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TRANSCRIPT
Gravity Survey and Depth to Bedrock In Carson Valley, Nevada-California
By Douglas K. Maurer
U.S. GEOLOGICAL SURVEY
Water-Resources Investigations Report 84-4202
Prepared in cooperation with the
DOUGLAS COUNTY PLANNING COMMISSION
Caraoa City, Nevada
~ 1986
UNITED STATES DEPARTMENT OF THE INTERIOR
WILLIAM P. CLARK, Secretary
GEOLOGICAL SURVEY
Dallas L. Peck, Director
For additional information Copies of this report may be write to: purchased from:
U.S. Geological Survey Open-File Sendees SectionRoom 227, Federal Building U.S. Geological Survey705 North Plaza Street Box 25425, Federal CenterCarson City,NV 89701 Denver, CO 80225
Call (303) 236-7476 for ordering information
CONTENTS
Page
ABSTRACT 1
INTRODUCTION 1
GEOLOGIC SETTING 1
METHODS OF DATA COLLECTION AND REDUCTION 2
ERRORS IN GRAVITY MEASUREMENTS AND METHODS 4Measurement Errors 4Interpretive Errors 4
INTERPRETATION OF GRAVITY DATA 5
SUMMARY 6
PRINCIPAL FACTS FOR GRAVITY STATIONS 7
REFERENCES CITED 19
ILLUSTRATIONS
[Plates are in pocket at back of the report]
Plate 1, 2. Maps showing:
1. Gravity stations, complete Bouguer gravity, and regional Bouguer gravity
2. Depth to bedrock
CONVERSION FACTORS AND ABBREVIATIONS
"Inch-pound" units of measure used in this report may be converted to International System (metric) units by using the following factors:
Multiply By To obtain
Acre-feet (acre-ft) 1,233 Cubic meters (m3)Feet (ft) 0.3048 Meters (m)Miles (mi) 1.609 Kilometers (km)
Geophysical and related units used in this report are as follows:
For gravity, milliGals (mGal).For density, grams per cubic centimeter (g/cm3).
ALTITUDE DATUM
The term "National Geodetic Vertical Datum of 1929" replaces the formerly used term "mean sea level" to describe the datum for altitude measurements. The datum is derived from a general adjustment of the first-order leveling networks of both the United States and Canada. For convenience in this report, the datum also is referred to as "sea level."
GRAVITY SURVEY AND DEPTH TO BEDROCK
IN CARSON VALLEY, NEVADA-CALIFORNIA
By Douglas K. Maurer
ABSTRACT
Gravity data were obtained from 460 stations in Carson Valley, Nevada and California. The data have been interpreted to obtain a map of approximate depth to bedrock for use in a ground-water model of the valley. This map delineates the shape of the alluvium-filled basin and shows that the maximum depth to bedrock exceeds 5,000 feet, on the west side of the valley. A north- south trending offset in the bedrock surface shows that the Carson-Valley/ Pine-Nut-Mountain block has not been tilted to the west as a simple unit, but is comprised of several smaller blocks.
INTRODUCTION
Carson Valley is the major storage reservoir of high-quality ground water in the Carson River basin (Glancy and Katzer, 1975, page 15). Ground water is a source of supply for the rapidly expanding urban population and for agricultural production a major economic base of the area. To assess the impact of these demands on the ground-water system in Carson Valley, data on the size and configuration of the reservoir are needed. Glancy and Katzer (1975, page 13) note that several wells as deep as 1,000 feet fail to penetrate basement beneath the valley fill; thus, the depth to bedrock is unknown throughout most of the valley.
The purpose of this study, made during the period from April 1980 through March 1981, was to determine the thickness of valley fill in Carson Valley using gravimetric geophysical methods. A gravity survey measures differences in the Earth 1 s gravitational field over the study area, and depth to bedrock can be calculated from these measurements.
GEOLOGIC SETTING
Carson Valley is bounded on the west by a steep, normal fault scarp with 5,000 feet of relief from the valley floor to the crest of the Carson Range (plate 1). The east side of the valley rises gently toward the crest of the Pine Nut Range through a fault system as much as 6 miles in width. The valley narrows to, the north where the Carson River drains the valley and to the south where the West Fork of the Carson River enters.
The mountain blocks bounding the valley to the east and west are westward-tilted structural units (Stewart, 1980, page 113), with Carson Valley occupying the downdropped western edge of the Pine Nut block (Moore, 1969, page 18). Recent westward tilting of the Pine Nut block is shown by faulting
-1-
along the east scarp of the Carson Range (Pease, 1979, page 15) and by displacement of the Carson River to the west side of Carson Valley (Moore, 1969, page 18).
The Carson Range is composed mainly of Cretaceous granodiorite (Pease, 1979, page 2). The crest of the Pine Nut Range is also composed of granodi orite, probably similar to that found in the Carson Range (Moore, 1969, page 18). In both ranges, some Triassic-Jurassic metavolcanic and medasedi- mentary rocks are exposed (Moore, 1969, page 16; Armin and others, 1983). Lower on the western flanks of the Pine Nut Range, Tertiary lake and stream deposits crop out and dip westward beneath the alluvial fill of Carson Valley (Moore, 1969, page 19).
In the north and south ends of the valley, the granodiorite and metavolcanic rocks form isolated bedrock knobs in the hills east of Jacks Valley, at Hot Springs Mountain, and in the hills south of Dresslerville (Moore, 1969). A large exposure of Tertiary volcanic rocks, mostly andesitic flows and breccia (Moore, 1969; Stewart and Noble, 1979), is located near the southeast end of the valley.
The Tertiary lake and stream deposits are variable in their degree of induration (Pease, 1979, page 4). They are described as soft sediments by Moore (1969, page 19), and as shales, siltstones, and sandstones by Stewart and Noble (1979). They are predominantly fine grained and similar in compo sition to the Pliocene Truckee Formation near Virginia City, Nev., 20 miles north of Carson Valley (Moore, 1969, page 13). Thus, these deposits probably form a hydrologic unit underlying Carson Valley. Moore (1969, page 19) suggests a total thickness of several hundred feet for the Tertiary sediments, and Robert C. Pease (1981, Nevada Bureau of Mines Geology, written communication) stated that 600 feet of Tertiary sediments are exposed in the hills east of Jacks Valley.
Sediments of Quaternary and Tertiary age probably form the major hydrologic unit in Carson Valley. The sediments range in lithology from fine-grained, flood-plain deposits of the Carson River on the valley floor to coarse Tertiary gravel, capping the semiconsolidated Tertiary sediments on the west flank of the Pine Nut Range.
Because water wells are drilled in both the Tertiary lake and stream deposits and in the unconsolidated Quaternary sediments, both will be treated as valley fill for purposes of gravity modeling.
METHODS OF DATA COLLECTION AND REDUCTION
The gravity measured by the gravity meter is in part determined by the density of materials which lie beneath it. A reading taken over a section of low density valley-fill deposits that overlie more dense crystalline bedrock is less than if the bedrock composed the entire section. This difference is referred to as a gravity anomaly. Corrections are made for altitude, latitude, earth curvature, and terrain roughness; and a value is computed for the measurement called a Bouguer anomoly. Measurements made over bedrock stations
2
reflect differences in the bedrock densities and the same corrections are applied to obtain a Bouguer anomoly for these stations. Bedrock stations on both sides of a valley define a regional gravity gradient. Subtracting the regional gradient from Bouguer anomolies measured over the valley fill gives a residual anomoly which is proportional to the thickness of the valley-fill material.
Gravity readings were taken at 460 stations (plate 1) in the study area at approximately a half-mile spacing. Most of the stations were located using topographic maps at a scale of 1:4,800 with a 5-foot contour interval. These maps, prepared for the Carson Valley Conservation District by Genge Aerial Surveys, Sacramento, Calif., permitted a location accuracy of 25 feet and a station altitude accuracy of ±1.5 feet. Sixty of the station altitudes were taken from preliminary U.S. Geological Survey topographic sheets (scale, 1:24,000), where altitudes of road intersections and hilltops were photo- grammetrically determined within ±6 feet. Four of the station altitudes on the east side of the valley were interpolated from contours on U.S. Geological Survey topographic maps (scale, 1:62,500) where altitudes were determined to an accuracy of ±12 feet.
A Texas Instruments Model-Ill^ gravity meter, with a scale constant of 0.0965 mGal (milliGal) per scale division, was used for the survey. This scale constant allowed readings to the nearest 0.01 mGal. A gravity base station used in this study, ACIC-2358-1, is located at the Douglas County Airport. The observed gravity of 979,606.24 mGal (Chapman's [1966] datum by Plouff, 1982), was used to tie in all stations. This base was read three times a day to provide corrections for tide and instrument drift.
The gravity readings were reduced to observed gravity and then converted to Bouguer anomalies using a computer program written by Plouff (1977). The program uses the International Gravity Formula of 1930 to calculate the anomaly, and applies corrections to the readings for altitude, latitude, earth curvature, and terrain from 1.42 to 103.6 miles from the station. A geographic grid interval of 1 minute was used for the digital terrain model. Terrain corrections from 0 to 1.42 miles were estimated by hand, using the Hayford-Bowie (1912, page 43) template. Hand terrain corrections were a maximum of 20 mGal along the crest of the Carson Range. The section titled "Gravity Data" lists the observed gravity and Bouguer gravity anomolies for the stations. The observed gravity data are also included in a regional gravity survey by Oliver and others (1982).
A computer program was then used to grid and contour the anomalies on a half-mile grid spacing. Nineteen readings were taken at stations on bedrock and Bouguer anomalies at these stations were contoured separately, by hand, to delineate the regional gradient of the gravity field. Lines of equal Bouguer gravity and the regional gradient are shown on plate 1. The regional gradient was then subtracted from the Bouguer anomolies to obtain residual anomalies, which should reflect the thickness of valley fill.
^ The use of brand names in this report is for identification purposes only and does not constitute endorsement by the U.S. Geological Survey.
-3-
Densities of 2.67, 2.00, and 1.70 g/cm^ (grams per cubic centimeter) were then assigned to bedrock, alluvium, and Tertiary sediments, respectively. A bedrock density of 2.67 g/cm3 is the standard value used for gravity surveys (Zohdy and others, 1979, page 90) and is an average of density values obtained by Pease (1979) for metamorphic and granitic rocks in the Carson Range. A density of 2.00 g/cm3 is used for valley-fill sediments by other authors in the Great Basin (Gimlett, 1967, page 18; Healey, 1970, page B52; Eaton and Watkins, 1970, page 545). The 1.70 g/cm3 value for Tertiary sediments was obtained from Pease (1979, page 19), who measured the density of sediments in Carson Valley, and from Gimlett (1967, page 18), who measured the density of sediments of the Truckee Formation which, as discussed previously, are similar to the Tertiary sediments found in Carson Valley.
The densities and residual gravity anomalies on a half-mile grid spacing were used as input to a three-dimensional inversion program from Cordell (1970). Using this program, depth to bedrock was calculated on a half-mile grid throughout the valley. The program was run once using a density contrast of 0.67 g/m3 and again with a density contrast of 0.97 g/m3 to obtain estimates of depths to bedrock on the east side of the valley where the less dense Tertiary sediments probably compose the entire valley-fill section. Depths obtained were then hand-contoured to obtain a depth-to- bedrock map (plate 2).
ERRORS IN GRAVITY MEASUREMENTS AND METHODS
Measurement Errors
The accuracy of the Bouguer gravity anomalies is limited by accuracy of the station altitudes and their horizontal positioning, and by repeatability of the readings.
Repeat readings were taken at 40 stations. Fifteen percent agreed within 0.03 mGal of the original reading, 60 percent agreed within 0.10 mGal, 98 percent agreed within 0.25 mGal, and 100 percent were within 0.49 mGal. Most station altitudes are known to the nearest 3 feet, giving a 0.18-mGal error; positions are known to within 25 feet, giving a 0.01-mGal error. Thus, the total error of each anomaly can be approximately 0.20 mGal. The maximum repeat error of 0.49 mGal occuring within the 0.20-mGal error possible for each anomaly gives a total "worst case" error of 0.69 mGal in observed gravity.
As a check on the accuracy of the calculated depths, the "worst case" error of 0.69 mGal was added to and subtracted from the values of the residual anomalies along a profile through the deepest part of the valley. The resultant depths differed from those calculated using the actual residuals by an average of 107 feet and by a maximum of 180 feet out of a total depth of about 5,000 feet.
Interpretive Errors
Errors in the interpretation of gravity data can occur as a result of (1) the assumed density assignments, (2) the assumption that densities of alluvial fill and basement are uniform, and (3) the validity of regional gravity contouring.
-4-
The computer program used to calculate depth to bedrock does not take into account varying densities with depth that might be significant if the less dense Tertiary sediments underlie the valley-fill materials. A thick section of less dense material would, in effect, increase the density contrast between bedrock and valley-fill materials, resulting in shallower calculated depths to bedrock. On the other hand, densities of valley fill probably increase with depth of burial, causing a decrease in density contrast. These two factors would tend to compensate for each other on the west side of the valley, where a thick section of unconsolidated valley-fill probably overlies less dense Tertiary sediments. In either case, the change in calculated depth to bedrock is relatively small. If the entire section consisted of less dense Tertiary sediments on the west side of the valley, the difference in calcu lated depths to bedrock is less than 30 percent. Drillers' logs show that valley-fill materials are at least 1,000 feet thick on the west side of the valley. Thus, errors in calculated depths to bedrock due to unknown horizon tal density variations are significantly less than 30 percent. Known lateral variations in density are corrected as described in the section, "Methods of Data Collection and Reduction."
Errors in contouring the regional gravity gradient are related to the uncertainty of large hand terrain corrections required for bedrock stations taken on mountain peaks and to estimation of the regional gradient over the center of the valley where no bedrock reading can be taken. Hand terrain correction errors may be as large as 2 mGal, and the error of estimating the regional gradient may approach 10 mGal. The latter could result in an error of 20 percent in calculated depth to bedrock. Estimating the regional gradient over large valleys is a problem inherent in all gravity studies. If calculated depths correspond closely to known depths, this error is probably small.
INTERPRETATION OF GRAVITY DATA
The distribution of Bouguer anomalies in Carson Valley follows the general trends shown by Erwin and Berg (1977) and Oliver and others (1982). Lines of equal depth to bedrock are shown on plate 2. The most conspicuous feature is a deep, elongate basin beneath the western half of Carson Valley. The depth of fill beneath Carson Valley exceeds 5,000 feet at a location about 2 miles southeast of Walleys Hot Springs. North of this basin, a bedrock high extends under Hobo Hot Springs to just south of Stewart, forming a separate basin beneath Jacks Valley up to 1,400 feet deep.
The steep gravity gradient on the east side of the basin implies offset of the basement. The offset extends from the west margin of Hot Springs Mountain to the Minden-Gardnerville area, with about 2,000 feet of relief. This north-trending scarp and the mapped zone of faulting on the east side of the valley imply that the Carson-Valley/Pine-Nut-Mountain block has not been tilted as a unit but is composed of at least two separate parts.
Depth to bedrock in the east half of the valley averages about 1,000 feet. A bedrock high extends south from Hot Springs Mountain about 3 miles. A basin with a maximum depth of 2,900 feet occurs east of this bedrock high. Bedrock beneath Fish Spring Flat appears to be relatively flat
-5-
and varies from 600 to 800 feet in depth. Two smaller basins occur between Fish Spring Flat and Gardnerville; the northern basin is 1,900 feet deep and the southern one 1,600 feet deep. These basins are separated from the main western basin by a ridge with 200 to 300 feet of relief.
The depth-to-bedrock configuration in plate 2 is consistent with well logs in the valley. Wells penetrating more than 20 feet of bedrock are plotted on plate 2 along with the depth where bedrock was first encountered. The depths correspond with calculated depths, and no wells were found to exceed calculated depths. The well penetrating bedrock at 750 feet was drilled after this interpretation was completed and tends to confirm the density contrasts assigned to valley-fill and bedrock materials.
SUMMARY
Data from 460 gravity stations in Carson Valley have been interpreted to obtain a map of approximate depth to bedrock, and the shape of the buried basin. The data show that the Carson-Valley/Pine-Nut-Mountain block has been tilted as two or more separate blocks. A structural scarp trends north-south near the center of the valley creating a deep, elongate basin under the west half of the valley and a relatively flat bench on the east.
Interpreted maximum depths show about 5,000 feet of fill on the west sideof the basin and a thickness of over 2,000 feet for Tertiary sediments on theeast side of the basin.
-6-
PRINCIPAL FACTS FOR
GRAVITY STATIONS
-7-
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-209.4
2-2
09.0
4-2
09.0
7-2
09
.51
-20
7.2
2-2
09.0
8-2
02.6
3
I NO
L
Sta
tion
(d
CU
SC
V
36
CU
SC
V
37
CU
SC
V
38
CU
SC
V
39
CU
SC
V
40
CU
SC
V
41C
US
CV
42
CU
SC
V
43
CU
SC
V
44
CU
SC
V
45
CU
SC
V
46
CU
SC
V
47
CU
SC
V
48
CU
SC
V
49
CU
SC
V
5CC
US
CV
51
CU
SC
V
52
CU
SC
V
53
CU
SC
V
54
CU
SC
V
55
CU
SC
V
56
CU
SC
V
57
CU
SC
V
58
CU
SC
V
59
CU
SC
V
60
CU
SC
V
61C
US
CV
6
2C
US
CV
63
CU
SC
V
64
CU
SC
V
65
CU
SC
V
66
CU
SC
V
67
CU
SC
V
68
CU
SC
V
69
CU
SC
V
7CC
US
CV
71
CU
SC
V
72
CU
SC
V
73
CU
SC
V
74
CU
SC
V
75
atitu
de
L
Bg
min
) (
39
5
.60
39
5.3
539
5.7
739
5.5
739
5.3
339
5.4
039
4.9
339
4.4
339
4.0
13?
3.4
739
2.6
53
9
2.1
73
9
0.0
73
9
0.0
733
59.3
03?
P .
6 3
59
1
. <
.f3
9
0.4
33
9
0.1
83
3
59
.78
I
3S
59.4
33
8
59.1
33
8
56
.48
38
55.5
038
55.5
03
3
54.6
338
54
.10
38
5
3.8
73
8
53
.55
38
5
3.1
53
8
52
.75
38
52.9
23
8
53
.02
38
52.3
33
8
52
.03
33
52
.02
38
51
.5
738
52
.02
38
51.9
83
3
52
.45
Altitu
de
ongitude
(feet
above
sea
le
g
min
) le
vel)
119
47
.07
| 4970.0
119
47
.60
4993.0
1 19
47
.52
4905.0
11
9
48.1
7
50
04
.01
19
48.8
3
51 5
0.0
1 19
49.5
3
51 7
3.0
11
9
49
.08
5
05
3.0
1 1
9
49
.22
4954.0
1 1
9
49.2
0
4960.0
1 19
4
9.2
3
49
53
.01
19
49
.52
4810.0
1 19
49
.77
4
75
3.0
11
9
46
.15
4694.0
11
9
46
.72
4
68
4.0
1 19
46
.72
4
68
4.
01
19
5
0.4
8
47
71
.0
119
S0.1
2
47
74
.01
19
50.0
3
4677.0
11
9
48.9
0
4669.0
1 1
9
50.4
3
4727.0
1 19
50
.17
|
46 9
8.0
11
9
49
.93
4685.0
119
50
.62
4762.0
19
50.2
5
4794.0
19
50
.72
4921.0
19
49.8
5
48
10
.019
49.5
3
48
25
.01
9
49.3
0
4805.0
19
49.1
0
4800.0
19
49
.08
4790.0
19
49.0
0
47
75
.019
48.4
3
47
24
.0119
48
.07
4
73
2.0
11
9
48.5
8
4806.0
1 1
9
48.0
6
4837.0
1 1
9
47.5
2
4791 .
0119
47.2
8
49
12
.01
19
47.0
5
47
76
.01
19
4
6.6
3
4790.0
11
9
46.6
3
4766.0
Ob
serv
ed
gra
vity
(mG
al)
97
95
99
.99
97
96
05
.07
97
96
02
.91
97
95
97
.33
97
95
90
.21
97
95
88
. 5
89
79
59
4.8
29
79
60
0.
23
979601 .
54
97
96
02
.96
97
96
1 0
.96
97
96
1 3
.09
97
96
01
.8
5979600.
79
P79599.4
59
79
61
0.4
19
79
61
2 .
52
97
96
1 3
.24
97
96
07
.21
979607 .
21
97
96
06
.07
97
96
04
.81
97
95
86
.86
979587.8
9979577.9
39
79
58
3.3
19
79
58
2.0
4979582.9
49
79
58
2.5
29
79
58
0.8
19
79
57
8.5
79
79
58
3.8
39
79
58
5.1
7979576.9
4979580.1
2979584.5
99
79
58
4.
74
97
95
86
.98
97
95
87
.35
97
95
88
.73
Fre
e-a
ira
no
ma
ly
(mG
al)
-32
.88
-25
. 27
-36
.32
-31
.75
-25
.34
1
-24
.91
-29
.26
-32
.42
!
-29
.93
-28
.37
-3?.
61-3
5.1
3-4
8.8
3
:-5
0.8
?
'-5
1 .
77
-33
.35
-3?.
71-3
9.5
6-4
5.9
8-3
9.9
4-3
3.8
9-4
5.
33-5
2.
1 5
-46
.67
-44
.69
-48
.46
-47
.55
-48.
19
-48
.61
-50
.67
-53
.73
-53
.52
-51
. 5
7-5
1.8
3-4
5.
30
-45
.1 4
-32
.95
-44
. 1
6-4
2.4
1-4
3.9
8
Te
rra
Han
d
0.2
43.3
10
.34
0.9
50.6
21
.60
0.3
80
.34
0.2
90
.55
2.2
43
.29
0.0
10.0
10.0
11
. 9
92.8
60.4
70
.01
4.5
37.0
93.0
83
.35
0.6
62
.40
0.6
10
.57
0.4
90.5
91 .2
62
.45
0.3
20.0
31
.45
0.3
20.0
90
.08
0.0
20
.01
0.0
1
in co
rre
ct
Com
p
1 .8
72.0
92.2
52
.45
2.6
73
.39
3.1
23.6
43.6
73
.87
4.9
05.5
71
. 71
1 .9
11
. 91
6.
63
6.
18
5.
79
3.5
26.1
55
.26
5.1
87
.26
7.0
37
.96
7.0
4,
7.0
6!
6.8
86
.94
7.6
58
.27
6.4
05.3
17
.53
6.1
55
.02
4.5
64
.24
3.6
63.4
6
ion
1
To
tal
2.1
1
|5
.40
'
2.5
9
i3.4
0
I3
.29
I
4.9
93
.50
3.9
83.9
64.4
27
. 14
8.8
61
.72
1 .9
21
.92
8.6
29.
046.2
63.5
310.6
81
2.3
58
.26
10.6
17.6
910.3
67.6
57
.63
7.3
77.5
38.9
110.7
26.7
25
.34
8.9
86
.47
5.1
14
.64
4.2
63.6
73.4
7
iou
gu
er
an
om
aly
(m
Ga
l)
-201.6
9-1
91.5
7-2
02
.42
-20
0.4
3-1
99
.1 2
-197.
79
-199.5
2-1
98.8
1-1
96.5
4-1
94.2
9-1
90
.90
-18
9.
76
-20
8.5
7-2
10
.03
-21
0.9
7-1
89.3
3-1
87
.84
-194.1
9-2
03
.06
-19
1 .
85
-18
6.5
7-1
98
.23
-20
5.3
3-2
CT
3.
87
-20
3.5
7-2
06.2
5-2
05
.86
-206.0
9-2
06.1
8-2
06.5
1-2
07.2
5-2
09
.29
-209.0
0-2
08.1
6-2
05.1
9-2
04
.82
-19
7.2
4-2
04
.17
-203.5
0-2
04
.44
I h- o
Altitude
Latitu
de
Longitude
(fe
et
above
Sta
tio
n
(de
g
min
) (d
eg
min
)
CU
SC
V
76
CU
SC
V
77
CU
SC
V
78
CU
SC
V
79
CU
SC
V
80
CU
SC
V
81C
US
CV
83
CU
SC
V
83
CU
SC
V
84
CU
SC
V
85
CU
SC
V
86
CU
SC
V
87
CU
SC
V
88
CU
SC
V
89
CU
SC
V
90
CU
SC
V
91C
US
CV
92
CU
SC
V
93
CU
SC
V
94
CU
SC
V
95
CU
SC
V
96
CU
SC
V
97
CU
SC
V
93
CU
SC
V
99
CU
SC
V100
CU
SC
V1
01
CU
SC
V102
CU
SC
V1 0
3C
US
CV
104
CU
SC
V105
CU
SC
V1
06
CU
SC
V1
07
CU
SC
V1C
3C
US
CV
109
c u s
c v 1
1 ncu
scvi
i 1
CU
SC
V1
12C
US
CV
1 1
3C
US
CV
1 1
4C
US
CV
1 1
5C
US
CV
1 1
6C
US
CV
1 1
7C
US
CV
1 1
3
33
52.9
033
53.3
33
8
53.7
23
8
54
.62
38
54.6
238
54.6
238
55.8
538
55.9
533
55.9
33
8
55.9
33
8
55
.77
38
55.9
33
8
55.9
33
8
55.9
53
8
55.5
038
55
.07
33
55.5
03
8
55.5
238
55.5
038
55.0
838
54
.63
38
54.6
338
55
. 23
33
5
6.
37
38
56.7
83
8
58.9
83
8
58.5
53
8
58.2
33
8
58.2
33
8
58
. 27
38
5
8.2
73
S
58.2
73
9
5.0
139
4.8
2?9
4.6
25
9
4.0
3?
5
4.2
739
4.6
53
9
4.9
6'3
9
6.4
23
9
0.3
039
0.7
239
1.1
7
11
9
46.6
8119
46.7
01
19
46.7
01
19
47 .
23
11
9
48.1
21
19
49.4
81
19
49.7
5119
49.3
31
19
48.7
21
19
4
8.1
51
19
48.1
31
19
47.5
51
19
47.0
51
19
46.1
71
19
4
6.1
71
19
4
6.1
5119
45.6
71
19
45.1
71
19
44.7
51
19
44
.75
119
45.5
8119
46.1
21
19
46.7
31
19
46
.75
119
46.7
51
19
4
6.7
7119
46
.77
11
9
46.7
5119
47
.32
11
9
48
.50
11
9
49
.52
11
9
50.3
01
19
48.1
71
19
47.6
31
19
48
.10
11
9
48.3
31
19
48
. 55
11
9
48.7
21
19
48.6
21
19
47
.2
51
19
46.7
01
19
46.7
21
19
4
6.7
2
sea
level)
Obse
rved
gra
vity
(mG
al)
47
50
.0
/97
95
88
.6S
4745.0
979588.2
94
73
6.0
I 979588.
78
4718.0
4709.0
4734.0
47
20
.04
69
9.0
46
99
.04700.0
4705.0
4706.0
47
14
.04
72
8.0
47
36
.04733.0
4792.0
47
45
.04
76
6.0
'4
77
2.0
4756.0
4730.0
4721.0
47
13
.04716.0
46
90
.04685.0
4699.0
46
90
.04
68
1 .
04
67
6.0
4697.0
4943.0
5096.0
52
12
.05
24
7.0
53
14
.05
21
0.0
52
45
.04
83
6.0
4680.0
4679.0
4672.0
979589.4
8979590.5
0979588.8
9979593.8
59
79
59
5.1
39
79
59
3.8
1979592.7
5979592.7
6979592.1
4979592.2
09
79
59
5.6
3979594.9
1979594.0
7979598.0
99
79
60
0.0
9979601.3
79
79
60
2.
14
97
95
96
. 79
979593.7
8979591.9
5979593.1
8979593.2
2979596.3
59
79
59
5.1
8979594.6
5979593.1
09
79
59
3.2
3979597.2
69
79
60
1 .
74
97
96
02
.02
979595.8
89
79
58
7.5
99
79
58
5 .
55
979531 .
27
97
95
86
.07
97
95
83
.62
979607.0
59
79
60
1 .
81
97
96
03
.67
97
96
05
.69
Fre
e-a
irT
err
ain
corr
ection
anom
aly
(m
Ga
l)
Han
d
-46.1
9-4
7.6
8-4
8.6
1-5
0.9
3-5
0.7
5-5
0.0
1-4
8.1
8-4
9.0
2-5
0.3
1-5
1 .
27
-50
. 5
6-5
1 .
32
-50
.51
-45
. 79
-45.
10-4
5.
59
-36.6
6-3
9.1
0-3
5.8
2-3
3.8
7-4
0.0
6-4
5.5
1-4
9.0
7-5
0.2
7-5
0.5
5-5
3.
10
-54.
11-5
2.8
5-5
5.2
5-5
6.0
2-5
2.4
6-4
6.0
1-3
2.5
2-2
4.0
0-2
1 .
09
-18.9
7-1
7.3
1-2
2.8
4-2
2.
46
-39
.6?
-50.
52
-49.
37-4
8.6
7
0.0
10
.01
i
0.0
1O
.D1
0.0
10.2
30
.09
'
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.1
00
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10.0
10.0
10
.16
2.8
70.4
90.7
70.5
4Q
.S9
0.7
00.3
60.3
80.6
20.0
10.0
10
.01
Com
p T
ota
l
3.3
1
3.3
23
.13
3.U
2.9
7
2.9
83
.03
3.0
43.9
2
3.9
36.3
4
6.5
75.6
5
5.7
44
.79
4.8
03.8
8
3.8
93.2
6
3.2
73.3
1
3.3
22.7
9
2.8
02
.48
2
.49
2.0
7
2.0
82
.15
2.1
62.2
4
2.2
51.9
2
1.9
31
.84
1
.85
1.7
4
1.7
51
.79
1.8
92.1
1
2.1
22
.34
2
.35
2.4
7
2.4
82.2
3
2.2
42
.15
2
.16
1.9
5
1.9
62.0
0
2.0
11.9
9
2.0
02
.26
2.2
73
.08
3
.09
4.4
5
4.6
15.9
0
8.7
72
.48
2.9
71.9
4
2.7
12.1
2
2.6
62
.27
3.1
62.3
6
3.0
62.5
2
2.8
82
.39
2
.77
2.
38
' 3.0
01.9
1
1.9
21
.91
1
.92
1.9
3
1.9
4
Bo
ug
ue
r anom
aly
(m
Ga
l)
-20
6.2
6-2
07
.76
-208.5
4-2
10.
17
-208.8
1-2
06.2
8-2
04.8
0-2
05
.85
-208.0
6-2
09
.68
-209.0
9-2
10.4
0-2
10
.1 7
-206.3
4-2
05
.85
-20
6.1
4-1
99.5
5-2
00
.46
-198.0
0-1
96.1
1-2
01
.53
-20
5.8
6-2
08
.98
-210.1
4-2
10.6
1-2
1 2
.47
-213.2
6-2
1 2
.49
-214.3
1-2
1 3
.95
-208.
70
-198.8
1-1
99.5
4-1
96
.52
-19
7.6
3-1
96.
20
- 196.9
4-1
99
.09
-20
0.0
1-2
02.9
5-2
09
.59
-20
8.4
0-2
01.4
4
L
Sta
tio
n
(d
CU
SC
V1
1 9
CU
SC
V1
20
CU
SC
V1
21C
US
CV
1 22
CU
SC
V1
23C
US
CV
12
4C
US
CV
12
5C
US
CV
1 26
CU
SC
V1
27C
US
CV
1 28
CU
SC
V129
CU
SC
V1
30
CU
SC
V1
31C
US
CV
1 32
CU
SC
V133
CU
SC
V1
34C
US
CV
1 35
CU
SC
V1
36C
US
CV
13
7C
U S
C V
1 3
3C
US
CV
1 39
CU
SC
VU
QC
US
CV
U1
CU
SC
V1
42
CU
SC
VU
3C
US
CV
1 44
cusc
vus
CU
SC
VU
6C
US
CV
1 4
7cu
scvu
sC
US
CV
14
9C
US
CV
1 50
CU
SC
V1
51C
US
CV
1 52
CU
SC
V1
53C
US
CV
1 54
CU
SC
V1
55C
US
CV
1 5
6C
US
CV
15
7C
US
CV
1 58
CU
SC
V1
59C
US
CV
1 60
atitu
de
L
on
gitu
de
eg
min
) (d
eg
min
)
39
1 .6
0
11
9
46
.73
39
1.
60
11
9
46.1
83
9
1 .6
0
119
45
.62
39
1
.60
11945 .
06
39
1
.60
11
94
4 .
48
39
1 .6
0
19
43.9
33
9
1 .6
2
19
43
.37
39
1
.60
19
4
2.8
239
2.0
5
19
42 .
80
39
2.4
3
19
42
.82
39
2.9
2
19
42.8
33
9
2.0
3
19
43
.38
39
2.4
8
19
43.3
839
2
.92
19
43.3
83
9
2.4
7
19
43
.93
39
2.0
3
19
43
.95
39
2
.05
1
19
44
.48
38
59.5
3
119
45.6
339
0.5
2
11
9
45
.60
39
0.9
5
119
45
.60
39
1 .3
8
11
9
45.6
03
9
2.0
5
11
9
45.6
23
9
2.4
8
119
45.6
239
2.9
3
11
9
45
.60
39
3.3
5
119
45.6
03
9
2.4
7
119
46.1
73
8
57
.73
1
19
4
6.7
338
59
.52
119
46.7
03
9
2.0
3
1 19
46.7
23
9
2.4
7
119
46
.72
39
2
.48
1
19
4
5.0
53
92
.47
119
44.4
739
2.9
2
119
44.4
83
9
2.9
2
1 19
45.0
539
3
. 35
1
19
4
4.4
739
2.8
7
1 19
4
3.9
339
1
.62
1
19
4
2.2
53
9
1 .0
3
119
42
.73
39
1
.05
1
19
42
.27
39
0.
73
11
9
42.5
03
9
0.7
5
119
41 .
97
39
0.3
2
1 19
42.1
5
Altitu
de
(f
ee
t above
sea
level)
46
66
.04
67
6.0
4679.0
4686.0
4707.0
4746.0
48
10
.04
87
7.0
48
33
.04
85
6.0
49
10
.04776.0
47
93
.04
81
3.0
4726.0
47
23
.04
69
8.0
4701.0
46
91
.0
4684.0
4681.0
46
71
.04
66
5.0
4657.0
4655.0
4660.0
4701.0
46
88
.04
66
6.0
46
56
.04674.0
4693.0
46
96
.04
67
1 .
04
70
5.0
-4
73
4.0
4941 .
04851.0
49
49
.04
86
2.0
49
46
.04874.0
Obse
rved
Fre
e-a
irgra
vity
an
om
aly
(m
Ga
l)
(mG
al)
979607.4
0
-48.1
6979607.3
8
-47
.24
97
96
08
.55
-4
5.7
99
79
60
9.9
2
-43.7
69
79
61
0.8
0
-40.
9f
97
96
11
.44
-3
6.6
0979609.2
5
-32.8
0979609.3
0
-26
.42
979614.6
6
-25
.86
97
96
14
.56
-2
4.3
6979613.0
3
-21.5
39
79
61
3.6
1
-32.2
4979616.0
3
-28
.88
97
96
17
.17
-2
6.5
19
79
61
6.7
8
-34
.42
97
96
14
.42
-3
6.4
1979612.5
2
-40
.69
979603.3
7
-45.8
5979606.0
0
-45
.62
97
96
06
.91
-4
6.0
0979608.0
3
-45
.79
97
96
10
.06
-4
5.6
99
79
61
2.0
4
-44.9
1979613.8
9
-44.4
7979616.1
2
-43
.05
979611.6
0
-45.8
09
79
59
4.2
6
-52.3
2979597.8
0
-52.6
3979608.9
5
-47
.24
979611.4
0
-46.3
8979612.8
8
-43.2
2979614.7
0
-39
. 6C
97
96
17
.00
-3
7.6
8979614.5
9
-42
.44
979618.5
1
-35.9
69
79
61
9.6
1
-31
.42
979612.5
5
-17
.19
979609.2
1
-28.1
29
79
61
0.5
1
-17.6
4979609.7
6
-26.0
9979609.8
6
-18
.13
97
96
09
.57
-2
4.5
5
Te
rra
Ha
nd
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10.0
20
.1 5
0.1
50.7
20.1
00.1
60.5
70
.06
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
10
.01
0.0
20.1
60
.01
0.4
40
.31
0.3
50.0
20.0
10.0
90
.09
0.0
3
tin corr
ection
Com
p T
ota
l
1.9
6
1.9
71
.75
;
1.7
61
.62
^
1.6
31
.52
' 1
.53
1.4
3'
1.4
41
.37
1.3
81
.28
1.2
91
.22
1
.24
1.3
0
1.4
51
.29
1
.44
1.2
3
1.9
51
.36
1
.46
1.3
6
1.5
21
.33
1
.90
1 .4
4
1 .5
01
.43
1
."
1.4
8
1.4
91
.60
1.6
11
.58
1
.59
1.6
0
1.6
11.6
1
1.6
21
.64
1
.65
1.6
7
1.6
81
.71
1
.72
1.7
4
1.7
51.8
1
1.8
22
.03
2
.04
1.9
0
1.9
11
.97
1.9
82.0
1
2.0
21
.58
1
.59
1.5
1
1.5
31
.52
1.6
81.6
1
1.6
21
.52
1
.96
1.4
4
1.7
51
.18
1
.53
1.2
2
1.2
41
.15
1
.16
1.2
0,
1.2
91
.14
1.2
31
.19
'
1.2
2
Bo
ug
ue
ranom
aly
(m
Ga
l)
-20
6.6
9-2
06.3
2-2
05.1
1-2
03.4
2-2
01
.37
-19
8.4
7-1
96
.95
-192.9
2-1
90
.64
-189.9
3-1
88
.45
-19
5.0
6-1
92.2
3-1
90.
16-1
95
.48
-197.4
4-2
00
.81
-20
5.9
5-2
05
.39
-20
5.5
2-2
05.2
0-2
04.7
2-2
03.7
0-2
02.9
5-2
01
.43
-20
4.2
8-2
11
.99
-211.9
8-2
05.7
6-2
04
.52
-202.4
1-1
99
.50
-197.5
3-2
01
.50
-195.8
4-1
92.5
1-1
85
.59
-19
3.7
2-1
86
.68
-192.0
2-1
86
.99
-190
.96
;
Sta
tion
CU
SC
V161
CU
SC
V1
62
CU
SC
V163
CU
SC
V1
64
CU
SC
V165
CU
SC
V1
66
CU
SC
V1
67
CU
SC
Vl
68
CU
SC
V1
69
CU
SC
Vl
70
CU
SC
Vl
71C
US
CV
l 72
'C U
S C
V 1
7 3
CU
SC
V174
CU
SC
V175
CU
SC
V176
CU
SC
V1 7
7C
US
CV
1 7
8C
US
CV
1 79
CU
SC
V180
CU
SC
V1
81C
US
CV
1 8
2C
US
CV
18
3C
US
CV
184
CU
SC
V1
85
-CU
SC
1 8
6C
US
CV
18
7C
US
CV
18
3C
US
CV
1 8
9C
US
CV
19
0C
US
CV
1 91
CU
SC
V1
92
CU
SC
V1
93
CU
SC
V1
94
CU
SC
V195
CU
SC
V1
96
CU
SC
Vl
97
CU
SC
V198
CU
SC
V199
CU
SC
V200
CU
SC
V201
CU
SC
V202
Latitu
de
(deg
min
)
39
0.0
73
8
59.6
73
8
59
.75
33
59.7
939
0.0
63
9
0.7
039
1.0
53
9
1.1
73<
? 0.8
73
9
1 .
333
? 0.5
?3
9
0.8
53
9
0.0
2[3
8
59
.65
I 39
2.9
839
3.2
53
9
3.7
53
9
4.7
339
5.4
83
9
5.4
73
9
4.5
23
9
5.1
23
8
57
.72
3d
57.2
83
8
57
.70
|38
56.5
7|3
8
56
.55
38
56.3
838
56.3
83
8
56.3
83
8
56.3
83
8
56
.96
38
56.6
83
8
56
.37
38
56.8
03
8
57.2
33
8
57.6
538
57.5
738
58
.02
38
58.4
338
58
.47
38
58.0
7
Lo
ng
itu
de
(deg
min
)
11
94
1 .7
21
19
41 .
98
1 19
42.5
01
19
43.1
31
19
43.4
21
19
43.5
3119
43.6
51
19
44
.37
11
94
4 .
92
11
94
5 .
02
11
94
4 .
48
11
9
44 .
02
1 1
9
44.4
71
19
44.4
81
19
46.7
2119
46.7
31
19
46.7
31
19
46.6
31
19
46.4
31
19
47.0
71
19
47.1
3119
47.2
51
19
47.2
21
19
46.0
7119
45.9
21 119
45.9
5!
11
9
45.0
71
19
44.4
81
19
43.9
2119
43.3
71
19
42.9
01
19
42.4
81
19
42.2
31
19
41 .
95
1 1
9
41 .9
51
19
41
.9
51
19
42.0
31
19
41
.4
31
19
41
.6
7119
41 .
67
1 1
9
42.2
2119
42.2
3
Altitu
de
(f
ee
t above
sea
leve
l)
49
12
.04
87
9.0
48
37
.04
79
5.0
4793.0
47
79
.04
77
9.0
4726.0
47
06
.04
69
3.0
4731 .
04
74
4.0
47
24
.04
72
3.0
46
50
.04
65
0.0
46
50
.04685.0
47
95
.04
86
5.0
48
16
.04
79
5.0
46
94
.04717.0
47
13
.04
73
8.0
47
43
.04
75
5.0
47
76
.04
79
5.0
48
26
.04
85
7.0
48
74
.04896.0
48
83
.04
90
5.0
4889.0
49
33
.04
89
7.0
48
98
.04
86
4.0
48
63
.0
Observ
ed
gra
vity
(mG
al)
579607.6
5579605.
51579607 .
24
57
96
10
.05
579609.
10
97
96
10
. 3
39
79
60
9.7
55
79
60
8.4
55
79
60
8.5
7579608.5
45796Q
9.
34579608.
70
57
96
08
.44
|57
96
07
. 2
69
79
61
4.
76
97
96
1 6
.74
979618.7
35
79
62
0.2
49
79
61
2.9
3979607.
1 1
97
96
1 2
.99
57
96
1 2
. 66
979592.4
6979597.5
35
79
59
8.
55
979601 .
19
57
96
02
.22
979603.3
6979602.6
6979601.
33
979599.9
71 9
79
59
9.5
5579598.5
6979597.5
59
79
59
9.3
1979597.
37
979597.2
35
79
59
5.6
05
79
59
6.3
39
79
59
6.4
0979597.
52
979597.2
8
Fre
e-a
iranom
aly
(m
Gal)
-22.5
3-2
7.1
9-2
9.
52-3
0.
72-3
2.2
5-3
3.2
8-3
4.3
8-4
0.8
3-4
2.1
5-4
4.0
8-3
8.
52
-38
.42
-39.
34
-40.
07
-44.3
3-4
2.
75
-41 .
49
-38
. 14
-36.
21-3
5.4
4-3
2.
76
-35.9
5-5
4.
76
-46.8
8-4
6.
85
-40.9
6-3
8.6
7-3
6.
16
-34.8
8-3
4.4
3-3
2.8
7-3
1 .
23
-30
.21
-28
. 7
0-2
8.
79
-29.3
0-3
1.5
6-2
8.9
3-3
2.2
5-3
2.6
9-3
4.8
2-3
4.
57
Te
rra
-
Ha
nd
0.0
30.0
10
.01
0.0
10.0
10.0
10.0
10
.01
0.0
10.0
10.0
1C
.01
0.0
1,
0.0
10.0
10
.03
0.1
00
.18
0.0
10.2
10.5
10.7
10
.01
0.0
10.0
10.0
10.0
10
.06
0.0
10
.05
0.0
60.0
10
.11
0.0
50.0
70
.01
0.0
10.1
10.0
30
.02
0.0
20
.02
Ln corr
ect
Com
p
1.1
61 .1
81
.21
1 .2
61 .2
71
.29
1.2
91.3
91
.46
1 .5
01
.38
1 .
35
1 .4
01
.41
2.0
52.0
72.0
92
.05
1 .8
5
,2.0
22
.02
2.1
82.2
61
.85
.78
.89
.69
.60
.51
1.4
51
.38
1.2
81
.28
1 .2
81.2
61.2
21.2
11
.18
1.1
91
.18
1.2
01
.22
ion
Bouguer
anom
aly
T
ota
l (m
Gal)
1.1
9
-190.2
71
.19
-1
93.8
01
.22
-1
94.6
71.2
7
-194.3
81
. 2
8
-195.
84
1.3
0
-196.3
61.3
0
-19
7.4
51.4
0
-202.0
01
.47
-2
02.5
61.5
1
-204.0
01
. 39
-199.8
61.3
6
-200.2
51.4
1
-200.4
31
.42
-2
01.
1 1
2.0
6
-202.2
32.1
0
-20
0.6
12
.19
-1
99
.26
2.2
3
-15
.7.0
61.8
6
-199.2
82.2
3
-200.5
32.5
3
-195.8
82.8
9
-19
7.9
92
.27
-2
13
.96
1.8
6
-20
7.2
71.7
9
-207.1
8.9
0
-20
1.7
5.7
0
-20
0.1
2.6
6
-198.0
5.5
2
-19
7.6
4.5
0
-197.8
6.4
4
-19
7.4
2.2
9
-196.9
9.3
9
-19
6.4
5.3
3
-19
5.7
5.3
3
-19
5.4
0.2
3
-19
6.7
61
.22
-1
98
.48
1.2
9
-19
7.2
91
.22
-1
99.4
51.2
0
-19
9.9
41
.22
-2
00.8
91
.24
-2
00
.58
Altitude
La
titu
de
Longitude
(fe
et
above
Sta
tion
(de
g
min
) (d
eg
m
in)
CU
SC
V2
03
3
8
58.9
3C
US
CV
204
33
59.3
0C
US
CV
20
5
38
5
5.9
5C
US
CV
206
33
5
5.9
5C
US
CV
20
7
38
55
.95
CU
SC
V2
08
38
55
.48
CU
SC
V209
38
5
5.0
8C
US
CV
210
38
5
4.6
3C
US
CV
211
38
5
4.6
5C
US
CV
212
38
54
.63
CU
SC
V2
13
3
8
54
.23
CU
SC
V2
14
38
53
.77
CU
SC
V2
15
38
54
.23
CU
SC
V216
38
5
4.2
5C
US
CV
21
7
38
5
4.2
7C
US
CV
21
8
38
53
.67
CU
SC
V2
19
3
8
53
.80
CU
SC
V220
38
53
.77
CU
SC
V221
38
54
.28
CU
SC
V222
38
53
.78
CU
SC
V223
38
5
3.7
8C
US
CV
224
38
5
3.3
5C
US
CV
225
38
52.8
8C
US
CV
22
6
38
52
.43
CU
SC
V2
27
3
8
52
.88
CU
SC
V223
38
52
.98
CU
SC
V2
2S
3
3 5
3.
08
CU
SC
V230
38
5?
. 95
CU
SC
V2
31
M
5
5.
55C
US
CV
232
38
53
.32
CU
SC
V233
|38
5
3.3
7C
US
CV
23
4
38
5
2.0
2C
US
CV
23
5
38
5
2.0
2C
US
CV
236
38
52.2
3C
US
CV
23
7
38
51
.55
CU
SC
V2
38
3
8
51 .
57
CU
SC
V239
38
51 .
20
CU
SC
V2
40
38
55
.87
CU
5C
V2
41
38
55
.43
CU
SC
V242
38
5
5.9
5C
US
CV
24
3
38
55.2
8C
US
CV
244
38
5
6.3
2C
US
CV
245
38
55.9
0
11
9
42.2
31
19
42.2
3119
44.5
21
19
4
4 .
92
11
9
43.9
21
19
43.5
51
19
43.0
71
19
43.3
81
19
43.9
01
19
4
4 .
47
119
44
.4
71
19
44.4
7119
45.1
21
19
43.8
51
19
43.3
71
19
43.3
71
19
43.8
7119
42.8
21
19
42.8
31
19
4
5.0
7119
45.8
21
19
44
.4
5119
44.4
5119
44.4
31
19
43.3
21
19
42.8
01
19
42.1
21
19
43.8
51
19
43.3
71
19
43.8
71
19
42.5
81
19
46.0
61
19
45.5
31
19
45.0
5119
45.2
31
19
46.6
21
19
46
.6
71
19
43.0
5119
42.8
71
19
42 .
42
1 19
42.4
51
19
41 .
43
11
9
40
.57
sea
leve
l)
4858.
04
85
5.0
47
65
.04
75
5.0
47
75
.04791 .
04
81
6.0
4852iO
48
42
.04
80
9.0
48
26
.04
84
5.0
47
97
.04
86
4.0
48
66
.04880.0
48
77
.04
89
3.0
48
37
.04
80
4.0
47
66
.04352.0
43
54
.04
86
8.0
49
18
.04
94
9.0
49
66
.04
89
0.0
43
95
.04882.0
4926.0
47
87
.04
79
0.0
48
25
.04844.0
4800.0
4822.0
48
17
.04
82
2.0
4856.0
4862.0
4936.0
49
86
.0
Ob
serv
ed
g
ravity
(mG
al)
97
95
99
.88
979603.4
5979601 .
96
979601 .
30
97
96
01
.6
49
79
59
9.7
19
79
59
7.4
6979596.5
5979597.7
99
79
60
0.
19
.97
95
98
.39
979597.6
59
79
59
7 .
09
97
95
97
. 3
6979596.2
99
79
59
5.
77
979597.1
39
79
59
4.9
79
79
59
8.2
4979596.2
99
79
59
3.
47
97
95
96
. 2
69
79
59
6.0
59
79
59
5.0
5979594.6
49
79
59
4.8
6970591 .
37
97
95
96
. 52
979595.3
5979596.
19
97
95
93
.36
979590.7
5979594.5
5979595.3
7979594.0
69
79
58
7.
10
97
95
85
.61
97
95
99
.00
57
95
98
.09
97
95
98
.02
579596.
35
979595.2
1979591 .
1 5
Te
rra
in corr
ection
Fre
e-a
ira
no
ma
ly
(mG
al )
H
and
-33.7
0
0.0
1-3
0.9
6
0.0
1-3
5.9
8
0.0
1-3
7.5
8
I 0
.04
-35.3
6
0.0
4-3
5.
1C
0.0
4-3
4.4
1
0.0
1-3
1.2
8
0.0
3-3
1.0
1
0.0
1-3
1.6
8
0.0
1-3
0.7
9
0.0
4-2
9.5
7
0.0
5-3
5.3
2
0.0
1-2
8.7
8
0.0
2-2
9.6
9
0.0
1-2
8.0
1
0.0
2-2
7.1
3
0.0
1-2
7.7
4
0.0
4-3
0.4
8
0.0
4-3
4.8
0
0.0
1-4
1.1
9
0.0
1-2
9.6
9
0.0
1-2
9.0
2
0.0
6-2
8.0
4
0.0
4-2
4.
41
I 0
.1 3
-21.4
2
0.1
6-2
2.
96
0.
18
-25
.27
I)
. 03
-26
.35
0.0
6-2
6.8
9
O.Q
5-2
5.1
6
, 0
.04
-39.3
5
0.0
1-3
5.2
7
0.0
1-3
1.4
7
0.0
1-2
9.9
9
0.0
1-4
1.1
2
Q.0
1-4
0.0
0
0.0
2-3
3.9
4
0.0
1-3
3.7
3
Q.0
1-3
1.3
7
Q.0
5-3
1.4
9
Q.0
7-2
7.2
0
Q.0
6-2
5.9
5
0.2
6
Com
p T
ota
l
1.1
9
1.2
0.1
9
1.2
0.6
5
1.6
6.7
4
1.7
8.5
6
1.6
0.5
6
1.6
0.5
4
1.5
5.5
7
1.6
01
.64
1.6
51
.76
1
.77
1.8
0
1.8
41.8
6
1.9
12.0
0
2.0
11
.67
1.6
91 .6
0
1 .6
11.6
7
1.6
91
.72
1
.73
1 .6
0
1 .6
41
.59
1
.63
2.0
7
2.0
82.3
9
2.4
01
.94
1
.95
2.0
2
2.0
82.0
9
2.1
31
.74
1
.87
1 .
64
1 .8
01
.59
1 .7
71
. 33
1 .8
61
. 70
1 .7
61
. 7
8
j 1
.83
1 .6
1
1 .6
53
.12
3
.13
2.7
7
2.7
82
.42
2.4
32.6
4
2.6
53.8
5
3.8
64.0
7
4.0
91
.45
1
.46
1 .4
8
1 .4
91
. 36
1 .4
11
.43
1
.50
1.2
2
1.2
81.
26
1.5
2
Bo
ug
ue
r anom
aly
(m
Ga
l)
-199.5
8-1
96
.74
-198.
23
-199.3
6-1
98.0
0-1
98.2
9-1
98
.51
-196.5
5-1
95
.89
-19
5.3
1-1
94
.94
-194.3
0-1
98
.31
-194.3
8-1
95.4
4-1
94.1
6-1
93.
14
-19
4.3
9-1
95.2
1-1
97.9
5-2
02.7
2-1
94.6
1-1
93.8
8-1
93
.33
-19
1.6
8-1
89.8
2-1
91 .
97
-19
1 .
58
-19
3.4
4-1
92.9
7-1
92
.93
-200.8
7-1
97
.24
-194.9
9-1
93
-94
-202.3
6-2
01
.75
-198.1
6-1
98
.09
-196.9
7-1
97
.21
-195.6
8-1
95.8
9
La
titu
de
Longitude
Sta
tio
n
(deg
min
) (d
eg
m
in)
CU
SC
V246
CU
SC
V2
47
CU
SC
V248
CU
SC
V249
CU
SC
V2
50
CU
SC
V2
51
CU
SC
V252
CU
SC
V2
53
CU
SC
V254
CU
SC
V2
55
CU
SC
V2
S6
CU
SC
V257
CU
SC
V2S
8C
US
CV
259
CU
SC
V2
60
CU
SC
V261
CU
SC
V262
CU
SC
V263
CU
SC
V264
CU
SC
V265
CU
SC
V266
CU
SC
V267
CU
SC
V268
CU
SC
V269
CU
SC
V270
CU
SC
V2
71
CU
SC
V2
72
CU
SC
V2
73
CU
SC
V2
74
CU
SC
V2
75
CU
SC
V2
76
CU
SC
V2
77
CU
SC
V278
CU
SC
V2
79
CU
SC
V2
80
CU
SC
V281
CU
SC
V282
CU
SC
V2
83
CU
SC
V284
CU
SC
V2
85
CU
SC
V2
86
CU
SC
V2
87
CU
SC
V2
88
38
5
5.5
83
8
55
.88
38
55.9
038
55
.27
38
54.8
338
5
4.8
538
54.6
738
54.4
538
54.3
538
54.3
838
53.9
038
5
3.5
538
5
3.1
038
53.1
238
53.5
538
5
8.5
738
58.5
538
5
8.1
238
5
8.1
23
8
58
.12
38
58
.13
38
5
7.6
838
5
6.8
233
5
7.1
238
57.6
838
5
7.6
838
5
7.4
833
56
.82
38
57.2
738
57.6
833
58
.07
33
57
.97
33
5
8.5
738
58.5
738
5
8.5
738
5
7.4
533
5
9.4
333
59.4
338
5
9.9
733
5
8.5
733
5
8.5
738
5
8.9
833
5
9.4
3
1 19
41
.0
2119
41 .
50
1 19
41
.9
51
19
41
.6
71
19
41
.4
8119
40
.67
1 19
41
.0
81
19
40.5
81
19
41 .
1 7
1 19
41
.6
71
19
40.7
81
19
40.7
81
19
4
0.7
811941 .
42
1 19
41
.4
0119
46
.18
11
9
45.5
81
19
45.5
81
19
46.1
8119
45
.05
1 19
4
4.5
01
19
44 .
50
11
94
4 .
48
11
9
44
.87
11
94
5 .
05
119
45
.57
119
43.9
31
19
43.6
3119
43.3
51
19
43.3
71
19
42
.83
119
43.9
21
19
43.9
21
19
43.3
71
19
4
2.8
71
19
42
.68
1 1
9
43.1
31
19
43
.68
1 19
4
3.8
51
19
44
.4
71
19
45.0
311945 .
03
119
45
.03
Altitude
(feet
above
O
bse
rved
sea
gra
vity
leve
l)
(mG
al)
4958.0
979591.5
64
94
0.0
9
79
59
2.9
34912.0
979594.1
74
89
8.0
979593.6
24945.0
979589.5
75
03
8.0
979585.6
04
98
0.0
9
79
58
8.8
85
05
9.0
979584.4
15
00
3.0
9
79
58
7.2
14
94
5.0
9
79
58
9.0
64
97
3.0
9
79
58
9.6
64
98
1.0
979589.4
64
98
3.0
979591.1
34949.0
979593.5
44936.0
9
79
59
2.5
34
70
3.0
979597.5
84713.0
9
79
60
0.7
44716.0
979600.6
44
70
6.0
9
79
59
7.2
54726.0
9
79
60
3.5
74746.0
979604.9
74
74
5.0
979605.1
44
74
9.0
979605.0
94
73
7.0
979604.4
64
72
8.
a
979603.3
54717.0
979600.7
44
76
6.0
,9
79
60
5.9
24
78
0.0
979603.6
44
79
0.0
979604.0
24803.0
979602.6
84832.0
9
79
59
9.0
34779.0
979604.3
24
76
7.0
9
79
60
4.6
04
79
4.0
979602.2
74
82
4.0
9
79
60
0.0
94849.0
979601.8
64789.0
9
79
60
7.8
24754.0
9
79
60
7.4
74
75
6.0
979608.6
44741 .
0
979606.6
14725.0
979604.2
04719.0
979605.3
74
71
1.0
9
79
60
6.4
0
Fre
e-a
ir
anom
aly
(m
Ga
l)
-27
.70
-28.4
6-2
9.8
8-3
0.8
2-2
9.8
1-2
5.0
7-2
6.9
7-2
3.7
0-2
6.0
1-2
9.6
6-2
5.7
2-2
4.6
5-2
2.1
4-2
2.9
5-2
5.8
1-5
0.0
4-4
5.9
1-4
5.1
0-4
9.4
3-4
1.2
3-3
7.9
6-3
7.2
3-3
5.6
4-3
7.8
4-4
0.6
2-4
4.2
6-3
4.1
8-3
4.1
7-3
3.5
1-3
4.2
4-3
5.7
3-3
5.2
8-3
7.0
1-3
6.8
0-3
6.1
6
,-3
0.3
9-3
2.9
8
'-3
6.6
2-3
6.0
6-3
7.
44-4
1.
36-4
1.4
5-4
1 .
74
Terr
ain
corr
ection
Bouguer
Hand
0.0
80.2
50
.01
0.0
10.0
70.0
90.0
50
.04
0.0
50
.06
0.1
60
.04
0.1
90
.05
0.0
20.0
10.0
10
.01
0.0
10.0
10
.06
0.0
30.0
20
.01
0.0
10
.01
0.0
10
.01
0.0
10
.02
0.0
10
.03
0.0
10
.01
0.0
20
.10
0.0
10.0
10
.01
0.0
30.0
10.0
10
.01
an
om
aly
C
omp
To
tal
(mG
al)
1.3
0
.38
I1.2
8
.53
1.3
0
.31
1.3
8
.39
1.3
7
.44
1.3
2
.41
1 .3
7
11 .
42
1.3
5
1.3
91.
39
1 .4
41
.44
1
.50
1.5
2
1.6
81
.57
1.6
11
.65
1
.84
1.6
4
1.6
91.5
9
1.6
11
.79
1
.80
1.6
3
1.6
41
.67
1.6
81
.82
1.8
31
.56
1
.57
1.4
6
1.5
21
.50
1.5
31
.56
1.5
81
.60
1 .6
11
.60
1
.61
1.7
0
1.7
11
.43
1
.44
1.4
4
1.4
51.3
6
1.3
71
.32
1
.34
1.2
6
1.2
71
.37
1.4
01
. 36
1 .3
71
.29
1.3
01.2
5
1.2
71.2
6
1.3
61
.27
1.2
81
.33
1.3
41
.32
! 1
.33
1.4
3
1 .4
61
.52
1
.53
1.
50
1.5
11
.49
1
.50
-19
6.8
3-1
96.8
2-1
97
.50
-19
7.8
9-1
98
.43
-19
6.9
0-1
96
.81
-196.2
7-1
96
.62
-198.2
2-1
95
.06
-194.3
3-1
91
.66
-19
1.4
6-1
93.9
6-2
10.0
2-2
06
.39
-20
5.6
4-2
09.4
8-2
02
.22
-19
9.6
9-1
98.9
2-1
97
.41
-199.1
6-2
01
.64
-20
4.8
0-1
96
.68
-197.1
4-1
96.9
0-1
98.0
9-2
00.6
6-1
98.2
5-1
99
.61
-200.3
9-2
00
.81
-19
5.8
0-1
96
.43
-19
8.8
1-1
98.3
2-1
99
.06
-20
2.3
5-2
02.2
6-2
02.2
8
Sta
tion
CU
SC
V2S
9C
US
CV
29
CC
US
CV
29 1
-CU
SC
V2
92
CU
SC
V2
93
CU
SC
V294
CU
SC
V2
95
CU
SC
V296
CU
SC
V2
97
CU
SC
V2
98
CU
SC
V299
CU
SC
V300
CU
SC
V3
01
CU
SC
V3
C2
CU
SC
V3
03
CU
SC
V304
CU
SC
V3
05
CU
SC
V3
06
CU
SC
V307
CU
SC
V3
08
CU
SC
V3
09
CU
SC
V310
CU
SC
V31
1C
US
CV
31
2C
US
CV
31 3
CU
SC
V31
4C
US
CV
31 5
CU
SC
V31
7C
US
CV
318
CU
SC
V31
9C
US
CV
320
CU
SC
V321
CU
SC
V322
CU
SC
V3
23
CU
SC
V3
24
CU
SC
V3
25
CU
SC
V326
CU
SC
V327
CU
SC
V328
CU
SC
V329
CU
SC
V33
CC
US
CV
331
CU
SC
V332
CU
SC
V3
33
La
titu
de
(deg
min
)
38
59
.02
37
3.7
835
4
.2?
\ 39
4
.65
' 3
9
5.0
33
9
3.9
239
4.3
73
9
5.1
039
3.7
539
4.2
339
4.5
039
5.0
339
5.7
53
9
6.2
03
9
6.1
539
6.2
73
8
52
.80
38
52
.63
38
53.8
538
53
.75
38
54
.30
38
54.7
038
54
.85
39
0.9
73
9
0.2
33
9
2.0
83
9
2.4
63
9
1.8
13
9
1.5
339
1.1
539
1.3
63
9
0.7
139
0.8
53
9
0.7
139
5.6
03
9
3.5
83
9
3.4
33
9
3.1
339
2.9
538
58
.98
38
58.9
638
58
.63
38
59.1
038
59.4
6
Longitude
(deg
min
)
119
45.5
71
19
45
.5
21
19
45
.4
31
19
45
.33
11
9
45.2
51
19
4
4.7
01
19
4
4.6
71
19
44
.4
8119
45
.98
11
9
45.8
31
19
4
6.2
8119
46.0
21
19
4
5.5
51
19
45 .
62
1 19
4
4.8
51
19
43
.97
1 19
41
.8
51
19
41
.0
81
19
41 .
37
1 19
42.0
1119
42
.30
119
42.6
21
19
42.1
01
19
47
.93
11
9
48.1
31
19
48
.88
1 19
48.3
1119
48
.35
1 19
4
8.9
0119
48.9
11
19
4
7.7
8119
48
.91
11
9
49
.63
1 19
47.2
11
19
44.4
61
19
47
.56
1 19
4
8.1
619
4
7.6
819
4
7.9
819
47.2
119
4
7.6
819
48.3
119
48.6
619
4
9.3
5
Altitu
de
(f
ee
t above
se
a
leve
l)
47
10
.04
64
9.0
46
46
.04
64
1 .
04
63
9.0
46
53
.04644.0
46
36
.04
65
0.0
4646.0
4654.0
4656.0
46
70
.04
71
9.0
46
57
.04807.0
4906.0
50
26
.04954.0
48
71
.04845.0
4840.0
4870.0
4665.0
4668.0
46
60
.04
65
8.0
46
60
.04
86
3.0
46
63
.04
66
1.0
4666.0
4666.0
4672.0
4632.0
46
79
.04
70
8.0
4667.0
46
54
.04686.0
4677.0
4681,0
46
76
.04
66
8.0
Obse
rved
Fre
e-a
ir
gra
vity
anom
aly
(m
Gal)
(mG
al)
579601 .
27
57
06
1 7
.95
97
96
1 8
.91
1979619.0
9
I9
79
61
9.7
1
!579620.9
5
1979622.4
0979623.3
197961 7
. 58
97961 8
.64
579620.4
3579620.5
3979620.
399
79
61
9.2
99
79
62
2.0
057961 6
.03
979597.5
3979590.2
6979590.
1 7
979595.6
69
79
59
6.8
9579598.0
39
79
59
4.3
69
79
60
8.5
89
79
60
4.
3797961 4
.48
57
96
1 5
.65
579612.2
19
79
61
3.4
69
79
61
2.9
1979609.
78979610.9
497961 5
.1 7
979604.4
8979623.6
99
79
61
9.7
59
79
61
7.9
257961 8
.38
97
96
1 6
.60
979595.5
49
79
59
6.4
79
79
59
4.4
6979597.2
65
79
60
2.5
1
-46
.36
-42.4
1-4
2.
38-4
3.3
0-4
3.4
3-3
9.2
4-3
9.
30-4
0.2
2-4
2.
64-4
2.6
7-4
0.
52-4
1 .
01
-40.9
0-3
8.0
5-4
1.1
0-3
3.1
4-2
2.5
3-1
8.2
7-2
6.9
2-2
9.0
9-3
1.1
1-3
1 .
03
-32
. 10
-46.
1 4
-48
.98
-42.3
5-4
1 .
92
-44.2
2-2
3.4
8-4
2.2
7-4
5.8
9-4
3.3
1-3
9.2
8-4
9.2
0-4
0.9
5-3
7.
50-3
6.3
8-3
9.
33-4
2.0
7-5
4.
28-5
4.
17-5
5.3
2-5
3.6
8-4
9.7
1
Te
rra
in corr
ection
Han
d
0.0
10
.01
0.0
10
.01
0.0
10.4
60
.42
0.2
60
.01
0.0
10
.05
0.1
30.5
30
.47
0.0
41.7
80.2
60
.36
0.0
30
.02
0.0
30.1
00
.04
0.0
10
.01
0.0
90.0
30
.01
0.0
10
.01
0.0
10
.01
0.0
40.0
20.3
30
.37
0.2
20.0
90
.01
0.0
10.0
50
.01
0.0
20.2
5
Com
p
1 .6
01
.76
1 .
77I
1 .7
91
.78
' 1
.66
1 .7
41
.70
1.8
41
.85
1.9
71
.93
1.8
11
.78
1.7
31
.41
1.7
41 .6
41
.52
1.6
21
.57
1.5
31
.47
2.6
42
.72
4.0
53
.26
3.2
03
.36
3.7
92
.55
3.6
55
.07
2.1
61
.74
2.5
12
.98
2.6
22
.92
2.1
42
.42
2.8
93
.22
4.1
9
Tota
l
1 .6
11
. 77
1 .
781
.80
I 1.7
92.1
22.1
61 .9
61
.85
1 .8
62
.02
2.0
62
.34
2.2
51
.77
3.1
92.0
02.0
01
.55
1 .6
41
.60
1 .6
31
.51
2.6
52.7
34
.14
3.2
93.2
13.3
73.8
02.5
63.6
65
.11
2.1
82.0
72.8
83.2
02
.71
2.9
32.1
52.4
72.9
03.2
44
.44
Bo
ug
ue
r a
no
ma
ly
(mG
al)
-206.
76-2
00
.57
-20
0.4
2-2
01 .
16
-20
1.2
2-1
97.
19-1
96.8
9-1
97.7
3-2
00.7
5-2
00.6
3-1
98
.60
-19
9.
12-1
99.2
0-1
98
.1 3
-199.5
3-1
95
.29
-18
9.2
6-1
89
.10
-195.7
5-1
94.9
8-1
96.1
5-1
95
.87
-198.0
9-2
03.9
7-2
06.8
3-1
98.5
1-1
98
.87
-201.3
1-1
87.3
6-1
98.8
7-2
03
.67
-200.1
5-1
94.6
8-2
07.7
4-1
98
.22
-19
5.5
7-1
95.1
3-1
97
.1 7
-19
9.2
4-2
1 3
.33
-21
2.5
9-2
13
.44
-21
1.2
9-2
05
.85
Altitu
de
L
atitu
de
Longitude
(feet
above
O
bse
rve
d
Sta
tion
(deg
min
) (d
eg
min
)
CU
SC
V3
34
CU
SC
V3
35
CU
SC
V336
CU
SC
V3
37
CU
SC
V3
38
CU
SC
V339
CU
SC
V3
40
CU
SC
V34
1C
US
CV
34
2C
US
CV
343
CU
SC
V344
CU
SC
V345
CU
SC
V3
46
CU
SC
V3
47
CU
SC
V348
CU
SC
VH
9C
US
CV
550
CU
SC
V35
1C
US
CV
552
CU
SC
V3
53
CU
SC
V5
54
CU
SC
V355
CU
SC
V3
56
CU
SC
V357
CU
SC
V3
58
CU
SC
V354
CU
SC
V56
QC
US
CV
36
1C
US
CV
363
CU
SC
V365
CU
SC
V366
,C
US
CV
367
CU
SC
V368
CU
SC
V369
CU
SC
V3
70
CU
SC
V371
CU
SC
V372
CU
SC
V3
73
CU
SC
V374
CU
SC
V375
CU
SC
V376
CU
SC
V377
CU
SC
V378
33
58
.60
38
57.3
83
8
57.8
038
5
7.3
638
57.3
638
56.9
038
5
6.6
038
56.5
03
8
56.9
338
55.6
338
54
.96
33
55.2
633
5
7.1
638
56
.36
38
56
.80
38
56.3
538
5
5.
3(S
38
54.9
0?S
54
. ?
038
55.2
133
5
5.0
638
5
3.6
833
5
4.1
833
53.3
033
51
.18
38
50.2
038
48
.81
39
2.7
33
9
2.5
139
3.6
53
9
2.3
039
1.6
33
9
2.4
63
9
1.2
139
1.5
53
9
1.8
639
0.5
63
9
1.1
33
9
1.0
83
9
0.3
83
9
0.4
139
0.1
03
9
1.0
0
119
49.3
01
19
49.0
11
19
49
.75
11
9
47
.86
1 19
4
8.4
81
19
47
.28
11
9
48
.13
119
45
.96
1 19
4
6.0
81
19
44.2
31
19
4
3.6
11
19
44.2
81
19
49.5
51
19
49.6
81
19
49.5
31
19
48
.90
119
48.1
11
19
4
8.0
11
19
50.5
11
19
47
.20
119
45.3
01
19
47
.20
1 19
47.4
11
19
48.3
01
19
47.4
01
19
4
7.5
81
19
46
.75
11
9
42.4
11
19
41 .
65
119
39
.28
119
40
.05
119
39.0
81
19
3
7.5
01
19
41 .
13
11
9
40
.25
1 19
41
.0
61
19
41 .
06
11
9
40
.08
11
9
37
.80
119
38.3
81
19
39.2
51
19
39.9
1119
38.8
5
sea
gra
vity
leve
l)
(mG
al)
46
74
. (j
97
95
97
.35
4683.0
'9
79
59
3.6
84
67
0.0
9
79
59
6.6
74686.0
9
79
59
1.5
04685.0
9
79
59
2.2
94
69
9.0
9
79
59
2.0
14693.0
^9
79592.
284
72
1.0
9
79
59
7.1
94
72
2.0
9
79
59
6.7
74778.0
979600.9
24
80
4.0
979599.3
64783.0
9
79
60
1 .
43
4682.0
9
79
59
5.8
04685.0
9
79
59
6.3
84
68
1.0
9
79
59
5.9
74
69
2.0
979594.6
64
70
6.0
9
79
59
2.6
54708.0
979591 .
14
4-74
Q.O
9
79
57
5.3
34
71
3.0
979591.5
54752.0
979599.
744
72
6.0
979586.9
54717.0
9
79
58
8.3
44724.0
979586.2
54
86
5.0
9
79
58
1.3
15
03
9.0
979570.5
35070.0
1979565.8
34
93
8.0
9
79
61
3.1
95102.0
9
79
60
7.2
15918.0
I 979558.
705296.0
979584.5
95275.0
9
79
57
6.2
35726.0
979556.3
75063.0
979606.0
15
61
1.0
979567.4
55213.0
979600.8
65064.0
9
79
60
1.0
45
19
1.0
9
79
59
3.0
05
40
2.0
9
79
56
4.1
55
40
3.0
979556.8
35198.0
9
79
57
8.5
65
09
6.0
9
79
58
6.7
75394.0
9
79
56
3.3
3
Fre
e-a
ir
anom
aly
(m
Gal)
-53
.04
-54.0
7-5
2.9
2-5
5.
9A-5
5.2
5-5
3.
53-5
3.
39-4
5.
70-4
6.6
6-3
5.3
3-3
3.4
6-3
3.
31-5
1.
72-4
9.6
9-5
1 .
12
-50
. 73
-49
. 9
7-5
0.
62-
4 5
. 9
F-5
0.1
9-3
8.
12-5
1 .
32
-51 .
52
-51
. 6
5-4
0.2
3-3
3.2
1-3
2.9
6-1
8.4
6-8
.70
1 7
.80
-12
.78
!
-22.1
3-0
.82
-1 1
.6
60.7
9-3
.66
-15
.58
-12.5
2-2
1 .
46
-27.6
6-2
5.2
4-2
6.1
6-2
2.9
2
Te
rra
in corr
ection
Ha
nd
0.2
10.0
40
.41
0.0
90.0
50.0
30.0
40.0
40
.01
0.0
10
.01
0.0
10
.1 4
0.
190.2
60
.01
0.0
10
.01
2.
7<*
0.0
10
.01
0.0
10.0
10
.02
0.2
12
.04
0.4
90
.33
0.3
31
.08
0.0
90.0
60.6
80
.12
2.5
40.5
10.1
40.3
40
.11
0.6
10
.11
0.0
10.5
0
Com
p T
ota
l
4.0
83.7
74
.95
2.6
93
.17
2.4
23
.04
1.9
21 .9
01
.63
1 .6
11
.68
4.7
25
.29
4.8
13
.93
3.4
73
.62
8.
512
.78
1 .9
43
.44
3.4
15
.48
5.2
45
.62
4.2
61
.23
1.1
3I
1.5
0i
1.1
31
.18
1.
311
.10
1.3
01.0
71
.08
1 .0
81
.26
1 .1
21
.12
1.1
11.1
1
4.2
93.8
15.3
62.7
83
.22
2.4
53.0
81.9
61
.91
1 .6
41
.62
1 .6
94.8
65.4
85
.07
3.9
43
.48
3.6
31
1 .0
52.7
91
.95
3.4
53
.42
5.5
05
.45
7.6
64.7
51 .5
61
.46
2.5
81
.22
1.2
41
.99
1 .2
23
.84
1.5
81
.22
1 .4
21
.37
1 .7
31.2
31
.12
1 .6
1
Bo
ug
ue
r anom
aly
(m
Ga
l)
-209.5
4-2
11
.35
-20
8.2
0-2
14.3
5-2
1 3
.18
-21
2.7
2-2
11
.74
-20
6.1
3-2
07.1
8-1
98
.04
-19
7.0
7-1
96.6
4-2
07
.92
-205.3
7-2
07
.08
-20
8.1
9-2
08
. 37
-20
8.9
4-2
04.8
2-2
09
.52
-19
9.6
2-2
10
.44
-21
0.3
5-2
08.6
5-2
02.1
0-1
98
.83
-202.5
5-1
86.7
3-1
82
.68
-182.9
5-1
93.6
4-2
02.2
4-1
95
.60
-18
4.5
4-1
88
.22
-181.3
1-1
88
.49
-18
9.5
7-2
05.7
9-2
11.6
6-2
02.7
4-2
00.2
7-2
06
.73
Altitu
de
L
atitu
de
Longitu
de
(feet
above
Sta
tio
n
(deg
min
) (d
eg
min
)
CU
SC
V3
79
CU
SC
V380
CU
SC
V381
CU
SC
V382
CU
SC
V383
CU
SC
V3
84
CU
SC
V3
85
CU
SC
V386
CU
SC
V387
CU
SC
V388
CU
SC
V389
CU
SC
V3
90
CU
SC
V3
91
CU
SC
V3
92
CU
SC
V393
CU
SC
V3
94
CU
SC
V3
95
CU
SC
V396
CU
SC
V397
CU
SC
V3
98
CU
SC
V399
CU
SC
V400
CU
SC
V401
CU
SC
V4Q
2C
US
CV
4C
3C
US
CV
404
CU
SC
V4
05
CU
SC
V406
CU
SC
V4
C7
CU
SC
V4
08
CU
SC
V409
CU
SC
V4
1Q
CU
SC
V4
1 1
CU
SC
V41
?'
CU
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(deg
min
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46.0
81
19
46.0
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1 4
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Ln
corr
ect:
Com
p
3.4
03.4
63
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3.6
54.2
74.0
34
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4.7
41
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1 .9
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49.8
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Bo
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Gal)
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3.1
1-1
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4-1
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1-1
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1.8
0-1
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.00
-183.3
8-1
85
.86
REFERENCES CITED
Armin, R. A., John, D. A., and Dohrenwend, J. C., 1983, Geologic map of theFreel Peak 15-minute quadrangle, California and Nevada: U.S. Geological Survey Miscellaneous Investigatons Map 1-1424.
Chapman, R. H., 1966, Gravity base station network: California Division of Mines and Geology Special Report 90, 53 p.
Cordell, Lindrith, 1970, Iterative three-dimensional solution of gravity anomaly data: U.S. Geological Survey Computer Contribution 10, 12 p. Available only from National Technical Information Service, U.S. Department of Commerce, Springfield, Va., 22161; accession no. PB-196 979.
Eaton, G. P., and Watkins, J. S., 1970, The use of seismic refraction andgravity methods in hydrogeological investigations, -In Merely, L. W., ed., Mining and groundwater geophysics 1964: Geological Survey of Canada, Economic Geology Report 26, p. 544-568.
Erwin, J. W., and Berg, J. C., 1977, Bouguer gravity map of Nevada, Reno sheet: Nevada Bureau of Mines and Geology Map 58.
Gimlett, J. I., 1967, Gravity study of Warm Springs Valley, Washoe County, Nevada: Nevada Bureau of Mines Report 15, 31 p.
Glancy, P. A., and Katzer, T. L., 1975, Water-resources appraisal of theCarson River basin, western Nevada: Nevada Division of Water Resources, Reconnaissance Report 59, 126 p.
Hayford, J. F., and Bowie, William, 1912, The effect of topography andisostatic compensation upon the intensity of gravity: U.S. Coast and Geodetic Survey Special Publication 10, 132 p.
Healey, D. L., 1970, Calculated in situ bulk densities from subsurface gravity observations and density logs, Nevada Test Site and Hot Creek Valley, Nye County, Nevada, in Geological Survey Research 1970: U.S. Geological Survey Professional Paper 700-B, p. B52-B62.
Moore, J. G., 1969, Geology and mineral deposits of Lyon, Douglas, and Ormsby Counties, Nevada: Nevada Bureau of Mines and Geology Bulletin 75, 42 p.
Oliver, H. W., Plouff, Donald, and Robbins, S. L., 1982, Bouguer gravity map of California Walker Lake sheet: California Division of Mines and Geology.
Pease, R. C., 1980, Geologic map, Genoa quadrangle [Nevada]: Nevada Bureau of Mines and Geology Urban Maps Series, Genoa Folio, Map ICg.
Plouff, Donald, 1977, Preliminary documentation for a FORTRAN program tocompute gravity terrain corrections based on topography digitized on a geographic grid: U.S. Geological Survey Open-File Report 77-535, 45 p.
-19-
Plouff, Donald, 1982, Gravity observations in the Walker Lake 1° X 2° quadrangle California-Nevada: U.S. Geological Survey Open-File Report 82-405, 105 p.
Stewart, J. H., 1980, Geology of Nevada: Nevada Bureau of Mines and Geology Special Publication 4, 135 p.
Stewart, J. H., and Noble, D. C., 1979, Preliminary geologic map of the Mount Siegel Quadrangle, Nevada-California: U.S. Geological Survey Open-File Report 79-225.
Zohdy, A. A. R., Eaton, G. P., and Mabey, D. R., 1974, Application of surface geophysics to ground-water investigations: U.S. Geological Survey Techniques of Water-Resources Investigations, Book 2, Chapter Dl, 116 p.
-20-