the packers was 1.6 ft lower than the pre-injection test static level and still falling when the pumping test in borehole UE-25c #3 started (fig. 27). Post-pumping test data indicate that the hydraulic head between the packers probably would have stabilized asymptotically with time at a level about 2.5 ft lower than before the injec tion test started, had the pumping test in borehole UE-25c #3 not been conducted.
Most of the data from the injection test were not analyzed. The head build-up in borehole UE-25c #2 above the packers (fig. 26) was erratic and indicative of possible mechanical problems. The head build-up in borehole UE-25c #1 above and below the packers (fig. 27) was insignificant. Although the head build-up in borehole UE-25c #1 between the packers (fig. 27) was large and steady enough to be analyzed, the data were considered less reliable than recovery data
58 Results and Interpretation of Preliminary Aquifer Tests In Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
ABOVE PACKERS, DASHED WHERE EXTRAPOLATED
BETWEEN PACKERS, DASHED WHERE EXTRAPOLATED
10 100
TIME SINCE INJECTION STARTED, IN MINUTES
1,000 10,000
Figure 26. Water-level changes in borehole UE-25c #2 during and after injection of water between packers on October 30,1984.
CONSTANT-FLUX TESTS 59
1.0
I 0.5 - O
UJ
LL)
INJECTION ENDED
UE-25c #1 ABOVE PACKERS UE-25c#1 BETWEEN PACKERS UE-25c#1 BELOW PACKERS UE-25c#3
0.1 10
TIME SINCE INJECTION STARTED, IN MINUTES
100 1,000
Figure 27. Water-level changes in boreholes UE-25c #1 and UE-25c #3 in response to injection of water into borehole UE-25C #2, October 30,1984.
60 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c f 1, UE-25c #2, and UE-25c *3, Yucca Mountain, Nye County, Nevada
obtained from the same interval during the subsequent pumping test in borehole UE-25c #3. Consequently, the data from UE-25c #1 between the packers were not analyzed. Only the data from borehole UE-25c #3 were analyzed because no comparable data were obtained from this borehole in any other constant-flux tests (This was the only test in which borehole UE-25c #3 was used as an observation well).
The composite transmissivity (J), storativity (5), and hydraulic conductivity (Kr) of the tuffaceous rocks in borehole UE-25c #3 could be determined from the head build-up data shown in figure 27 assuming an infi nite, homogeneous, isotropic, confined aquifer. Using the method of Cooper and Jacob (1946) and equations 12 and 13, the following calculations were made:
T = 23Q = 2.3 x 167gal/min x 192.5ft3 /d = 35 QQO^/J A ~*s, 47TX (0.40-0.23)/f x Igal/min ' *
2.25 Tto 2.25 x 35, 000ft2/d x 0.42mm nrvv, U.UUZ
r (95/0 xl,440min/</
Assuming b to be the thickness of transmissive inter vals:
Values of transmissivity and hydraulic conduc tivity determined for the rocks in borehole UE-25c #3 from the injection test are two orders of magnitude larger than values determined from the drawdown in borehole UE-25c #3 during the pumping test in this borehole in May-June 1984. Yet, the transmissivity determined from the pumping test in borehole UE-25c #3 is the same, to one significant figure, as the composite transmissivity determined in borehole UE-25c #1 from fluid-injection tests (261 ft2/d). Larger values of transmissivity and hydraulic conductivity apparently are determined as the radius of investigation expands and encompasses more conduits for ground- water flow, such as faults and fracture zones. Cross- hole tests indicate site-scale hydrologic properties, whereas single-well tests indicate hydrologic proper ties within a small radius of the pumping or injection well. Consequently, the remainder of this report emphasizes analyses of data obtained from observation wells.
Second Pumping Test in Borehole UE-25c #3
A second pumping test was conducted in bore hole UE-25c #3 from October-December 1984, prima rily to determine vertical and lateral variations in hydrologic properties of the Crater Flat Tuff. In addi tion to the monitoring network for the injection test described in the previous section, a piezometer was monitored in borehole UE-25p #1, and a recording barometer was maintained at borehole USW H-4. Because the piezometer record from borehole UE-25p #1 indicated an erratic but progressive increase in hydraulic head throughout the entire two weeks that borehole UE-25c #3 was pumped, it is believed that the transducer installed in borehole UE-25p #1 was miscal- ibrated or malfunctioned during this pumping test. The barometric record obtained at borehole USW H-4 (fig. 28) was not used to correct drawdown data, because head changes in the c-holes were considered large enough that atmospheric pressure changes proba bly would have had little or no effect on data analyses.
Procedures and Problems
Pumping in borehole UE-25c #3 began at 1756 on October 30,1984, and continued until 1342 on November 15,1984, a period of about 15.8 days (USGS records, unpublished). The test was interrupted by an 8.3 minute pump failure on November 2,1984 (3,839 minutes into the test), which caused a 97 percent recovery of the water level in the pumped well but only slight (4-8 percent) recovery in monitored intervals of boreholes UE-25c #1 and UE-25c #2 (USGS records, unpublished). During the first few hours of the test, the discharge rate varied from 400 to 410 gal/min, but for most of the test, the discharge rate varied from 422 to 429 gal/min (USGS logbook for the c-holes, 1984- 1985, unpublished). At an average discharge rate of 425 gal/min, a volume of 9,675,942 gallons of water was withdrawn during the test (USGS logbook for the c-holes, 1984-1985, unpublished).
In addition to the pump failure, the second pump ing test in borehole UE-25c #3 was hampered by sev eral other mechanical problems and the short interval between the injection test in borehole UE-25c #2 described previously and the pumping test. The trans ducer in borehole UE-25c #2 below the packers was inoperative for the entire pumping test, and the trans ducer in borehole UE-25c #1 between the packers intermittently gave spurious readings (USGS logbook for the c-holes, 1984-1985, unpublished; USGS records unpublished). During the first few days of the test, the discharge meter was slightly inaccurate
CONSTANT-FLUX TESTS 61
28.6
27.830 31 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 1 2 3 4 5 6 7 8 9 10
OCT NOV DEC
Figure 28. Atmospheric pressure at borehole USW H-4 during the pumping test in borehole UE-25c #3, October to December 1984.
because of leakage through a fitting in the discharge line (USGS logbook for the c-holes, 1984-1985, unpublished). Oscillations in the power supply cou pled with Earth tides caused diurnal fluctuations in recorded drawdown (USGS records, unpublished). Problems with data loggers caused intermittent losses of drawdown and recovery data (USGS logbook for the c-holes, 1984-1985, unpublished). In borehole UE-25c #2 above the packers, a 13-ft head decrease followed by a 7-ft head increase occurred as borehole UE-25c #3 was being pumped. Regardless of whether the head increase during pumping resulted from ante cedent effects of the preceding injection test, changing hydrologic conditions during pumping (e.g. boundary effects), or a transducer malfunction, the entire record from borehole UE-25c #2 above the packers is suspect. Consequently, this record could not be analyzed to determine hydrologic properties. Finally, antecedent drawdown from the injection test required a correction to the recorded drawdown data from borehole UE-25c #2 between the packers for these data to be used to calculate hydrologic properties. The anteced ent drawdown trend was estimated by extrapolation between drawdown values recorded prior to pumping and apparent steady-state drawdown values obtained 23.7 days after pumping ceased.
As in the first pumping test in borehole UE-25c #3 (fig. ISA), turning the pump on and off dur
ing the second pumping test in this borehole caused rapid, large changes in the water level in the pumped well (fig. 29). Ten minutes after pumping began, the water level in borehole UE-25c #3 had decreased 61 ft; when the pump was turned off, the water level rose about 65 ft in ten minutes. Maximum drawdown in the pumped well during this test was about 65 ft (USGS records, unpublished).
-RECOVERY DURING PUMP FAILURE
-5
0
5
10
15
20
25
30
35
40
45
50
55
60
65
30 31 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24
OCT NOV
Figure 29. Drawdown as a function of time in borehole UE-25c #3 during the pumping test in borehole UE-25C #3, October to December 1984.
62 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c *2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
The drawdown in monitored intervals of bore hole UE-25c #1 caused by pumping borehole UE-25c #3 was much slower and smaller than in the pumped well (USGS records, unpublished). The max imum drawdown in borehole UE-25c #1 above the packers was about 1.1 ft; the maximum drawdown between the packers was about 2.2 ft; and the maxi mum drawdown below the packers was about 3.15 ft (fig. 30). Water-level recovery in the pumped well was
complete 444 minutes after pumping ceased (fig. 29), but complete recovery in monitored intervals of bore hole UE-25c #1 required 20.7 to 21.7 days (fig. 30).
Similar to borehole UE-25c #1 between the packers, the maximum drawdown in borehole UE-25c #2 between the packers after correcting for residual drawdown from the injection test was about 2.3 ft (USGS records, unpublished). Complete recov ery in borehole UE-25c #2 between the packers occurred 23.7 days after pumping ceased (fig. 31).
-0.5
0
0.5
1.0
' '2.0
2.5
3.0
3.5
UE-25c #1, ABOVE PACKERS
UE-25c#1, BETWEEN PACKERS
UE-25c #1, BELOW PACKERS
29 30 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 1 2 3 4 5 6 7 8 9 10
OCT NOV DEC
Figure 30. Drawdown as a function of time in borehole UE-25c #1 during the pumping test in borehole UE-25c #3, October to December 1984.
-0.5
RECOVERY DURING PUMP FAILURE
I I I I I30 31 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 25 26 27 28 29 30 1 2 3 4 5 6 7 8 9 10 11
OCT NOV DEC
Figure 31. Drawdown as a function of time in borehole UE-25c #2 between the packers during the pumping test in borehole UE-25c #3, October to December 1984, with residual drawdown from a preceding injection test subtracted.
CONSTANT-FLUX TESTS 63
Test Analyses
The second pumping test in borehole UE-25c #3 produced analyzable data sets from boreholes UE-25c #3, UE-25c #2 between the packers, and UE-25c #1 above, between, and below the packers. Analyses of the data from the pumped well, borehole UE-25c #3, produced nearly identical results as analy ses of data from this borehole obtained during the first pumping test in the borehole. To avoid redundancy, analyses of data from the pumped well obtained during the second pumping test in the borehole are not dis cussed further in this report. The remaining data sets are discussed with respect to the hydrogeologic inter vals tested, instead of by borehole.
For drawdown and recovery data from borehole UE-25c #1 above the packers, the pumping test in bore hole UE-25c #2 indicated that using the analytical solu tion of Neuman (1975) for an unconfmed aquifer and matching the data curve to the type curve for 6 = 0.06 provided the most reasonable calculations of hydro- logic properties. Therefore, in the second pumping test in borehole UE-25c #3, drawdown data from borehole UE-25c #1 above the packers again were matched to the type curve of Neuman (1975) for 6 = 0.06 (fig. 32), and the following values of transmissivity (7), storativ- ity (5), specific yield (Sy), horizontal hydraulic conduc tivity (Kr), vertical hydraulic conductivity (Kz), and anisotropy (K/K,) were calculated:
T =Q x , \L,
4ns
0.125 x 425gal/min x 192.5ft*/d) x 1
(47tx0.21/0 x Igal/min/d
_ 4x3,900/r/dx6.1mmxl - - *T
r (267/0 xl,440min/d
4x3,900/y/dx80mfn x 2
(267/0 xl,440mm/d
K =Z
P 7/f/dx[528/f2Jx0.06
267 !
= 2ft/'d
K /K = 2/7 = 0.3z r
64 Results and Interpretation of Preliminary Aquifer Tests In Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
10
0.1
0.01
EARLY-TIME DATA MATCH POINT
LATE-TIME DATA MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
10 100 1,000
TIME SINCE PUMPING STARTED, IN MINUTES
10,000 100,000
Figure 32. Analytical solution for drawdown data from borehole UE-25c #1 above the packers assuming an infinite, homoge neous, anisotropic, unconfined aquifer, pumping test in borehole UE-25c #3, October to December 1984.
The average transmissivity of the Prow Pass- upper Bullfrog aquifer was estimated to equal the aver age transmissivity of the rocks in borehole UE-25c #1 above the packers minus the transmissivity of the Calico Hills aquifer, which was calculated as follows:
Transmissivity
UE-25c #1 above packers, pumping test in borehole UE-25c #2UE-25c #1 above packers, second pumpingtest in borehole UE-25c #3UE-25c #1 above packers, averageCalico Hills aquiferProw Pass - upper Bullfrog aquifer
2,900
3,900
3,400 -100
3,300
The average horizontal hydraulic conductivity of the Prow Pass-upper Bullfrog aquifer, then, would be 3,300 ft2/d divided by 326 ft of transmissive rocks, which equals 10 ft/d. Multiplying the average hori zontal hydraulic conductivity of the Prow Pass-upper Bullfrog aquifer by the average anisotropy in borehole
UE-25c #1 above the packers, 0.2, indicates an aver age vertical hydraulic conductivity of 2 ft/d for the Prow Pass-upper Bullfrog aquifer.
As in the above calculations, the average specific yield of the Prow Pass-upper Bullfrog aquifer was esti mated to equal the average specific yield of the rocks in borehole UE-25c #1 above the packers minus the spe cific yield of the Calico Hills aquifer, which was calcu lated as follows:
UE-25c #1 above packers, pumping test in borehole UE-25c #2UE-25c #1 above packers, second pumpingtest in borehole UE-25c #3UE-25c #1 above packers, averageCalico Hills aquiferProw Pass-upper Bullfrog aquifer
Specific yield
0.004
.01
O007 -.003
Recovery data obtained from boreholes UE-25c #1 and UE-25c #2 between the packers, both,
CONSTANT-FLUX TESTS 65
conform to the type curve of Theis (1935) for an infi nite, homogeneous, isotropic, confined aquifer (figs. 33 and 34) and indicate hydrologic properties for the Bullfrog aquifer. Based on heat-pulse flowmeter sur veys done in December 1991, it was assumed that 29.5 percent of the flow in rocks below casing and con
crete in borehole UE-25c #1 and 14 percent of the flow in rocks below casing and concrete in borehole UE-25c #2 come from the packed-off intervals in these boreholes. The following calculations of transmissiv- ity (7), storativity (5), and horizontal hydraulic conduc tivity (Kr) were made:
UE-25c #1 Between Packers UE-25c #2 Between Packers
4ns 4ns
[o.295 x 425gal/min x 192.5/f3/rfJ x 1
(4rex0.23/0 x Igal/min
[o.!4 x 425gal/min x 192.5ft3 /d) x
(4nx 0.22/0 x Igal/min
T = 8, 400ft /d T = 4,100/r /d
s = 4x8. 400ft /d x 7.0mm x 0.1
(280/0 2 xl,
5 _ 4x4,100/f /d x 5.6mm x 0.1
(92/f)
5 = 0.0002 S = 0.0008
70ft 74/f
66 Results and Interpretation of Preliminary Aquifer Tests In Boreholes UE-25c f 1, UE-25c f2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
10
0.1 -
0.01
MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
10 100 1,000
TIME SINCE PUMPING STOPPED, IN MINUTES
10,000 100,000
Figure 33. Analytical solution for recovery data from borehole UE-25c #1 between the packers assuming an infinite, homoge neous, isotropic, confined aquifer, pumping test in borehole UE-25C #3, October to December 1984.
Because of uncertainty regarding the estimate of flow contributed by rocks between the packers, calculated values of hydrologic properties presumably bracket the actual values.
Drawdown data obtained from borehole UE-25c #1 below the packers reveal the influence of fault boundaries on the Tram aquifer. Drawdown below the packers became essentially constant after about 5,000 minutes of pumping, indicating a constant flux to the Tram aquifer from that point until pumping ceased. The two faults that are shown in figure 7 cut ting the Tram aquifer at the c-hole complex probably are the source of the water recharged to the aquifer dur ing pumping. As discussed previously, a constant flux from a fault is analogous to constant leakage from a confining unit without storage. Hence, the drawdown data from borehole UE-25c #1 below the packers were matched to the type curve of Cooper (1963) for v = 0.02 (fig. 35), and values of transmissivity (7), storativity (5), and horizontal hydraulic conductivity (ATr) were then calculated. Based on a heat-pulse flowmeter sur vey done in December 1991, it was estimated that
58 percent of the flow from rocks below casing and concrete in borehole UE-25c #1 comes from the inter val that was below the packers during this pumping test. The following calculations were made:
r=4715
0.58 x 425gal/min x 192.5ft /dj x 1
(4nx0.48/0 x \gal/min~ '
_ 4Tt/r2 _ 4x7, 900ft2/d x0.00012min/ft2 _ nnn, ~ ~ lxl,440mm/</ ~
As a check on the assumptions made regarding the percentage of flow contributed from rocks in bore hole UE-25c #1 above, between, and below the pack ers, values of transmissivity, storativity, and hydraulic conductivity obtained for each interval from the second pumping test in borehole UE-25c #3 were added or averaged, as appropriate, and compared to composite values of hydrologic properties obtained from bore holes UE-25c #2 and UE-25c #3 during the first pump-
CONSTANT-FLUX TESTS 67
10
0.1
0.01
MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
10 100 1,000
TIME SINCE PUMPING STOPPED, IN MINUTES
10,000 100,000
Figure 34. Analytical solution for recovery data from borehole UE-25c #2 between the packers assuming an infinite, homoge neous, isotropic, confined aquifer, pumping test in borehole UE-25c #3, October to December 1984.
10
0.1
MATCH POINT
DATA POINT
TYPE CURVE MATCHED TO DATA
0.010.00001
_l I I I I I
0.0001 0.001 0.01 0.1
TIME SINCE PUMPING STARTED/DISTANCE FROM THE PUMPED WELL, SQUARED, IN MINUTES PER SQUARE FOOT
Figure 35. Analytical solution for drawdown data from borehole UE-25c #1 below the packers assuming an infinite, homoge neous, isotropic, confined aquifer with leakage from a confining unit without storage, pumping test in borehole UE-25c #3, October to December 1984.
68 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c *3, Yucca Mountain, Nye County, Nevada
ing test in borehole UE-25c #3 and the injection test in borehole UE-25c #2. As indicated in table 9, compos ite values of transmissivity = 20,000 ft2/d, storativity = 0.004, horizontal hydraulic conductivity = 30 ft/d, and vertical hydraulic conductivity = 2 ft/d calculated for borehole UE-25c #1 compare favorably with compos ite values of transmissivity, storativity, and hydraulic conductivity obtained for rocks in boreholes UE-25c #2 and UE-25c #3. Therefore, calculations of hydrologic properties of the four aquifers penetrated by borehole UE-25c #1 can be considered reasonable esti mates.
SUMMARY AND CONCLUSIONS
Fluid-injection and pumping tests conducted in 1983 and 1984 in boreholes UE-25c #1, UE-25c #2, and UE-25c #3 (the c-holes) on the east side of Yucca Mountain, Nev., were analyzed and interpreted in the context of other hydrogeologic information obtained from lithologic logs, borehole geophysical logs, core permeameter tests, and borehole flow surveys.
The c-holes, each of which is about 3,000 ft deep, are 100 to 251 ft apart at the surface. The three boreholes are completed in a 5,000-ft-thick sequence of Miocene tuff aceous rocks that is underlain by Paleozoic carbonate rocks and transected by high- angle, north-northeasterly and northwesterly striking faults. The contact between the Miocene and Paleozoic rocks generally is believed to be a detachment fault, into which the north-northeasterly striking faults merge listrically. A pumping test conducted in borehole UE-25c #2 indicated hydraulic connection between the Miocene and Paleozoic rocks, possibly through the net work of faults cutting these rocks.
The depth to water at the c-hole complex ranges from 1,312 to 1,320 ft below land surface. The c-holes are open in the saturated zone below an average depth of about 1,370 ft from the land surface. Each of the c-holes is open in the tuffs and lavas of Calico Hills and the Prow Pass, Bullfrog, and Tram Members of the Crater Flat Tuff. These geologic units consist mostly of nonwelded to densely welded ash-flow tuff with interlayered ash-fall tuff and volcaniclastic rocks. A tuff breccia occurs in the Tram Member where the unit is transected by the Paintbrush Canyon Fault and another high-angle, north-northeasterly striking fault.
Tectonic and cooling fractures pervade the tuf- faceous rocks penetrated by the c-holes, although frac tures are distributed unevenly, and intervals range from unfractured to very fractured. Because of the fault brecciation, fracture frequency is greatest in the Tram Member. The bedded zone of the tuffs and lavas of Calico Hills, also, is very fractured. On the average,
moderately to densely welded zones of the Prow Pass and Bullfrog Members are more fractured than bedded zones which, in turn, are more fractured than non- welded to partially welded zones. Most fractures strike approximately south and dip westward at angles of 50°-87°. The least common fractures strike generally east or west, and many of these are shallow-dipping or mineralized.
Within the saturated zone open to the c-holes, the tuffaceous rocks display layered heterogeneity. Per meameter tests indicate a vertical range in matrix per meability of 0.001 to 20 mD, with slightly larger permeability horizontally than vertically. Falling-head and pressure-injection tests in borehole UE-25c #1 indicate a vertical range in hydraulic conductivity of 0.003 to 2 ft/d. The average hydraulic conductivity in the horizontal direction in borehole UE-25c #1 is 0.2 ft/d, whereas the average hydraulic conductivity in the vertical direction is 0.02 ft/d.
Fluid-injection tests and single-well pumping tests in boreholes UE-25c #1 and UE-25c #3 indicate a composite transmissivity of about 300 ft2/d for the tuffs and lavas of Calico Hills and the Crater Flat Tuff. However, multiple-well, constant-flux tests in the c-holes indicate that single-well injection and with drawal tests are not reliable indicators of site-scale hydrologic properties. For the entire thickness of rocks below casing and concrete in a borehole, cross-hole tests generally indicate values of transmissivity and hydraulic conductivity that are about two orders of magnitude larger than values obtained in single-well tests. This dependence of results on the radius of inves tigation can be interpreted as an effect of encompassing more conduits for ground-water flow, such as faults or fracture zones, as a larger volume of aquifer is investi gated.
In the c-holes, eleven transmissive intervals were identified on the basis of fracture and matrix perme ability distributions, borehole resistivity, temperature, and caliper logs, and heat-pulse flowmeter and trace- jector surveys. The heat-pulse flowmeter surveys indi cated downward flow in the upper parts and upward flow in the lower parts of boreholes UE-25c #1 and UE-25c #2, but upward flow through the entire sur veyed section of borehole UE-25c #3 (below a depth of about 1,500 ft). The eleven transmissive intervals at the c-hole complex were grouped for purposes of investigation and discussion into four informal aquifers with intercalated confining units. In descending order, the four aquifers are the Calico Hills, Prow Pass-upper Bullfrog, Bullfrog, and Tram.
The Calico Hills aquifer is unconfined and aniso- tropic. The aquifer has a transmissivity of 100 ft2/d, a specific yield of 0.003, a horizontal hydraulic conduc-
SUMMARY AND CONCLUSIONS 69
3 31
| iZ
3D
«<
9
9
W s a o 3 | 1
| i
Tabl
e 9.
Sum
mar
y of
ana
lyse
s of
198
4 co
nsta
nt-f
lux
aqui
fer t
ests
in b
oreh
oles
UE
-25c
#1,
UE
-25c
#2,
and
UE
-25C
#3
[Val
ues
of tr
ansm
issi
vity
roun
ded
to tw
o si
gnifi
cant
figu
res;
oth
er h
ydro
logi
c pr
oper
ties
roun
ded
to o
ne s
igni
fican
t fig
ure]
Mon
itore
d in
terv
al o
r bo
reho
leTr
ansm
issi
vity
(feet
squ
ared
per d
ay)
Stor
ativ
ltyFr
actu
re
Blo
ck
Spec
ific
stor
ativ
lty
Stor
ativ
lty
yiel
d
Hyd
raul
ic c
ondu
ctiv
ity (f
eet p
er d
ay)
Hor
izon
tal
Vert
ical
Fr
actu
re
Blo
ck
UE
-25c
*lC
alic
o H
ills
aqui
fer
Prow
Pas
s-U
pper
Bul
lfrog
aqu
ifer
Bul
lfro
g aq
uife
rT
ram
aqu
ifer
Com
posi
te
UE
-25c
#2C
ompo
site
(Neu
man
, 19
75)
Com
posi
te (S
trelts
ova-
Ada
ms,
197
8)
UE
-25c
#3C
ompo
site
(C
oope
r-Ja
cob,
194
6)
100
3,30
08,
400
7,90
020
,000
23,0
0029
,000
35,0
00
0.00
05
.000
2.0
03
0.00
3
0.00
4
.004
.004
.002
.07
.004
.04
0.5
10 100 40 30 40 40
1 210
0 40
0.01
500.
01
m m m I 3
tivity of 0.5 ft/d, and a vertical hydraulic conductivity of about Ift/d.
The Prow Pass-upper Bullfrog aquifer may be either an unconfined, anisotropic aquifer or a fissure- block aquifer. If unconfined, the aquifer has an average transmissivity in pumping tests of 3,300 ft2/d, a specific yield of 0.004, a storativity, combined with the Calico Hills aquifer, of 0.0005, a horizontal hydraulic conduc tivity of 10 ft/d, and a vertical hydraulic conductivity of 2 ft/d.
The Bullfrog aquifer is confined, nonleaky, and isotropic. The aquifer has a transmissivity that in bore hole UE-25c #1 was determined to be 8,400 ft2/d and in borehole UE-25c #2 was determined to be 4,100 ft2/d. Assuming the larger value to be correct, the aquifer has a storativity of 0.0002, and a hydraulic conductivity of 100 ft/d.
The Tram aquifer, although confined, is recharged by leakage from faults. The aquifer has a transmissivity of 7,900 ft2/d, a storativity of 0.003, and a hydraulic conductivity of 40 ft/d.
Composite values of hydrologic properties deter mined for rocks in borehole UE-25c #1 by adding or averaging interval values, as appropriate, compare favorably with composite values determined by moni toring borehole UE-25c #2 during a pumping test in borehole UE-25 c#3 and by monitoring borehole UE-25c #3 during an injection test in borehole UE-25c #2. For the entire thickness of rocks pene trated by the c-holes, transmissivity was determined to be between 20,000 and 35,000 ft2/d, storativity was determined to be between 0.002 and 0.004, horizontal hydraulic conductivity was determined to be between 30 and 40 ft/d, and vertical hydraulic conductivity was determined to be between 2 and 5 ft/d.
SELECTED REFERENCES
Barker, J.A., and Black, J.H., 1983, Slug tests in fissured aquifers: American Geophysical Union, Water Resources Research, v. 19, no. 6, p. 1558-1564.
Bredehoeft, J.D., and Papadopulos, S.S., 1980, A method for determining the hydraulic properties of tight forma tions: American Geophysical Union, Water Resources Research, v. 16, no. 1, p. 233-238.
Carr, M.D., Waddell, S.J., Vick, G.S., Stock, J.M., Monsen, S.A., Harris, A.G., Cork, B.W, and Byers, P.M., Jr., 1986, Geology of drill hole UE-25p #1: A test hole into pre-Tertiary rocks near Yucca Mountain, southern Nevada: U.S. Geological Survey Open-File Report 86-175, 87 p.
Carr, W.J., 1990, Styles of extension in the Nevada Test Site region, southern Walker Lane Belt; An integration of volcano-tectonic and detachment fault models, in
Wernicke, B.P., ed., Basin and Range extensional tec tonics near the latitude of Las Vegas, Nevada: Boulder, Colo., Geological Society of America Memoir 176, p. 283-303.
Cooper, H.H., Jr., 1963, Type curves for nonsteady radial flow in an infinite leaky artesian aquifer, in Bentall, Ray, Compiler, Shortcuts and special problems in aqui fer tests: U.S. Geological Survey Water-Supply Paper 1545-C, p. 48-55.
Cooper, H.H., Jr., and Jacob, C.E., 1946, A generalized graphical method for evaluating formation constants and summarizing well-field history: American Geo physical Union Transactions, v. 27, no. 4, p. 526-534.
Cooper, H.H., Jr., Bredehoeft, J.D., and Papadopulos, I.S., 1967, Response of a finite-diameter well to an instanta neous charge of water: American Geophysical Union, Water Resources Research, v. 3, no. 1, p. 263-269.
Driscoll, F.G., 1986, Groundwater and wells: St. Paul, Minnesota, Johnson Division, 1089 p.
Fenix and Scisson, Inc., 1986, NNWSI hole historiesUE-25c #1, UE-25c #2, UE-25c #3: Tulsa, Okla., 60 p.
Freeze, R.A., and Cherry, J.A., 1979, Groundwater: Engle- wood Cliffs, N.J., Prentice-Hall, Inc., 604 p.
Frizzell, V.A., Jr., and Shulters, Jacqueline, 1990, Geologic map of the Nevada Test Site, southern Nevada: U.S. Geological Survey Miscellaneous Investigations Map 1-2046, scale 1:100,000.
Galloway, D.L., and Rojstaczer, Stuart, 1988, Analysis of the frequency response of water levels in wells to Earth tides and atmospheric loading, in Hitchon, Brian, and Bachu, Stefan, eds., Proceedings Fourth Canadian/ American Conference on Hydrogeology - Fluid flow, heat transfer, and mass transport in fractured rocks: Dublin, Ohio, National Water Well Association, p. 100-113.
Geldon, A.L., 1993, Preliminary hydrogeologic assessment of boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada: U.S. Geologi cal Survey Water-Resources Investigations Report 92-4016, 85 p.
Gringarten, A.C., 1982, Flow-test evaluation of fractured reservoirs, in Narasimhan, T.N., ed., Recent trends in hydrogeology: Boulder, Colo., Geological Society of America Special Paper 189, p. 237-263.
Hess, A.E., 1990, Thermal-pulse flowmeter for measuring slow velocities in boreholes: U.S. Geological Survey Open-File Report 87-121, 70 p.
Lobmeyer, D.H., Whitfield, M.S., Lahoud, R.R., and Bruckheimer, Laura, 1983, Geohydrologic data for test well UE-25b #1, Nevada Test Site, Nye County, Nevada: U.S. Geological Survey Open-File Report 83-855,48 p.
Lohman, S.W., 1979, Ground-water hydraulics: U.S. Geo logical Survey Professional Paper 708, 70 p.
SELECTED REFERENCES 71
Nelson, P.H., Muller, D.C., Schimschal, Ulrich, and Kibler, J.E., 1991, Geophysical logs and core measurements from forty boreholes at Yucca Mountain, Nevada: U.S. Geological Survey Geophysical Investigations MapGP-1001.
Neuman, Shlomo, 1975, Analysis of pumping test data from anisotropic unconfined aquifers considering delayed gravity response: American Geophysical Union, Water Resources Research, v. 11, no. 2, p. 329-342.
Neuzil, C.E., 1982, On conducting the modified "slug" test in tight formations: American Geophysical Union, Water Resources Research, v. 18, no. 2, p. 439-441.
Reed, J.E., 1980, type curves for selected problems of flow to wells in confined aquifers: U.S. Geological Survey Techniques of Water-Resources Investigations, book 3, chap. B3.
Robison, J.H., and Craig, R.W., 1991, Geohydrology of rocks penetrated by test well USW H-5, Yucca Moun tain, Nye County, Nevada: U.S. Geological Survey Water-Resources Investigations Report 88-4168, 44 p.
Robison, J.H., Stephens, D.M., Luckey, R.R., and Baldwin, D. A., 1988, Water levels in periodically measured wells in the Yucca Mountain area, Nevada, 1981-87: U.S. Geological Survey Open-File Report 88-468, 132 p.
Rush, F.E., Thordarson, William, and Bruckheimer, Laura, 1983, Geohydrologic and drill-hole data for test well USW H-l, adjacent to Nevada Test Site, Nye County, Nevada: U.S. Geological Survey Open-File Report 83-141, 38 p.
Scott, R.B., 1990, Tectonic setting of Yucca Mountain, southwest Nevada in Wernicke, B.P., ed., Basin and Range extensional tectonics near the latitude of Las Vegas, Nevada: Boulder, Colo., Geological Society of America Memoir 176, p. 251-282.
Scott, R.B., and Bonk, Jerry, 1984, Preliminary geologic map of Yucca Mountain, Nye County, Nevada, with geologic sections: U.S. Geological Survey Open-File Report 84-494, scale 1:12,000.
Streltsova-Adams, T.D., 1978, Well testing in heterogeneous aquifer formations, in Chow, V.T., ed., Advances in hydroscience: New York, Academic Press, v. 11, p. 357-423.
Theis, C.V., 1935, The relation between the lowering of the piezometric surface and the rate and duration of dis charge of a well using ground-water storage: American Geophysical Union Transactions, v. 16, p. 519-524.
72 Results and Interpretation of Preliminary Aquifer Tests in Boreholes UE-25c #1, UE-25c #2, and UE-25c #3, Yucca Mountain, Nye County, Nevada
SUPPLEMENTAL DATA
SUPPLEMENTAL DATA 73
74
Results
and
Nye
County, af
fl»
9 1 S. F
Preliminary
Aquifer T iw 5* o 3 0 « C m k
% i? % ,r* 5 i? $ 3 a C i S g s 1 ^
TA
BL
E 1
0.
SUM
MA
RY
OF
INFO
RM
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ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELEV
ISIO
N (
TV),
AC
OU
STIC
TEL
EVIE
WER
(A
T), C
ALI
PER
(C
), A
ND
TE
MPE
RA
TU
RE
(T
EM
P) L
OG
S FO
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OL
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5C #
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[Abb
revi
atio
ns fo
r tab
les
10, 1
1, a
nd 1
2: S
G, c
asin
g; N
W, n
onw
elde
d; N
W-P
W, n
onw
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par
tially
wel
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MW
, mod
erat
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wel
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MW
-DW
, mod
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to d
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ly w
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artia
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wel
ded
to n
onw
elde
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W, p
artia
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elde
d; N
.VER
T, n
ear v
ertic
al; L
JTH
, lith
olog
ic; T
D, t
otal
dep
th; N
, nor
th, S
, sou
th; S
W, s
outh
wes
t, SE
, sou
thea
st; S
SW, s
outh
-sou
thw
est]
DE
PTH
BLW
C
ASI
NG
(F
EE
T)
GE
OL
OG
IC U
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TO
P
1313
1332
13
62
1362
1427
1461
1486
1486
1505
1506
1510
1515
1521
1522
1523
1523
1525
1530
1530
1531
1532
1535
1535
1541
1561
1582
BOT
TO
M
TOPO
PAH
SPR
ING
CA
LIC
O H
ILLS
1371
1428
1461
1486
1487
1506
1506
1511
1516
1523
1524
1525
1534
1528
1534
1531
1532
1532
1541
1535
1544
1562
1584
LITH
G'C
«niH
E£U
Nc
DIP
A
ZI
MUT
HD
IP A
NG
LEST
RIK
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IM
UTH
BA
SAL
WA
TER
TA
BLE
NW
C
ON
TAC
T B
OTT
OM
OF
CSG
CO
NC
RET
E
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
LED
GE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
265
225
280
225 20 30 95 180
210 95 275 95 105
270
260
260
350
145
270
255
170
N.V
ER
T
SHA
LLO
WN
.VE
RT
SHA
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WST
EEP
STEE
P
STEE
PST
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STEE
PST
EEP
VER
TIC
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N.V
ER
TN
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RT
STEE
PST
EEP
STEE
PV
ERTI
CA
LST
EEP
N.V
ER
TSH
ALL
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STEE
P
175
135
190
135
290
300 5 90 120 5
185 5 15 180
170
170
260 55 180
165 80
REM
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AB
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FOR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, TE
LEV
ISIO
N (
TV),
AC
OU
STI
C T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TUR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#1
-Con
tinue
d
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L
°1
°G
IC
FEA
TUR
E
TO
P
1592
1593
1623
1636
1636
1638
1672
1691
1693
1722
1759
1767
1778
1785
1791
1802
1803
1805
1806
1806
1806
1808
1809
1809
1811
1815
BOT
TO
M
1593
C
ALI
CO
HIL
LS
NW
BED
DED
1630
1637
1637
1639
1673
1692
PR
OW
PA
SS
NW
-PW
1694
1722
1765
1768
1778
1785
1791
1802
1804
1806
1806
1807
1808
1809
1810
1813
1817
1821
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
AZ
I M
UTH
285
287
270
180
285
170
117
305
309
315
285
230
210
230
315
230
125
230
245
190
250
298
300
215
DIP
AN
GLE
VER
TIC
AL
83N
.VE
RT
SHA
LLO
WN
. VER
TN
.VE
RT
27ST
EEP
80N
. VER
TST
EEP
SHA
LLO
WSH
ALL
OW
SHA
LLO
WSH
ALL
OW
N.V
ER
TSH
ALL
OW
STEE
PST
EEP
N.V
ER
TN
. VER
T76
VER
TIC
AL
VER
TIC
AL
STR
IKE
AZI
M
UTH
195
197
180 90 195 90 27 215
219
225
195
140
120
140
225
140 35 140
155
100
160
208
210
125
REM
ARK
S LO
G
TV
TEX
TUR
E R
OU
GH
ER A
ND
VIS
IBIL
- L
ITY
PO
OR
ERA
TTV TV TV TV
OPE
N P
AR
TIN
G
TV/L
AT
TV AT
TV TV TV TVM
INER
ALI
ZED
TV TV TV TV TV TV TV TV A
TTV TV
76T
AB
LE
10.
S
UM
MA
RY
OF
IN
FO
RM
AT
ION
FR
OM
LIT
HO
LOG
IC (
L),
TE
LEV
ISIO
N (
TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
AT
UR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#1
-Co
ntin
ue
d
Results
ant Ny
e Coun
t] fl
|| 1 a I i | > i I 5" 0 1 J m » _t c s » * 8. m K* 2 "-< 1 s § 1 "
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
""!!
*£
*
TOP
1817
1818
1818
1819
1819
1820
1821
1821
1822
1822
1823
1823
1823
1825
1825
1828
1830
1831
1832
1833
1834
1834
1835
1835
1835
1836
1836
1837
1837
BO
TTO
M
1818
PR
OW
PA
SS
NW
-PW
1819
1819
1819
1821
1821
1821
1823
1822
1822
1823
1823
1824
1825
1825
1828
1830
1833
1833
1834
1835
1835
1837
1836
1840
1836
1836
1837
1839
FEA
TUR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH
255
235
245
245
235
250
235
105
110
100
105
200
285 15 240
250
175 35 5
255
330
100
235
110
284
260
145
190
245
DIP
AN
GLE
STE
EP
N. V
ER
TN
. VE
RT
N. V
ERT
N.V
ER
TN
.VE
RT
N. V
ERT
N.V
ER
TN
.VE
RT
N. V
ER
TN
.VE
RT
N. V
ER
TST
EE
PN
. VE
RT
N.V
ER
TV
ER
TIC
AL
N. V
ER
TST
EE
PN
.VE
RT
VE
RT
ICA
LST
EE
PST
EE
PN
. VER
TN
.VE
RT
79N
. VER
TN
.VE
RT
N.V
ER
TN
. VE
RT
STR
IKE
AZI
- R
EMA
RK
SM
UTH
165
145
155
155
145
160
145 15
O
PEN
AT
UPT
OE
20 10 15 110
195
285
OPE
NA
TD
OW
NT
OE
150
160 85 305
275
165
240 10 145
CA
VED
AT
UPT
OE
20 194
170 55 100
155
LOG
TV TV
TV
TV
TV
TV
TV
TV
TV
TV TV
TV
TV
TV TV
TV
TV
TV
TV
TV
TV
TV TV
TV
AT
TV
TV
TV TV
TAB
LE 1
0.
SU
MM
AR
Y O
F IN
FOR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, TE
LEV
ISIO
N (
TV),
AC
OU
STI
C T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TUR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#1
-Con
tinue
d
DE
PTH
BLW
C
ASI
NG
(FE
ET
) G
EO
LO
GIC
UN
IT
"""^S
^6
'0
FEA
TUR
E
TO
P
1838
1839
1839
1839
1840
1840
1840
1841
1841
1842
1843
1843
1844
1844
1860
1860
1860
1866
1871
1879
1884
1887
1890
H
1892
o
1893
m
18%
®
1898
1899
BOT
TO
M
DIP
AZ
I M
UTH
DIP
AN
GLE
STR
IKE
A
Zh
RE
MA
RK
S M
UTH
PRO
W P
ASS
M
W
CO
NTA
CT
1841
1839
1840
1840
1841
1846
1841
1843
1842
1843
1843
1844
1845
1860
1860
1861
1871
1872
1883
1884
1888
1892
1893
1895
1898
1899
1901
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
PW-N
W
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
285
110
165 95 295
260
115
200 75 285
265
235
235
275
220
263
240
273
260
235
272
200
258
281
105
277
N.V
ER
TN
. VER
TN
. VER
TST
EEP
N.V
ER
T82
SHA
LLO
WST
EEP
N. V
ERT
N. V
ERT
N. V
ERT
N. V
ERT
N.V
ER
TSH
ALL
OW
SHA
LLO
W
80ST
EEP
79N
.VE
RT
STEE
P70
N.V
ER
TN
. VER
T58
N. V
ERT
64
195 20 75 5
205
170 25 110
345
195
175
145
145
185
130
OPE
N P
AR
TIN
G17
315
018
317
014
518
211
016
819
1 15 187
LOG
L TV TV TV TV TV AT
TV TV TV TV TV TV TV TV TV TV/L
AT
TV AT
TV TV AT
TV TV AT
TV AT
78
Results
am Nye
Coun
t) d
Interpre
f, Nevada
g o i 3 i > c H § 3 0 i 1 c
m g| 2 c m $» S fl» c
m IS> s s IE g i -3
TAB
LE 1
0. S
UM
MA
RY O
F IN
FOR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L),
TELE
VIS
ION
(TV
), A
CO
UST
IC T
ELEV
IEW
ER (
AT)
, CA
LIPE
R (
C),
AN
D T
EMPE
RA
TUR
E (T
EMP)
LO
GS
FOR
BO
REH
OLE
UE-
25C
#1
-Con
tinue
d
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L °!£
GIC
TOP
1902
1907
1910
1911
1919
1920
1921
1924
1939
1940
1942
1943
1947
1963
1974
1982
2071
2079
2081
2087
2114
2115
2118
2118
.211
921
2121
2221
24
BOT
TO
M
1903
PR
OW
PA
SS
PW-N
W19
0919
1019
1319
2219
2119
2219
2519
4219
4119
4819
4519
5019
6419
7519
8520
71
2079
2081
2087
2115
2118
BED
DED
2119
2119
2122
2122
2124
FEA
TUR
E
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
AZI
MUT
H
295
262
195
260
275
180
105
105
275
280
280
290
322
105
110
273
265
180
215
145 25 285
270
235
272
260
280
DIP
AN
GLE
STEE
PST
EEP
SHA
LLO
WST
EEP
STEE
PST
EEP
SHA
LLO
WSH
ALL
OW
N. V
ERT
STEE
PV
ERTI
CA
L63 74 28 44 73
SHA
LLO
W
VER
TIC
AL
VER
TIC
AL
VER
TIC
AL
N. V
ERT
VER
TIC
AL
N. V
ERT
N.V
ER
T30 22
SHA
LLO
W
STRI
KE
AZI
M
UTH
205
172
105
170
185 90 15 15 185
190
190
200
232 15 20 183
175 90 125 55 295
195
180
145
182
170
190
REM
ARK
S
MA
NY
SPL
AY
S
BO
TH T
OES
OPE
N (C
AV
ED)
OPE
NA
TU
PTO
E
OPE
N
OPE
NO
PEN
VIS
IBIL
ITY
PO
OR
206
1-21
18B
ECA
USE
OF
SKEW
ED H
OLE
OPE
N
SMO
OTH
ER T
EXTU
RE,
CO
RR
UG
A
TIO
NS
AT
CO
NTA
CT
LOG
TV TV TV TV TV TV TV TV TV TV TV AT
AT
AT
AT
AT
TV TV TV TV TV TV TV/L
TV TV AT
AT
TV
TAB
LE 1
0.
SU
MM
AR
Y O
F IN
FOR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, TE
LEV
ISIO
N (
TV),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TUR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#1
-Con
tinue
d
09
DEP
TH B
LW
CA
SIN
G
(FE
ET
) G
EOLO
GIC
UN
IT
U **
TO
P
2125
2127
2130
2130
2137
2140
2146
2150
2151
2152
2152
2153
2181
2182
2201
2204
2204
2206
2209
2209
2215
2216
2216
2217
2219
2230
2234
2238
BO
T
TOM
2125
PR
OW
PA
SS
BE
DD
ED
2129
2131
2131
2138
2141
2147
2150
2152
2152
2153
B
UL
LFR
OG
N
W-P
W21
5621
8221
8322
0222
0422
0422
0622
0922
1022
1522
1622
1822
2222
2022
3022
3422
38
FEA
TUR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
DIP
A
ZI
MU
TH
325
274
265 35 145
291
259
120
160
120
131 5 5
175
320 95 285
220
225
110
265
220
283
260
220 90 240
DIP
AN
GLE
N. V
ER
T58 42
VE
RT
ICA
L49 59 30
SHA
LL
OW
SHA
LL
OW
VE
RT
ICA
L
25SH
AL
LO
WSH
AL
LO
WN
. VE
RT
SHA
LL
OW
SHA
LL
OW
N. V
ER
TSH
AL
LO
WSH
AL
LO
WN
. VE
RT
SHA
LL
OW
N. V
ER
T78
VE
RT
ICA
LN
. VE
RT
VE
RT
ICA
LN
. VE
RT
STR
IKE
AZI
- R
EMA
RK
S M
UTH
235
184
175
305 55
O
PEN
201
169 30 70 30
OPE
N P
AR
TIN
G41 27
527
5 85 230 5
195
130
135 20 175
130
OPE
N19
317
013
0 015
0 O
PEN
UPT
OE
LOG
TV
AT
AT
TV
AT
AT
AT
TV
TV
TV TV
/LA
TT
VT
V TV
TV TV
TV
TV
TV
TV
TV
TV
AT
TV
TV
TV
TV
g
TA
BL
E 1
0.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT
), C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
1 -C
on
tinu
ed
Results
and
Interpretation of
Preli
Nye County, Nevada
3 S > 1 H 2. 5" 09 I 1 m K * F * -J Q.
C g 9"< 8 s § |
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
"^JS
?"
TOP
2239
22
4122
41
2260
2270
22
8123
0123
1123
1223
1523
1823
2023
2723
3223
42
2352
23
6223
6323
6523
6623
6823
7823
8523
8723
9023
9224
0724
2424
3224
36
BOT
TO
M
2240
B
ULL
FRO
G
NW
-PW
2241
2243
BU
LLFR
OG
M
W-D
W22
74
2281
2304
2314
2313
2318
2318
2326
2328
2333
2344
23
58
2364
2363
2370
2366
2370
2381
2385
2388
2391
2397
2411
2427
2436
2439
J FE
ATU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
210
240
267
235
265
250
280 55 10 245
190 10 270
190
265
260
270
255
225
230
205
260
245
250
190
255
267
275
285
DIP
AN
GLE
N. V
ERT
N. V
ERT
67
N.V
ER
T
N. V
ERT
N. V
ERT
N.V
ER
TN
. VER
TN
. VER
TN
.VE
RT
VER
TIC
AL
STEE
PN
.VE
RT
N. V
ERT
VER
TIC
AL
N. V
ERT
N. V
ERT
VER
TIC
AL
N. V
ERT
N. V
ERT
N. V
ERT
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N.V
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TV
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T67
N.V
ER
TV
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L
STRI
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H
120
150
177
145
175
160
190
325
280
155
100
280
180
100
175
170
180
165
135
140
115
170
155
160
100
165
177
185
195
REM
ARK
S
MIN
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D
MIN
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DM
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ALI
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DPA
RTL
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DM
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MIN
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D
LOG
TV
TV AT
L TV
TV
TV TV TV TV TV TV TV TV TV
TV
TV TV TV TV TV TV TV TV TV TV TV AT
TV TV
TA
BL
E 1
0.
SU
MM
AR
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F I
NF
OR
MA
TIO
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M L
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LEV
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N (
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AC
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AN
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TU
RE
(T
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LOG
S F
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BO
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on
tinu
ed
DE
PTH
BLW
C
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(F
EE
T)
GEO
LOG
IC U
NIT
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2449
2450
2454
2463
2466
2469
2476
2479
2479
2480
2482
2489
2498
2498
2502
2516
2525
2526
2534
2535
2537
2542
2543
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2547
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2548
2549
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2453
2457
2476
2466
2471
2478
2483
2484
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9025
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0825
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2725
2925
3525
3525
4125
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4425
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FRA
CTU
RE
FRA
CTU
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CTU
RE
FRA
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RE
DIP
AZ
I M
UTH
260
265
258
190
145
245
185
287
293
291
200
282
220
278
235
215
264
220 85 270
240
260
215
200
282
220
DIP
AN
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E
N. V
ER
T
N. V
ER
T
N. V
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T
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RT
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L
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RT
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78 80 79
N. V
ER
T
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VE
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81
N. V
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T
ST
EE
P
68
N. V
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T
N. V
ER
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RT
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T
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EE
P
67
ST
EE
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STR
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A
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RE
MA
RK
S M
UTH
170
175
MIN
ERA
LIZE
D16
8 PA
RTL
Y M
INER
ALI
ZED
100 55 155 95 197
OPE
N20
3 O
PEN
201
OPE
N11
019
2 O
PEN
130
188
OPE
N14
512
517
413
0 O
PEN
355
OPE
N18
0 O
PEN
150
170
125
1 10
TER
MIN
ATE
D B
Y S
SW-S
TRIK
ING
FRA
CTU
RE
192
130
LOG
TV TV TV
TV
TV TV TV AT
AT
L AT
TV AT
TV AT
TV TV AT
TV TV TV TV TV TV TV AT
TV
B n ft f 1
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ATI
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FRO
M L
ITH
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TELE
VIS
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T), C
ALI
PER
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AN
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EMP)
LO
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FOR
BO
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UE-
25C
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ontin
ued
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
"""^
Me6
'0
TOP
2554
2558
2565
2568
2572
2572
2572
2572
2574
2574
2574
2574
2577
2578
2578
2588
2590
2590
2594
2603
2656
2677
2682
2694
2695
2698
2703
BOT
TOM
2556
B
ULL
FRO
G
PW-N
W25
6025
6625
6925
72
2572
2573
2573
2575
2575
2575
2575
2578
2578
2579
2589
2591
2591
2595
2604
2657
2679
2684
2695
BED
DED
2699
2704
FEA
TURE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
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FRA
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AC
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AC
TU
RE
CO
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CT
UR
EFR
AC
TU
RE
DIP
AZ
IM
UTH
260
277
205
135
295 80 165
195
150
150 90 83 105
110
110
122 85 85 110
105 80 110
108
108 95 110
DIP
AN
GLE
N. V
ERT
70N
.VE
RT
STEE
PSH
ALL
OW
SHA
LLO
WV
ERTI
CA
LV
ERTI
CA
LSH
ALL
OW
SHA
LLO
WN
. VER
T32
SHA
LLO
W
SHA
LLO
WSH
ALL
OW
SHA
LLO
WSH
ALL
OW
SHA
LLO
WSH
ALL
OW
SHA
LLO
WSH
ALL
OW
STE
EP
STEE
PSH
ALL
OW
SHA
LLO
WSH
ALL
OW
STRI
KE
AZI
MUT
H
170
187
115 45 205
350 75 105 60 60 0
353 15 20 20 32 355
355 20 15 350 20 18 18 5 20
RE
MA
RK
S
OPE
N, C
AV
ING
OPE
N; H
OLE
EN
LAR
GED
BY
FRA
CTU
RES
257
2-25
73O
PEN
OPE
NO
PEN
OPE
N; H
OLE
EN
LAR
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BY
FRA
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RES
257
4-25
75O
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NO
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AC
TUR
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577-
2579
OPE
NO
PEN
LOG
TV AT
TV TV TV TV TV TV TV TV TV AT
TV TV TV TV TV TV TV TV TV TV TV TV L TV TV
TAB
LE 1
0. S
UM
MA
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OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
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(TV
), A
CO
US
TIC
TE
LEV
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(A
T),
CA
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(C
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ND
TE
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(T
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LOG
S F
OR
BO
RE
HO
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DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
^"oM
c6
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FEA
TUR
E
TABLE o
TOP
2708
2715
2716
2718
2729
2730
2730
2731
2731
2732
2733
2734
2735
2742
2742
2742
2743
2750
2759
2761
2762
2762
2763
27
63
2764
2765
2766
BO
T
TOM
2709
B
UL
LFR
OG
2715
TR
AM
2718
2729
2731
2731
2733
2734
2733
2733
2734
2738
2743
2742
2743
2750
2752
2760
2761
2763
2764
2764
27
64
2765
2766
2767
BE
DD
ED
FR
AC
TU
RE
FRA
CT
UR
E
UPP
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(N
W-P
W)
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
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AC
TU
RE
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CT
UR
EFR
AC
TU
RE
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CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
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CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
DIP
A
ZI
MU
TH
105
110
285
325
105
300
127
297
285
210
205
304 85 5
195
355
300
290
305
305
280
205 35
30
5 029
3
DIP
AN
GLE
SHA
LL
OW
SHA
LL
OW
N. V
ER
TN
. VE
RT
SHA
LL
OW
VE
RT
ICA
L56 68
N.V
ER
TV
ER
TIC
AL
STE
EP
66SH
AL
LO
WSH
AL
LO
WN
. VE
RT
VE
RT
ICA
L
55N
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RT
SHA
LL
OW
SHA
LL
OW
64ST
EE
P SH
AL
LO
W
64SH
AL
LO
W62
STR
IKE
AZI
- R
EMA
RK
S M
UTH 15 20 195
MIN
ER
AL
IZE
D23
5 15 210 37 207
195
120
115
MIN
ER
AL
IZE
D21
435
527
5 O
PEN
105
OPE
N26
5 C
AV
ERN
OU
S; H
OL
E F
OL
LO
WS
FRA
CT
UR
E21
020
0 O
PEN
215
OPE
N21
519
011
5 C
AV
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OU
S U
PTO
E
305
215
270
203
LOG
TV
TV TV
L TV
TV
TV
TV
AT
AT
TV
TV
AT
TV
TV TV
TV
AT
TV
TV
TV
AT
TV
T
V
AT
TV
AT
S
8
TA
BL
E 1
0.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(T
V),
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OU
ST
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ELE
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WE
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RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
1 -C
on
tinu
ed
Results
and
Interpretation of
F
Nye
County, Nevada
3 3 g > i 51 § 5" 1 CD C m <P 2 c
m 81 i i ^ 0 I i 3
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
TO
P
2766
2767
2768
27
6827
6827
70
2770
2772
2773
2774
2775
2776
2777
2777
27
7727
8027
8227
8427
8427
84
2784
2787
2788
27
9027
9127
9127
94
BO
T
TOM
2768
T
RA
M27
6827
68
2768
2770
2771
27
7227
7327
7427
75
2776
2777
2779
27
7927
8227
8327
8427
8627
86
2784
2789
2790
27
9127
9127
9127
95
NIT
U
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C FE
ATU
RE
UPP
ER
(NW
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) FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
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FRA
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EFR
AC
TU
RE
FRA
CT
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E
TU
FF B
RE
CC
IA
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
DIP
A
ZI
MU
TH
299
303
330
335
279
266
278
289
284
291
260
305
300
260
281
287 50 293
266
240
275
282
110
345 30 195
DIP
AN
GLE
64 64
STE
EP
STE
EP
61 59
66 58 57 53
SHA
LL
OW
STE
EP
STE
EP
STE
EP
63 51SH
AL
LO
W64 48
ST
EE
P65 64
N
.VE
RT
N.V
ER
TN
.VE
RT
N.V
ER
T
STR
IKE
AZI
M
UTH
209
213
240
245
189
176
188
199
194
201
170
215
210
170
191
197
320
203
176
150
185
192 20 255
300
105
REM
AR
KS
LOG
AT
AT
TV
T
VA
TA
T A
TA
TA
TA
T
L TV
OPE
N;
HO
LE
EN
LA
RG
ED
BY
T
VFR
AC
TU
RE
S 27
77-2
779
TV
T
VA
TA
TT
VA
TA
T T
VPA
INT
BR
USH
CA
NY
ON
FA
ULT
ON
A
T/L
LIT
HL
OG
AT
TV TV
TV
TV
TV
TA
BL
E 1
0.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
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GIC
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, T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
1 -C
on
tinu
ed
DEP
TH B
LW
CA
SIN
G(F
EET)
G
EOLO
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FE
ATU
RE
TO
P
2794
2794
2795
2795
2796
2796
2796
2802
2803
2804
2814
2816
2817
2820
2822
2822
2828
2832
2836
2836
2837
2838
2840
2843
>
2843
m
2845
o
2845
2850
BO
T
TOM
2794
T
RA
M27
9527
9527
9527
9627
9728
0228
0228
0428
0428
1628
2028
1828
2228
2228
2828
30
2833
2837
2838
2838
2839
2840
2844
2844
2845
2847
2851
TU
FF B
RE
CC
IA
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
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EFR
AC
TU
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FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH
200
200
345
155
205
320
116
175
200
200
220
255
230
270
265
225
198 65 50 70 10 164
285 35 20 15 20 15
DIP
AN
GLE
N. V
ER
TN
. VE
RT
VE
RT
ICA
LN
. VE
RT
N. V
ER
TN
. VE
RT
82N
. VE
RT
N. V
ER
TN
. VE
RT
N. V
ER
T76
STE
EP
64ST
EE
PV
ER
TIC
AL
STE
EP
N. V
ER
TN
. VE
RT
N. V
ER
TST
EE
P56
N.V
ER
TSH
AL
LO
WSH
AL
LO
WSH
AL
LO
WST
EE
PST
EE
P
STR
IKE
AZI
M
UTH
110
110
255 65 115
230 26 85 110
110
130
165
140
180
175
135
108
335
320
340
280 74 195
305
290
285
290
285
REM
AR
KS
LOG
TV
TV TV
TV TV
TV
OPE
N
AT
TV
TV
TV TV
AT
OPE
N
TV
AT
TV
SPLA
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T
VT
RU
NC
AT
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TR
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TV
FRA
CT
UR
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BO
VE
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LO
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AC
TU
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FA
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TV
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MIN
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AL
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D
TV AT
TV
MIN
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AL
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D
TV
MIN
ER
AL
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D
TV
MIN
ER
AL
IZE
D
TV
MIN
ER
AL
IZE
D
TV
MIN
ER
AL
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D
TV
TA
BL
E 1
0.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
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GIC
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ELE
VIS
ION
(T
V),
AC
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ST
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ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
1 -C
on
tinu
ed
Results
and
Interpretation of
Preli
Nye County, Nevada
3 1 > 1 i1 i CO 5* 0 i 1 c
m S? a 5 s £ i m 1 cS "^ 1 s o | -
DEP
TH B
LW
CASI
NG
(F
EET)
G
EOLO
GIC
UN
IT
TOP
2854
28
5428
5628
5728
5828
59
2860
2860
2863
2865
2866
2867
2868
2868
2870
2870
28
7228
7228
7228
7228
7328
7428
75
2875
2876
2876
28
7728
7728
7828
79
BOT
TO
M
2857
TR
AM
28
5728
5628
5828
5928
60
2860
2863
2866
2867
2868
2870
2868
2870
2870
2872
28
7328
7228
7228
7628
7328
7428
78
2875
2876
2876
28
7728
8028
7928
79
LIT
ZON
^GIC
FE
ATU
RE
TUFF
BR
ECC
IA
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FAU
LT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
80
75 35 255 65 265 65 60 121
270
115
279
125 70 5 55
119
270 95 65 180
265
320
290
180
250 0
210 95 305
DIP
AN
GLE
N. V
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N. V
ERT
SHA
LLO
WN
. VER
TSH
ALL
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N.V
ER
T
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. VER
T71
STEE
PN
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N. V
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STEE
PSH
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OW
SHA
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W
64V
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CA
LV
ERTI
CA
LN
.VE
RT
N.V
ER
TV
ERTI
CA
LV
ERTI
CA
L
VER
TIC
AL
SHA
LLO
WN
.VE
RT
SH
ALL
OW
N. V
ERT
N. V
ERT
VER
TIC
AL
STR
IKE
AZI
M
UTH
350
345
305
165
335
175
335
330 31 160 25 189 35 340
275
325 29 180 5
335 90 175
230
200 90 160
270
120 5
215
REM
ARK
S
MIN
ERA
LIZE
D
PART
LY M
INER
ALI
ZED
MIN
ERA
LIZE
DO
PEN
MIN
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D
MIN
ERA
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D
MIN
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D
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SE-
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RA
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RE
AT
2877
PART
LY M
INER
ALI
ZED
PART
LY M
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ALI
ZED
LOG
TV
TV TV TV TV TV
TV TV AT
TV TV AT
TV TV TV AT
TV TV TV TV TV TV TV TV TV TV
TV TV TV TV
TAB
LE 1
0. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
1 -C
ontin
ued
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L
mi°
TA
BL
E 1
0.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, TE
LEV
ISIO
N (
TV),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
1 -C
on
tinu
ed
Results atv
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m 1 1 8
DEP
TH B
LW
CASI
NG
(F
EET)
G
EOLO
GIC
UN
IT
^"S
uc
610
FEA
TURE
TOP
2921
2921
2922
2923
2924
2924
2925
2925
2926
2926
2929
2930
2930
2933
2935
2935
2936
2937
2940
2941
2954
2962
BOT
TOM
2921
TR
AM
2922
2923
2924
2924
2925
2925
2927
2926
2926
2930
2930
2931
2933
2935
2936
2937
2937
2940
2941
2955
TU
FF B
RE
CC
IA
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
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FRA
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AC
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FRA
CT
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AC
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TU
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FRA
CT
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AC
TU
RE
FRA
CT
UR
EB
OT
TO
M
DIP
A
ZI
MU
TH 55 15 265
260 80 260 60 60 50 90 115
105
310
280 70 130
185 65 305
250
285
DIP
AN
GLE
VE
RT
ICA
L
N. V
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STEE
PST
EE
PN
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TST
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PST
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STE
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TN
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RT
N. V
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SHA
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RT
SHA
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RT
N.V
ER
TN
.VE
RT
N.V
ER
TN
. VER
TN
.VE
RT
STR
IKE
AZI
- R
EMA
RK
SM
UTH
325
285
175
170
350
170
330
330
320 0 25 15 220
190
340
OPE
N40 95 33
521
516
019
5H
OL
E C
AV
ED T
O O
RIG
INA
L T
DA
T 30
00
LOG
TV
TV TV
TV TV
TV
TV
TV TV
TV TV
TV
TV
TV
TV
TV
TV
TV TV
TV TV
TV
TA
BL
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1.
SU
MM
AR
Y O
F I
NF
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MA
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(C
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TE
MP
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AT
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E
(TE
MP
) LO
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FO
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OR
EH
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#2
[Abb
revi
atio
ns fo
r tab
les
10,1
1, a
nd 1
2: C
SG, c
asin
g; N
W, n
onw
elde
d; N
W-P
W, n
onw
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d to
par
tially
wel
ded;
MW
, mod
erat
ely
wel
ded;
MW
-DW
, mod
erat
ely
to d
ense
ly w
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d; P
W-N
W, p
artia
lly
wel
ded
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d; P
W, p
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lly w
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d; N
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T, n
ear v
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al; L
ITH
, lith
olog
ic; T
D, t
otal
dep
th; N
, nor
th, S
, sou
th; S
W, s
outh
wes
t, SE
, sou
thea
st; S
SW, s
outh
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thw
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TH B
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(FEE
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GEO
LOG
IC U
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"^S
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FEA
TUR
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TOP
1315
1316
1360
1360
1395
1461
1461
1465
1467
1510
1514
1515
1518
1550
1552
1570
1600
1624
1624
1626
1626
1627
1627
1628
1629
1630
BO
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DIP
A
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1469
1470
1472
1477
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1539
1555
1552
1600
1625
1625
1626
1626
1627
1628
1629
1630
1631
CSG
BO
TT
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CO
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RE
TE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
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FRA
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AC
TU
RE
FRA
CT
UR
EFR
AC
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LE
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AC
TU
RE
FRA
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AC
TU
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C
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AC
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RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
235 65 65 95 75 255 65 70 90 120
120
120
120
120
115
105
110
120 75 100
35 81 82 79 82 >35 86 87 >78
VE
RT
ICA
L
32 43 27 27 43 36 36 45 35 48
145
335
335 5
345
165
335
340 0 30 30 30 30 30 25 15 20 30 345 10
REM
AR
KS
LOG
TV
L TV
RO
UG
H; S
PALL
ED; H
OL
E
TV
/C
AB
RU
PTL
Y W
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NS
BE
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365-
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TV
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N
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TVH
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N
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TV
TV
TV
TV
TV TV
MIN
ER
AL
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D
TV
AT
PAR
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MIN
ER
AL
IZE
D
TV
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
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2 -C
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Results
an< Ny
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i "0 3 1 1 | i s1 5" 1 1 (D C i _* C $ S &> C s s £ s 2 f i P
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"^ow
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TOP
1631
1632
1633
1644
1645
1645
1646
1650
1652
1652
1653
1653
1653
1654
1655
1655
1655
1655
1656
1656
1658
1658
1659
1659
1660
1661
1663
1664
BOT
TO
M16
32
CA
LIC
O H
ILLS
B
EDD
ED16
3316
3416
4516
4516
50
1650
1653
1652
1653
1653
1653
1654
1654
1655
1656
1656
1656
1656
1657
1658
1659
1659
1660
1660
1662
1664
1665
FEA
TURE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
AZ
IM
UTH
110
110
105
110
145 75 225
255
115 15 225
320
270 20 75 155
115
115
120
120
120
120
125
125
125
130
130
315
DIP
AN
GLE
48 40 42 40V
ERTI
CA
L78 74 68 27
VER
TIC
AL
VER
TIC
AL
VER
TIC
AL
27 27 22ST
EEP 26 26 26 26 30 30 16 16 21 34 26 22
STRI
KE
AZI
M
UTH
20 20 15 20 55 345
135
165 25 285
135
230
180
290
345 65 25 25 30 30 30 30 35 35 35 40 40 225
REM
ARK
S
MIN
ERA
LIZE
DM
INER
ALI
ZED
OPE
N
OPE
N A
T IN
TER
SEC
TIO
N W
ITH
SE-S
TRIK
DSf
G F
RA
CTU
RE
OPE
N A
T IN
TER
SEC
TIO
N W
ITH
N-S
TRIK
DSf
G F
RA
CTU
RE
MIN
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D
RO
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CH
AN
GES
CO
LOR
BEL
OW
FRA
CTU
RE
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
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LIZE
DM
INER
ALI
ZED
MIN
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LIZE
DM
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ALI
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MIN
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DM
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ALI
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MIN
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LIZE
DM
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ALI
ZED
MIN
ERA
LIZE
DM
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ALI
ZED
MIN
ERA
LIZE
DM
INER
ALI
ZED
LOG
TV TV AT
TV TV TV TV AT
TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV
TA
BL
E 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 -C
ontin
ued
09
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L
mJ°
w°G
IC
TOP
1665
1665
1666
1670
1671
1672
1676
1676
1676
1677
1679
1681
1704
1709
1787
1789
1790
1798
1801
1802
1810
1812
1812
1812
1818
BOT
TO
M
1665
C
AL
ICO
HIL
LS
BE
DD
ED
1666
1666
1670
1672
1673
PR
OW
PA
SS
NW
-PW
1676
1677
1678
1678
1679
1683
1710
1710
1788
1789
1790
1800
1803
1803
1811
M
W18
1718
1818
1518
20
FEA
TUR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
CO
NT
AC
T
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EC
OR
RU
GA
TE
D
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH
130
110
135
190 60 115
280
202
120
255
270
180 10 300 80 35 270
200
262
262
315
280
DIP
AN
GLE
11N
.VE
RT
39V
ER
TIC
AL
47 16N
.VE
RT
46ST
EE
PSH
AL
LO
W>6
4 79V
ER
TIC
AL
VE
RT
ICA
LV
ER
TIC
AL
VE
RT
ICA
L65
VE
RT
ICA
L
80 81V
ER
TIC
AL
69
STR
IKE
AZI
M
UTH 40 20 45 100
330 25 190
112 30 165
180 90 280
210
350
305
180
110
172
172
225
190
REM
AR
KS
MIN
ER
AL
IZE
D
OPE
N P
AR
TIN
G; D
EA
D L
IZA
RD
ON
TO
P O
F PR
OW
PA
SS
TE
RM
INA
TE
S A
T SE
-ST
RIK
ING
FR
AC
TU
RE
OPE
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OW
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D D
OW
NT
OE
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
HO
RIZ
ON
TA
L W
ASH
OU
TS
TE
XT
UR
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EC
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ES
SMO
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RO
PEN
DO
WN
TO
EO
PEN
DO
WN
TO
EPA
RTL
Y M
INE
RA
LIZ
ED
LOG
TV
TV TV
TV TV
TV
/L
TV
TV TV
TV
TV TV
TV TV
TV TV
TV
TV TV
TV TV
/LT
VT
VT
V TV
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L),
TELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
AT
UR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#2
-Con
tinue
d
Results
an Nye
Count ^ a
. a TJ 3 3 1 | 5* 3- 0 i w c s o 2 c s }? JS 1 m SP f S f i 5°
\ -
- --
7
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
^"S
ue
6'0
TOP
IS22
1823
1826
1834
1836
1840
1846
1848
1848
1848
1849
1851
1857
1866
1881
1958
1960
1995
2021
2022
2025
2032
2035
2110
2131
2132
2132
BOT
TO
M
1826
PR
OW
PA
SS
MW
1824
1830
1836
1839
PW-N
W18
4918
5118
4818
4918
5318
5418
6118
7018
8319
5919
61
1995
2022
2023
2027
2033
2037
BED
DED
2132
2132
2133
FEA
TURE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
WA
SHO
UT?
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
270
265
275
275
263
260
248
150 5
270
260
245
215
100
220
260
270
305
305
220
285
240
242
245
DIP
AN
GLE
77N
.VE
RT
78V
ERTI
CA
L72 75 74 18
VER
TIC
AL
74 75 77 77 >57 38 52
STEE
PN
.VE
RT
74 28V
ERTI
CA
L
28 32 36
STRI
KE
AZI
M
UTH
180
175
185
185
173
170
158 60 275
180
170
155
125 10 130
170
180
215
215
130
195
150
152
155
REM
ARK
S LO
G
TVM
INER
ALI
ZED
T
VTV TV T
V L TV TV TVM
INER
ALI
ZED
TV A
TA
TTV TV T
V TVH
OLE
OU
T O
F R
OU
ND
BU
T N
O
TVFR
AC
TUR
ES V
ISIB
LETV TV TV A
TTV TV
VIS
IBIL
ITY
IMPA
IRED
205
5-21
22 B
Y
LSK
EWED
HO
LETV
MIN
ERA
LIZE
D
TV TV
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, TE
LEV
ISIO
N (
TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
AT
UR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#2
-Co
ntin
ue
d
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
'"
"^i,
?3'
0
TOP
2134
2134
2138
2173
2194
2240
2252
2258
2262
2297
2298
2298
2299
2299
2300
2300
2300
2302
2304
2306
2314
2330
H
2335
00 m
2336
-
2338
2340
BO
T
TOM
2134
PR
OW
PA
SS
BE
DD
ED
2135
2139
B
UL
LFR
OG
N
W-P
W21
7421
99
MW
-DW
2256
2263
2267
2298
2298
2300
2300
2302
2303
2303
2301
2304
2305
2309
2315
2332
2339
2337
2340
2340
FEA
TUR
E
FRA
CT
UR
EFR
AC
TU
RE
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
E
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH
245
165
285
270
280
270
255
300
275
275
275
225
225
225
195
230
275
275
220
270
285
280
180
270
DIP
AN
GLE
36 45
VE
RT
ICA
LV
ER
TIC
AL
77 80 79N
.VE
RT
N.V
ER
T59 59 75 74 71
N.V
ER
T70
N.V
ER
T75
N.V
ER
TN
.VE
RT
77
N.V
ER
TV
ER
TIC
AL
N.V
ER
T
STR
IKE
AZI
- R
EMA
RK
S M
UTH
155
MIN
ER
AL
IZE
D75
M
INE
RA
LIZ
ED
OPE
N P
AR
TIN
G19
518
0 M
INE
RA
LIZ
ED
190
180
OPE
N16
521
0 M
INE
RA
LIZ
ED
185
185
185
135
135
135
105
140
185
185
130
OPE
N18
019
5 M
INE
RA
LIZ
ED
; IN
TE
RSE
CT
ING
FR
AC
TU
RE
S 23
35-2
342
190 90
MIN
ER
AL
IZE
D18
0
LOG
TV
TV TV
/LT
VT
V L TV TV AT
TV TV TV
TV TV TV
TV TV TV
TV AT
TV
TV
AT
TV
TV TV
8
Z
3D
TA
BL
E 1
1. S
UM
MA
RY
OF
IN
FO
RM
AT
ION
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT
), C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 --
Con
tinue
d
lesults
and
Interpretation of
Prel
lye
County, Nevada
3 1 > 1 H & 5* ? I £ c i * m
ro J? 0 £ m & 2 * i £ i
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
"^S
S
TOP
2340
23
4023
4123
4223
4423
45
2345
2346
2347
2348
2348
2348
2348
2350
23
5023
50
2351
2352
2352
2352
2353
2356
2356
2357
2357
2358
2358
23
5923
6123
6123
61
BOT
TO
M
2340
B
ULL
FRO
G
MW
-DW
23
4123
4223
4523
4523
46
2347
2348
2349
2349
2348
2350
2352
2350
23
5223
58
2355
2353
2352
2355
2356
2359
2358
2360
2361
2358
2361
23
6423
6123
6223
63
1 FE
ATU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
300
275
300 95 250
275
260
272
300
300
230
300
295
210
350
265
270
205
155
255
265
260
270
255
278
260
295
275
295
295
260
DIP
AN
GLE
N.V
ER
T
N.V
ER
TN
.VE
RT
77V
ERTI
CA
LV
ERTI
CA
L V
ERTI
CA
L51
STEE
PST
EEP
N.V
ER
TST
EEP 69
N.V
ER
T
N.V
ER
T84 77
N.V
ER
TV
ERTI
CA
L69 69 77 71 73 75
N.V
ER
T72
79
STEE
PST
EEP 74
STRI
KE
AZh
RE
MA
RKS
MUT
H
210
185
210 5
160
185
170
182
210
210
140
210
205
120
260
175
180
115
MIN
ERA
LIZE
D65 16
517
5 M
INER
ALI
ZED
170
MIN
ERA
LIZE
D18
0 M
INER
ALI
ZED
165
MIN
ERA
LIZE
D18
8 M
INER
ALI
ZED
170
205
PART
LY M
INER
ALI
ZED
18
5 PA
RTLY
MIN
ERA
LIZE
D20
520
517
0
LOG
TV
TV TV AT
TV TV
TV TV TV TV TV TV TV TV
TV AT
TV TV TV AT
AT/
TVA
T/TV
TV TV TV TV TV
TV TV TV AT
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L),
TELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 --
Con
tinue
d
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L °!£
GIC
FE
ATU
RE
09 m _t
TOP
2362
2363
2365
2366
2366
2367
2368
2372
2373
2376
2378
2378
2380
2381
2382
2382
2387
2388
2388
2389
2390
2390
2390
2391
23
9123
9123
92
BO
T
TOM
2365
B
UL
LFR
OG
M
W-D
W23
6623
6723
6623
6923
71
2368
2375
2376
2379
2378
2380
2383
2384
2387
2388
2390
2389
2390
2395
2391
2391
2393
2391
23
9423
9223
98
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
DIP
A
ZI
MU
TH
278
270
310
282
265
250
285
262
262
245
295
250
255
250
275 70 200
255
205
130
250
210
270
250 78 110
272
DIP
AN
GLE
71 74 61 45 74 79 34 74 75 71 34 62 72 66 77 80 74ST
EE
P 63 >81
STE
EP
STE
EP 71
STE
EP 67
VE
RT
ICA
L80
STR
IKE
AZI
M
UTH
188
180
220
192
175
160
195
172
172
155
205
160
165
160
185
340
110
165
115 40 160
120
180
160
348 20 182
REM
AR
KS
PAR
TLY
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
OPE
N
CA
VER
NO
US
INT
ER
SEC
TIO
N O
FFR
AC
TU
RE
S 23
82-2
390
OPE
NO
PEN
OPE
N
INT
ER
SEC
TS
S-ST
RIK
ING
FRA
CT
UR
EM
INE
RA
LIZ
ED
OPE
N
LOG
TV
TV AT
TV
AT
AT/
TVT
V TV
TV
AT
TV
TV
TV
TV TV
TV TV
TV
TV TV
TV
TV TV
TV
T
VT
VT
V
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT
), C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 -C
on
tinu
ed
ilts
and
Interpretation of
f
County, Nevada
w 1 3 nary
Aquifer 1 i«o 5" 09 O ? i c S % c K1 S | m £ c Z o i 3
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
""S
^6
TOP
2394
2395
2395
23
96
2396
23
9623
9623
9723
9823
9923
9923
9924
0224
0424
0824
0824
1024
1324
1624
1624
17
2417
2418
2420
2420
2422
24
24
2425
2426
2427
BOT
TO
M
2396
B
ULL
FRO
G
MW
-DW
2396
2396
23
97
2396
23
9723
9723
9924
0324
0424
0524
0124
0524
1224
0824
1624
1624
1324
1624
1724
18
2418
2419
2421
2422
2424
24
26
2426
2427
2428
' FE
ATU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
68 215
120
130
320
245
255
305
270
260
240
105
240
265 70 260 68 100
280
295
220
280
270
275
295
295
190
285
250
260
DIP
AN
GLE
64
STEE
PV
ERTI
CA
L V
ERTI
CA
L38
45
N.V
ER
TN
.VE
RT
79 80 80V
ERTI
CA
L71 83
VER
TIC
AL
82 81V
ERTI
CA
LN
.VE
RT
STEE
PST
EEP
STEE
PST
EEP 51 49 64
N
.VE
RT
ST
EEP
N.V
ER
TV
ERTI
CA
L
STRI
KE
AZI
M
UTH
338
125 30
40
23
0 15
516
521
518
017
015
0 15 150
175
340
170
338 10 190
205
130
190
180
165
205
205
100
195
160
170
REM
ARK
S
CA
VER
NO
US
WH
ERE
FRA
CTU
RES
INTE
RSE
CT
2394
-239
7
OPE
NO
PEN
OPE
N U
PTO
EO
PEN
OPE
N, W
ITH
CA
VIT
IES
LOG
TV TV TV
TV
TV
TV TV TV TV TV TV TV TV TV TV AT
TV TV TV TV TV
TV TV AT
AT
AT
TV
TV TV TV
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
AT
UR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#2
--C
ontin
ued
DE
PTH
BLW
C
ASI
NG
(FE
ET
) G
EOLO
GIC
UN
IT
L °i°
GIC
FE
ATU
RE
TABLE
^
TO
P
2429
2429
2430
2431
2432
2432
2432
2432
2432
2434
2434
2434
2435
2435
2436
2436
2437
2437
2439
2439
2439
2441
2441
2444
24
45
2446
2449
2449
BO
T
TOM
2432
B
UL
LFR
OG
M
W-D
W24
3224
3124
3224
3224
3324
3324
3524
3424
3524
3524
3524
3724
3724
3824
3824
3724
41
2440
2440
2442
2444
2443
2445
24
48
2448
2459
2451
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
DIP
A
ZI
MU
TH
300
270
280
315
285
282
160
280
250 60 245
255
285
280
240
280
205
275 60 220
278
240
245
110
285
265
300
310
DIP
AN
GL
E
STE
EP 72 24
STE
EP 41 62
N.V
ER
T
N.V
ER
T
N.V
ER
T
SHA
LL
OW
VE
RT
ICA
L
64 66
N.V
ER
T
53
N.V
ER
T
N.V
ER
T
>75 71
N.V
ER
T
70 72 55 52
72
60 85N
.VE
RT
STR
IKE
A
Zh
RE
MA
RK
S M
UTH
210
180
190
225
195
192 70 190
160
MIN
ER
AL
IZE
D
330
MIN
ER
AL
IZE
D
155
MIN
ER
AL
IZE
D
165
195
190
160
190
115
1 85
RO
CK
BR
OK
EN
UP
WH
ER
E F
RA
C
TU
RE
S IN
TE
RS
EC
T 2
437-
2444
330
OPE
N
130
188
OPE
N
150
OPE
N
155
OPE
N
20
195
175
210
OPE
N
220
LOG
TV
AT
TV
TV
TV
TV
TV
TV
TV
TV
TV
AT
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
/AT
TV
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
AT
UR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#2
-Co
ntin
ue
d
Results
and
Interpretation of
Prel
Nye
County, Nevada
3 i 1 j 3 0 i 1 m » * s 3 I c i * -< flM i Mountai
n,
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
""i^
TOP
2451
24
5224
53
2454
2456
2460
2410
2413
2413
2415
241%
24S9
2492
2492
24
9524
99
2500
2506
2510
2530
2532
2539
2539
2548
25
55
2556
2558
2561
2561
BOT
TO
M
2452
B
ULL
FRO
G
MW
-DW
2453
2462
24
5524
57
BU
LLFR
OG
PW
-NW
2473
2477
2479
2476
2483
2489
2492
2492
24
9925
00
2500
2506
2517
2534
2533
2544
2548
2551
25
56
2560
2559
2562
2561
' FE
ATU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
CO
NTA
CT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
255
265
285
260
260
270
268
320
110
300
240
195
160
250
270
260
300
258
UN
K25
528
028
0 92
270
268
245
145
135
DIP
AN
GLE
VER
TIC
AL
VER
TIC
AL
84
VER
TIC
AL
VER
TIC
AL
>74 78 81 24 80
VER
TIC
AL
VER
TIC
AL
N.V
ER
T>7
5V
ERTI
CA
L V
ERTI
CA
LV
ERTI
CA
L82
VER
TIC
AL
VER
TIC
AL
>80
>84 68
VER
TIC
AL
75V
ERTI
CA
L46 17
STR
IKE
A
ZI-
RE
MA
RK
S M
UTH
165
175
195
170
170
180
MIN
ERA
LIZE
D17
8 O
PEN
230
OPE
N20 210
150
105 70
16
018
0 M
INER
ALI
ZED
17
0 M
INER
ALI
ZED
210
MIN
ERA
LIZE
D16
8 M
INER
ALI
ZED
UN
K16
519
019
0 2 18
0 M
INER
ALI
ZED
17
8 M
INER
ALI
ZED
155
MIN
ERA
LIZE
D55
M
INER
ALI
ZED
45
MIN
ERA
LIZE
D
LOG
TV
TV AT
TV TV L TV TV TV TV AT
TV TV TV
TV TV
TV TV TV TV TV TV TV TV
TV
TV TV TV TV
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
AT
UR
E
(TE
MP
) LO
GS
FO
R B
OR
EH
OLE
UE
-25C
#2
-Con
tinue
d
DEP
TH B
LW
CA
SIN
G
(FE
ET
) G
EOLO
GIC
UN
IT
LITI
Jfti
£G
IC
TOP
2561
2662
2663
2664
2675
2686
2691
2704
2706
2707
2708
2708
2709
2709
2710
2710
2710
2712
2712
2713
2714
2717
2717
2717
2718
2718
BO
T
TOM
2562
B
UL
LFR
OG
PW
-NW
2663
2663
2665
BU
LL
FRO
G
BE
DD
ED
2691
2694
2705
2706
2708
2709
2708
2712
2719
2710
2710
2713
2713
2713
2719
2715
2717
2718
2723
2718
2719
FEA
TUR
E
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
CO
NT
AC
TFR
AC
TU
RE
FAU
LTFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH
335 8 5
275
245
280
255
115
325
265
265
265 60 335
210
260
215
325
260
150 25 205
250
210 0
DIP
AN
GLE
46 36 32 43 >81
75-9
0 32ST
EE
PV
ER
TIC
AL
STE
EP
VE
RT
ICA
L70 84
STE
EP
STE
EP 70
STE
EP
STE
EP 78
N.V
ER
TV
ER
TIC
AL
N.V
ER
T77
STE
EP
VE
RT
ICA
L
STR
IKE
AZI
M
UTH
245
278
275
185
155
190
165 25 235
175
175
175
330
245
120
170
125
235
170 60 295
115
160
120
270
REM
AR
KS
CA
VIT
Y F
OR
ME
D B
Y I
NT
ER
SEC
T
ING
FR
AC
TU
RE
S 25
61-2
562
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
DPA
RTL
Y M
INE
RA
LIZ
ED
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
MIN
ER
AL
IZE
D
OPE
N;
HO
LE
EN
LA
RG
ED
BY
FR
AC
TU
RE
S 27
09-2
724
OPE
N
OPE
N
OPE
NO
PEN
OPE
NO
PEN
OPE
N
LOG
TV
TV
TV
TV
L TV
TV
/LT
VT
VT
VT
VT
VT
V/C
TV
TV
TV
TV
TV
TV
TV
/CT
VT
VT
VT
VT
VT
V
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 -C
on
tinu
ed
Results
an< Ny
e Coun
t) ft il S i" 2. o 3 3 S > 1 ^ ito 5" o3 1 1 C io * C m S S o I m 1 8 "< i f-
3 I
> -
- -
/
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L °^°
FEA
TURE
TOP
2718
2718
2719
2720
2722
2722
2728
2729
2730
2731
2732
2732
2733
2733
2734
2734
2734
2736
2737
2739
2739
2749
2751
2752
2752
2754
2755
2757
2757
2757
BOT
TOM
2720
B
ULL
FRO
G27
19
TRA
M27
2427
2527
2627
2927
2927
3227
3227
3227
3327
3327
3427
3527
3527
3927
3827
4127
4027
4427
5127
5427
5227
5427
5527
5927
5727
5827
61
BED
DED
FR
AC
TUR
EFR
AC
TUR
E
UPP
ER
(NW
-PW
) C
ON
TAC
TFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
E
DIP
A
ZI
MUT
H
330
215
272
250
285
285
105
282
100 0
110
105 95 240
250
245 90 278
280
245 90 92 275
265
115 90 255
265
115
DIP
AN
GLE
VER
TIC
AL
STEE
P 72 70 74 47N
.VE
RT
64V
ERTI
CA
LV
ERTI
CA
LSH
ALL
OW
SHA
LLO
WSH
ALL
OW
58 62 79 X34 77
N.V
ER
T79 62 72
N.V
ER
T66
N.V
ER
T>7
8V
ERTI
CA
LV
ERTI
CA
L76
STR
IKE
AZI
- R
EM
AR
KS
MU
TH
240
OPE
N12
5
182
OPE
N16
0 O
PEN
195
195 15 192 10 270 20 15
M
INER
ALI
ZED
515
016
015
5 018
819
015
5 0 2 O
PEN
185
175
OPE
N25 0
OPE
N16
517
5 25
LOG
TV TV L TV TV/C
TV/C
AT
TV TV TV TV TV TV TV TV TV TV TV TV TV AT
TV TV TV TV TV TV TV TV AT
TA
BL
E 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 -C
ontin
ued
DE
PTH
BLW
C
ASI
NG
(FE
ET
) G
EO
LO
GIC
UN
IT
^"nw
c0
'0
FEA
TUR
E
TO
P
2758
2758
2759
2765
2765
2767
2771
2773
2774
2775
2776
2777
2780
2780
2781
2781
2782
2783
2784
2785
2786
2786
H
2788
5
2789
2
2789
2790
2790
BO
T
TOM
2760
TR
AM
2759
2759
2766
2766
2768
2772
2774
2774
2778
2779
2780
2780
2783
2784
2782
2784
2787
2787
2789
2788
2790
2789
27
9027
9027
90
UPP
ER (N
W-P
W)
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
TUFF
BR
EC
CIA
C
ON
TAC
TFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
EFR
AC
TUR
E
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
250
255
250
280 90 90 270
270
300
270
295
170
170
255
262 80 260
280
255
268 75 270 0
270
270
290
DIP
AN
GLE
VER
TIC
AL
VER
TIC
AL
N.V
ER
T58 43
N.V
ER
TN
.VE
RT
N.V
ER
TN
.VE
RT
59 69SH
ALL
OW
SHA
LLO
W63 73
VER
TIC
AL
64 72 60 73 61 49SH
ALL
OW
SH
ALL
OW
SHA
LLO
W19
STR
IKE
A
ZI
MU
TH
160
165
160
190 0 0
180
180
210
180
205 80 80 165
172 0
180
190
165
178
345
180
270
180
180
200
REM
AR
KS
MIN
ER
AL
IZE
D
RO
CK
VIS
IBL
Y B
RE
CC
IAT
ED
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
INT
ER
SEC
TS
N-S
TR
IKIN
G
FRA
CT
UR
E A
T 2
782
PAR
TL
Y M
INE
RA
LIZ
ED
PAR
TL
Y M
INE
RA
LIZ
ED
PAR
TL
Y M
INE
RA
LIZ
ED
MIN
ER
AL
IZE
D
LOG
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
/L
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
AT
TV
TV
TV
TV
TV
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
OLO
GIC
(L)
, T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 -C
on
tinu
ed
Results
and
Interpretation of
1
Nye
County, Nevada
i I J .0 i H 3 * 1 1 C 1 s J? 3 n £ C & S 1< 1 3E o | *
\
/
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
LI
T t
£G
IC
FEA
TUR
E
TO
P
2791
2793
2793
2794
27
95
2795
2796
2796
2796
2799
2799
2800
2800
28
0028
02
2802
2802
2802
2804
2804
2805
2805
2806
2806
2807
2807
28
0728
0828
0928
10
BO
T
TOM
2792
T
RA
M27
94
2794
2795
27
96
2797
2797
2799
2797
2799
2800
2800
2800
28
0028
02
2802
2802
2803
2804
2804
2805
2806
2807
2807
2807
2808
28
0828
1028
1028
12
TU
FF B
RE
CC
IA
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH
300
278
275
268 25
20 280
286
315
335
225
250
160
355
155
270
250
270 90 215
260
340
240
260
300
220
270
250
150
145
DIP
AN
GLE
SHA
LL
OW
56 49 54
STE
EP 66 56 72
STE
EP
STE
EP
N.V
ER
TST
EE
PST
EE
P ST
EE
PST
EE
P ST
EE
PN
.VE
RT
N.V
ER
TST
EE
PN
.VE
RT
N.V
ER
TN
.VE
RT
N.V
ER
TN
.VE
RT
STE
EP
N.V
ER
T
N.V
ER
TN
.VE
RT
N.V
ER
TV
ER
TIC
AL
STR
IKE
AZI
M
UTH
210
188
185
178
295
290
190
196
225
245
135
160 70
265 65
18
016
018
0 012
517
025
015
017
021
013
0 18
016
0 60 55
REM
AR
KS
OPE
N; P
AIN
TB
RU
SH C
AN
YO
NFA
ULT
ZO
NE
279
3-27
95
OPE
N
PAR
TLY
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
DM
INE
RA
LIZ
ED
M
INE
RA
LIZ
ED
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
LOG
TV
TV
/L
TV
TV
T
V
TV
AT
AT
TV
TV
TV
TV
TV
T
VT
V
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
T
VT
VT
VT
V
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
5C #
2 -C
ontin
ued
DEP
TH B
LW
CASI
NG
(F
EET)
G
EOLO
GIC
UNI
T L
mJn
McG
'C
FEA
TURE
TOP
2810
2811
2812
2813
2814
2815
2815
2816
2818
2821
2822
2822
2822
2822
2824
2824
2824
2824
2824
2824
2825
2825
2826
2826
£
2826
P
28
28
2833
2833
2834
BOT
TO
M
2811
TR
AM
2812
2813
2814
2816
2816
2816
2816
2818
2822
2822
2822
2823
2823
2824
2824
2824
2825
2825
2825
2826
2826
2826
2826
2827
28
29
2833
2834
2835
TUFF
BR
ECC
IA
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
25 295 70 270
265 60 270
255
295
270
270
270
305
350
280
345 85 270
345
350
340
175
135
300
340
310 90 35 100
DIP
AN
GLE
STEE
PSH
ALL
OW
49V
ERTI
CA
LST
EEP
STEE
PST
EEP
N.V
ER
TSH
ALL
OW
N.V
ER
TN
.VE
RT
N.V
ER
TN
.VE
RT
N.V
ER
TN
.VE
RT
42N
.VE
RT
N.V
ER
TSH
ALL
OW
49SH
ALL
OW
SHA
LLO
WST
EEP
N.V
ER
TST
EEP 64
V
ERTI
CA
LN
.VE
RT
N.V
ER
T
STRI
KE
AZI
M
UTH
295
205
340
180
175
330
180
165
205
180
180
180
215
260
190
255
355
180
255
260
250 85 45 210
250
220 0
305 10
REM
ARK
S
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
D
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
D
MIN
ERA
LIZE
DM
INER
ALI
ZED
LOG
TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV
TV
TV T
V TV
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T), C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
E-2
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2 -C
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Results
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DEP
TH B
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CASI
NG
(F
EET)
G
EOLO
GIC
UN
IT
"""^
ftl^
310
FEA
TURE
T P
2840
2840
2841
2842
2843
2844
2845
2861
2868
2873
2874
2874
2875
2876
2877
2880
2881
2881
2882
2882
2882
2883
2883
2884
2884
2884
2884
2885
2886
2888
2888
BOT
TOM
2842
TR
AM
2841
2842
2842
2843
2844
2847
2862
2869
2875
2875
2876
2876
2876
2878
2880
2882
2882
2883
2883
2883
2883
2884
2884
2884
2884
2885
2885
2887
2889
2888
TUFF
BR
ECC
IA
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
80 325
335
120 90 80 0
235
120
275
292
290
285
285
355
345
310
270
355
275
340
300 70 300 70 155
125
225
255
326
115
DIP
AN
GLE
VER
TIC
AL
N.V
ER
TV
ERTI
CA
LSH
ALL
OW
VER
TIC
AL
VER
TIC
AL
65ST
EEP
N.V
ER
T61
-65 54 60 30 25
N.V
ER
TN
.VE
RT
N.V
ER
TN
.VE
RT
N.V
ER
TN
.VE
RT
N.V
ER
T34 54
SHA
LLO
WST
EEP 34
STEE
PSH
ALL
OW
N.V
ER
T59 30
STR
IKE
AZI
- RE
MA
RKS
MUT
H
350
235
245 30 0
350
270
MIN
ERA
LIZE
D14
5 30
MIN
ERA
LIZE
D18
520
220
019
519
526
525
522
018
026
518
525
021
034
021
034
0 65 35 135
165
236 25
LOG
TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV AT
TV
TA
BL
E 1
1.
SU
MM
AR
Y O
F I
NF
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MA
TIO
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RO
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ITH
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V),
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ST
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ELE
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ALI
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C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
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5C #
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ed
DE
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ASI
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TUR
E
TO
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2889
2890
2892
2893
2893
2893
2896
2897
2897
2897
2897
2898
2899
2900
2901
2901
2902
2902
2904
2904
2904
2905
2906
2906
£
2907
?
2907
*
2907
2907
2907
BO
T
TOM
2890
T
RA
M28
9128
9428
9328
9328
9428
9828
9728
9828
9728
9828
9929
0029
0029
0229
0229
0329
0329
0429
0429
0529
0529
0629
0829
07
2908
29
0829
0829
08
TU
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IA
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CT
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TU
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CT
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UR
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TU
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FRA
CT
UR
E
FRA
CT
UR
E
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
DIP
A
ZI
MU
TH 90 295
265
250
250
280
282
110
270
115
300
295
295
295
155
280
270
125 90 125 60 180
270
270
340
275
300
315
275
DIP
AN
GLE
30 35 69ST
EE
PST
EE
P 58 71 43N
.VE
RT
19 30 35 30 30 46 39SH
AL
LO
W35 35
SHA
LL
OW
N.V
ER
TST
EE
PSH
AL
LO
W58
SHA
LL
OW
35
SH
AL
LO
W54
STE
EP
STR
IKE
AZI
M
UTH 0
205
175
160
160
190
192 20 180 25 210
205
205
205 65 190
180 35 0 35 330 90 180
180
250
185
210
225
185
REM
AR
KS
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
OP
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MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
MIN
ER
AL
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D
MIN
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AL
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D
MIN
ER
AL
IZE
D
MIN
ER
AL
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D
MIN
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IZE
D
OP
EN
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
MIN
ER
AL
IZE
D
OPE
N
LOG
TV
TV
TV
TV
TV
TV
AT
/TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TV
TA
BL
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1.
SU
MM
AR
Y O
F I
NF
OR
MA
TIO
N F
RO
M L
ITH
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GIC
(L)
, T
ELE
VIS
ION
(T
V),
AC
OU
ST
IC T
ELE
VIE
WE
R (
AT)
, C
ALI
PE
R (
C),
AN
D T
EM
PE
RA
TU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
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ed
Results
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ty IfI a I 3 s 2 1 1 3 ft (0 0 1 » C m S o C s $ £ 1 C m JS * "K I | £
DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
LI
TIJ°
McG
IC
FEA
TUR
E
TOP
2908
2908
2909
2909
2910
2910
2910
2910
2910
2910
2910
2910
2911
2912
2912
2912
2913
2914
2914
2914
2914
2915
2916
2918
2919
2920
2921
2922
2922
2923
BOT
TOM
2908
T
RA
M29
0929
0929
0929
1029
1029
1029
1029
1129
1129
1129
11
2911
2913
2913
2914
2914
2914
2915
2914
2915
2916
2917
2919
2920
2920
2921
2922
2923
2923
TUFF
BR
ECC
IA
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FAU
LT
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MU
TH
322
300
300 60 315
355
300 30 345
285
205 90 300 30 45 5 0
255 70 200
100
195 50 10 2 2
105
165
295
355
DIP
AN
GLE
46 30 25SH
ALL
OW
N.V
ERT
N.V
ERT
SHA
LLO
WST
EEP
STEE
P 54ST
EEP
VER
TIC
AL
SHA
LLO
WN
.VER
TST
EEP 52 55
SHA
LLO
WSH
ALL
OW
SHA
LLO
WSH
ALL
OW
SHA
LLO
W55 57 25 25 25 25
SHA
LLO
W19
STRI
KE
AZI
MUT
H
232
210
210
330
225
265
210
300
255
195
115 0
210
300
315
275
270
165
340
110 10 105
320
280
272
272 15 75 205
265
REM
ARK
S
MIN
ERA
LIZE
D
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
DM
INER
ALI
ZED
OFF
SETS
SW
-STR
IKIN
G F
RA
CTU
RE
AT
2911
OFF
SET
BY
FA
ULT
MIN
ERA
LIZE
D
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
DM
INER
ALI
ZED
MIN
ERA
LIZE
D
LOG
TV TV TV TV TV TV TV TV TV AT
TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV
TAB
LE 1
1. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
ER
(A
T),
CA
LIP
ER
(C
), A
ND
TE
MP
ER
ATU
RE
(T
EM
P)
LOG
S F
OR
BO
RE
HO
LE U
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5C #
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DEP
TH B
LW
CA
SIN
G
(FEE
T)
GEO
LOG
IC U
NIT
L
ml^
GIC
FE
ATU
RE
TOP
2923
2923
2924
2925
2925
2926
2926
2927
2927
2933
2933
2935
2936
2937
2939
2943
2945
2946
2960
2986
BO
T
TOM
2925
T
RA
M29
24
2925
2926
2926
2926
2927
2928
2929
2933
2934
2937
2938
2942
2943
2946
2946
2961
TU
FF B
RE
CC
IA
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
E
LO
WE
R (
PW)
CO
NT
AC
TFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
FRA
CT
UR
EFR
AC
TU
RE
BO
TT
OM
DIP
A
ZI
MU
TH 85 300 25 165 55 355
355
348 65 355
340
325
165
160
300
340
260
265
DIP
AN
GLE
59 25 52 >43
STE
EP 43 43 43 69 30 30 35
N.V
ER
T>7
6SH
AL
LO
WV
ER
TIC
AL
25 25
STR
IKE
AZI
M
UTH
355
210
295 75 325
265
265
258
235
265
250
235 75 70 210
255
170
175
REM
AR
KS
LOG
TV TV
TV TV
TV
TV
TV
TV
OPE
N
TV
TV TV
L TV
TV
TV
MIN
ER
AL
IZE
D
TV TV
TV
OPE
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TV
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MM
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F I
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RO
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(L)
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LEV
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N (
TV),
AC
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ELE
VIE
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R (
AT
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ALI
PE
R (
C),
AN
D T
EM
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RA
TU
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Results
and
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NW
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DE
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C
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GE
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IC U
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1316
13
20
1370
13
8213
8914
1314
1614
3314
4414
4414
4514
4614
8314
9114
9214
9314
9314
9514
9614
9914
9915
0515
1215
1315
1415
1615
1815
2015
2115
34
BOT
TO
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LIC
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ILLS
13
68
1372
13
8314
0614
1414
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3514
4514
4514
4914
5014
9014
9314
9814
9514
9814
9915
0415
0115
0215
1015
1315
1415
1415
1915
2015
2115
2215
41
LITH
OLO
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FE
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ZO
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FE
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RE
NW
W
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AB
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CO
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RET
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CTU
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CTU
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FRA
CTU
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FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
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FRA
CTU
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FRA
CTU
RE
FRA
CTU
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FRA
CTU
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LED
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FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
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FRA
CTU
RE
FRA
CTU
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DIP
A
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LEST
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MUT
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MA
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LOG
DEA
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SEC
T O
N W
ATE
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UR
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SP
ALL
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LE
TV/C
A
BR
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SPIR
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D W
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TV/A
T H
OR
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NTA
L W
ASH
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TV
93 82 68 310 65 58 90 90 232 88 268
263 75 275
263 98 315
325
110
100 95
UN
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N.V
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54 >48
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3>7
4>7
9 51 77 50 75 70 >79
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SHA
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W>6
8N
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RT
N.V
ER
TN
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RT
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3
352
338
220
335
328 0 0
142
358
178
173
345
185
173 8
225
235 20 10 5
UN
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SPIR
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SU
MM
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1552
1560
1569
1581
1581
1582
1582
1585
1615
1616
1616
1616
1616
1617
1619
1620
1622
1622
1623
1624
1624
1624
1624
1624
BO
T
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C
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1543
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1569
1582
1582
1582
1584
1586
1618
1617
1616
1617
1617
1617
1620
1620
1623
1625
1624
1625
1625
1624
1625
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DIP
A
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200
200
200
200
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115
170
210
115
292
230
230
230
235
105 95 260
145 2 95 140
280
245
255
DIP
AN
GLE
>81 23 23 23 23 23
SHA
LL
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64 24 71 41 33 23 23 24 29 38N
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RT
>69 37
N.V
ER
TN
.VE
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N.V
ER
TST
EE
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7
STR
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AZI
M
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165
110
110
110
110
110 25 80 120 25 202
140
140
140
145 15 5
170 55 272 5 50 190
155
165
REM
AR
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LOG
TV
TV
TV L TV
TV
TV
TV
TV
TV
CA
VE
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OU
S IN
TE
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CT
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TV
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VT
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TV
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TV
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-
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TOP
1625
1626
1628
1628
1629
1629
1631
1633
1633
1634
1635
1638
1639
1640
1651
1657
1666
1668
1672
1750
1751
1751
1752
1753
1760
1761
1771
1776
1778
BOT
TO
M
1627
C
ALI
CO
HIL
LS
BED
DED
1627
1629
1628
1630
1631
PR
OW
PA
SS
NW
-PW
1631
1633
1634
1635
1636
1638
1639
1640
1652
1658
1669
1669
1674
1751
1752
1752
1752
1755
1760
1761
1773
1776
1782
FRA
CTU
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FRA
CTU
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FRA
CTU
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FRA
CTU
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FRA
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CO
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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FRA
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TUR
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AC
TUR
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FRA
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FRA
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FRA
CTU
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FRA
CTU
RE
FRA
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DIP
A
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MUT
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245 75 265
235
105 75 170
335
155
325
350 25 130 95 60 300
190
265
326
335 91 150
205
323 60 100
268
305
DIP
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SHA
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SHA
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76
STRI
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155
345
175
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260
295 40 5
330
210
100
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236
245 1 60 115
233
330 10 178
215
REM
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MIN
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DM
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DM
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DM
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D
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TV XT/
TVA
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TV TV TV TV TV TV TV
TV TV AT
TV TV TV TV TV TV TV TV TV TV TV XT/
TVT
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T
TAB
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2.
SU
MM
AR
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FOR
MA
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RO
M L
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OLO
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S F
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BO
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DE
PTH
BLW
C
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(FE
ET
) G
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LO
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L °
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1779
1780
1795
1796
1804
1805
1806
1813
1814
1814
1815
1820
1825
1825
1829
1830
1830
1831
1835
1835
1837
1846
1849
1855
1863
1938
2085
BO
T
TOM
1779
PR
OW
PA
SS
NW
-PW
MW
1797
1796
1806
1806
1807
1814
1815
1815
1817
1823
1825
1826
1830
PW-N
W18
3118
3318
3518
3518
3918
4718
5218
6018
6519
38B
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FEA
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FRA
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CO
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FRA
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TAC
T
DIP
AZ
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325
260
130
300
180 55 310
270
200
285
250
140
145 50 262
245
135
285 20 160
268
270
245
355
DIP
AN
GLE
N.V
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T
68N
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72N
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>58
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T66 73 19 19 35
N.V
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TN
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SHA
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75 >80
N.V
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T30
STRI
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REM
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S M
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235
170
MIN
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LIZE
D40 21
0 90 325
220
MIN
ERA
LIZE
D18
0 M
INER
ALI
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110
MIN
ERA
LIZE
D19
5 M
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ALI
ZED
160 50 55
MIN
ERA
LIZE
D32
0
172
155 45 195
MIN
ERA
LIZE
D29
0 70 178
180
155
265
MIN
ERA
LIZE
D
LOG
TV L TV TV AT
TV TV TV TV TV AT/
TVA
TTV TV TV L TV TV TV TV TV TV TV TV TV TV L
TA
BL
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2.
SU
MM
AR
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S F
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(FE
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IC
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2112
2116
2116
2117
2117
2117
2118
2119
2119
2120
2120
2121
2122
2123
2124
2125
2126
2128
2128
2128
2129
2129
2130
2130
2143
2174
2210
2258
2263
2267
2286
BO
TTO
M
BU
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N
W-P
W21
1721
1721
1721
1721
1821
1821
1921
1921
2021
2121
2121
2321
2421
2521
2521
2621
2921
2921
2921
3021
3021
3121
3221
4721
77B
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FRO
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2268
2269
2271
2292
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CO
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CO
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DIP
A
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MUT
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350
350
350
350
350
350
350
350
350
350
350
345
345
345
345
345
275
110
345
290
285
275
285
245
270
280
275
285
260
DIP
AN
GLE
23 23 18 24 24 38 29 24 24 29 24 18 29 38 24 29 29 48 38N
.VE
RT
N.V
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TN
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RT
64 >77 75 85 82 76 81
STRI
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AZI
M
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260
260
260
260
260
260
260
260
260
260
260
255
255
255
255
255
185 20 255
200
195
185
195
155
180
190
185
195
170
REM
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S
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DM
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DM
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MIN
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DM
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LOG
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BL
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2294
2298
2333
2337
2340
2343
2347
2349
2352
2353
2354
2356
2368
2368
2372
2374
2374
2374
2379
2379
2379
2380
2382
2421
2422
24
24
2430
24
3024
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T
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2302
B
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2308
2333
2342
2342
2344
2348
2353
2353
2356
2354
2357
2369
2372
2373
2375
2374
2379
2379
2379
2380
2381
2385
2426
2428
2431
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FRO
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2440
2451
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CO
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FRA
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FRA
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UR
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DIP
A
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MU
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255
175
315
255
295
285
280
270
285
295
295
180
235
260
255
295
220
245
245
250
200
210
195
275
270
275
275
260
DIP
AN
GL
E
83 85
SHA
LL
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83 58 56 54 78
N.V
ER
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N.V
ER
T
80
N.V
ER
T
N.V
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N.V
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T
80
VE
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L
SHA
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N.V
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T
N.V
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>77 81 82
83 83 83
STR
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AZI
M
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165 85 225
165
205
195
190
180
195
205
205 90 145
170
165
205
130
155
155
160
110
120
105
185
180
185
185
170
RE
MA
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MIN
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AL
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D
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AL
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MIN
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AL
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AL
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AL
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D
MIN
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AL
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D
MIN
ER
AL
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D
MIN
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AL
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D
OPE
N
MIN
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AL
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D
OPE
N
OPE
N
OPE
N
OPE
N
OPE
N
LOG
AT
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TV
TV
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TV
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TV
TV
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TV
TV
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2444
2445
2446
2447
2450
2454
2470
2476
2480
2503
2511
2520
2521
2556
2563
2611
2619
BOT
TO
M
2448
B
ULL
FRO
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PW-N
W24
6224
6424
6524
5224
5624
7524
7824
8025
0425
2525
2125
2725
5725
6326
1226
20
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RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
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FRA
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FRA
CTU
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FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
H
255
255
268
262 85 280
260
270
200
285
275
285
265
115
270
265 85
DIP
AN
GLE
72 87 87 87 >62
N.V
ER
T80 >67
SHA
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WV
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CA
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TIC
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.VE
RT
N.V
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T49
STRI
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165
165
178
172
355
190
170
180
110
195
185
195
175 25 180
175
355
REM
ARK
S
OPE
NO
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MIN
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D
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2650
2670
2685
2690
2690
2692
2692
2693
2694
2695
2696
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BED
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2686
2691
2691
2692
2693
2693
2697
2696
2696
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FRA
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FRA
CTU
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FRA
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125 54 50 50 50 50 155 10 265
49 38 42 34 29 34 69N
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35 324
320
320
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TV
TV
TV
TV
TV
TV
TV
TAB
LE 1
2. S
UM
MA
RY
OF
INFO
RM
ATI
ON
FR
OM
LIT
HO
LOG
IC (
L), T
ELE
VIS
ION
(TV
), A
CO
US
TIC
TE
LEV
IEW
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(A
T),
CA
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(T
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LOG
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TE
LEV
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16
Results
am Nye
Coun
t d
Interpre
f, Nevada
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(TEM
P) L
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FE
ATU
RE
TOP
2763
2763
2764
2764
2765
2766
2770
2771
2772
2773
2774
2776
2777
2777
2777
2777
2782
2783
2785
2787
2790
2791
2793
2793
2796
2798
2801
2803
2803
2803
BOT
TO
M
2763
TR
AM
2765
2765
2765
2767
2767
2772
2773
2773
2774
2774
2777
2778
2778
2778
2778
2783
2784
2788
2788
2792
2793
2794
2795
2798
2799
2801
2804
2804
2804
UPP
ER (N
W-P
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FRA
CTU
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FRA
CTU
RE
FRA
CTU
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CTU
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FRA
CTU
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CTU
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CTU
RE
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CTU
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FRA
CTU
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FRA
CTU
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FRA
CTU
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FRA
CTU
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FRA
CTU
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DIP
A
ZI
MUT
H
315 95 90 270
170 90 85 90 92 90 290 95 90 95 280
305 85 92 110 85 280 82 85 270 80 330
195
345
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19 64 60N
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N.V
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SHA
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STRI
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225 5 0
180 80 0
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200 5 0 5
190
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355 2 20 355
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MIN
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LIZE
D10
525
5 B
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ALL
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ATT
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2803
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425
5 2
LOG
TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV TV
TV
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BL
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2.
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MM
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Y O
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TUR
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TO
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2803
28
04
2804
2805
2807
2811
2814
2814
2814
2819
2820
2824
2824
2824
2825
2825
2825
2827
2830
2830
2830
2831
2831
2839
2843
BOT
TO
M
2804
T
RA
M
2804
2805
2806
2808
2811
2814
2814
2816
2820
2821
2825
2825
2825
2825
2825
2826
2828
2830
2831
2832
T
RA
M28
3228
38
2841
2843
UPP
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DIP
A
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MU
TH 90
270 W
230 90 170
265 90 80 75 305
285 75 70 335 60 307
270 50 240
300 65 285
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DIP
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N
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51
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55 58 43ST
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STR
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140 0 80 175 0
350
345
215
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340
245
330
217
180
320
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210
335
195
215
345
REM
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TV
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AT
UR
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(TE
MP
) LO
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FO
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#3
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Results
am Nye
Coun
ty -* *
*
fi l! ff § a TJ 3 3 i .0 i 3 1 £ i o g C E * C m
10 {? J5 a> I C rn SP S .< i s o 3 S 3
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IC U
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FE
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2849
2849
2849
2850
2865
2869
2871
2872
2880
2881
2881
2881
2884
2884
2886
2886
2886
2886
2887
2887
2888
2888
2888
2892
2892
2895
2895
2896
2898
2899
BOT
TOM
2849
TR
AM
2850
2850
2851
2868
2870
2872
2877
2881
2881
2883
2882
2885
2885
2886
2887
2887
2887
2888
2888
2889
2889
2889
2893
2893
2896
2896
2897
2899
2900
TUFF
BR
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IA
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
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FRA
CTU
RE
FRA
CTU
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CTU
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FRA
CTU
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FRA
CTU
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CTU
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FRA
CTU
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CTU
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FRA
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CTU
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CTU
RE
FRA
CTU
RE
FRA
CTU
RE
FRA
CTU
RE
DIP
A
ZI
MUT
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210 10 95 35 265
265 78 270
122 68 120 55 65 47 60 55 75 65 70 65 45 45 45 45 45 40 40 40 65 60
DIP
AN
GLE
SHA
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STEE
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N.V
ER
TN
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RT
49 >79 56 35 63 49 49 49 42 49 58 45 51 55 51 38 38 54 54 49 58 53 51 52
STRI
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M
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120
280 5
305
175
175
348
180 32 338 30 325
335
317
330
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533
534
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531
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531
531
531
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TAB
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MA
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ON
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FEA
TUR
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2899
2900
2900
2902
2903
2904
2904
2906
2906
2907
2907
2908
2908
2908
2909
2910
2923
2926
2932
2937
2940
2944
2950
2954
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BO
T
TOM
2900
T
RA
M29
0129
0129
0429
0329
0529
0529
0729
0729
0829
0729
0829
0829
0929
0929
1029
2429
2829
3329
4029
4229
4529
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TU
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CC
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FRA
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TU
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TU
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TU
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CT
UR
EFR
AC
TU
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UR
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TU
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TU
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TU
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CA
BL
EB
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TO
M
DIP
A
ZI
MU
TH 65 85 95 80 5 80 45 0 90 70 65 40 175 40 40 155
112 5
260 85 95 90
DIP
AN
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STE
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52 46 52SH
AL
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W52 56 25 30 42 30 30
SHA
LL
OW
35 43 43 46 67V
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TIC
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STR
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355 5
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