Geophysical Studies in the Vicinity of Blue Mountain 

and Pumpernickel Valley near Winnemucca, NorthCentral Nevada

 

Open-File Report 2012–1207

U.S. Department of the Interior

U.S. Geological Survey
Cover: Blue Mountain, Nev. View southeastward. 
Geophysical Studies in the Vicinity of Blue Mountain 

and Pumpernickel Valley near Winnemucca, NorthCentral Nevada

By David A. Ponce

 

 

Open-File Report 2012–1207

 

 

 

U.S. Department of the Interior

U.S. Geological Survey
iv

U.S. Department of the Interior

KEN SALAZAR, Secretary

U.S. Geological Survey

Marcia K. McNutt, Director

U.S. Geological Survey, Reston, Virginia 2012

For more information on the USGS—the Federal source for science about the Earth, its natural 

and living resources, natural hazards, and the environment, visit http://www.usgs.gov or call 

1-888-ASK-USGS

For an overview of USGS information products, including maps, imagery, and publications, visit 

http://www.usgs.gov/pubprod

Suggested citation:

Ponce, D.A., 2012, Geophysical studies in the vicinity of Blue Mountain and 

Pumpernickel Valley near Winnemucca, north-central Nevada: U.S. Geological Survey 

Open-File Report 2012–1207, 14 p. 

Any use of trade, product, or firm names is for descriptive purposes only and does not imply 

endorsement by the U.S. Government.

Although this report is in the public domain, permission must be secured from the individual 

copyright owners to reproduce any copyrighted materials contained within this report.
v

Contents

Introduction ........................................................................................................................................................ 1

Gravity, Magnetic, and Physical-Property Data.......................................................................................... 1

 Gravity Data .................................................................................................................................................... 1

 Magnetic Data................................................................................................................................................ 2

 Physical-Property Data ................................................................................................................................ 3

Discussion .......................................................................................................................................................... 4

Acknowledgments ............................................................................................................................................ 5

References Cited............................................................................................................................................... 5

Appendix. Gravity Base Stations.................................................................................................................. 13

Figures

1. Index map ....................................................................................................................................................... 7

2. Locations of gravity and physical-property data. ................................................................................... 8

3. Isostatic gravity map .................................................................................................................................... 9

4. Aeromagnetic map. .................................................................................................................................... 10

5. Location of truck-towed magnetic profiles. ........................................................................................... 11

6. Truck-towed magnetic profiles. ............................................................................................................... 12 

 

Tables

1. Gravity data, format, and description of codes ...................................................... t1_gravity_data.xls

2. Truck-towed magnetic data................................................................................t2_truck_mag_data.xls 

3. Physical-property data, format, and rock types........................................t3_rock_property_data.xls 

4. Summary of selected physical property data by rock type.................................................................. 4 
vi

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Geophysical Studies in the Vicinity of Blue Mountain 

and Pumpernickel Valley near Winnemucca, NorthCentral Nevada

By David A. Ponce1

Introduction 

From May 2008 to September 2009, the U.S. Geological Survey (USGS) collected data from 

more than 660 gravity stations, 100 line-km of truck-towed magnetometer traverses, and 260 physicalproperty sites in the vicinity of Blue Mountain and Pumpernickel Valley, northern Nevada (fig. 1). 

Gravity, magnetic, and physical-property data were collected to study regional crustal structures as an 

aid to understanding the geologic framework of the Blue Mountain and Pumpernickel Valley areas, 

which in general, have implications for mineral- and geothermal-resource investigations throughout the 

Great Basin. 

Gravity, Magnetic, and Physical-Property Data

Gravity Data 

Gravity data, which were collected between May 2008 and September 2009, consist of records 

from more than 660 new stations concentrated in areas of sparse control, as well as along traverses of 

interest (fig. 2). All the gravity data were tied to a primary base station at the Winnemucca airport (WIN, 

Jablonski, 1974) and a secondary base station established at the Winnemucca courthouse (WINCH); 

both base stations are described in the appendix. Gravity stations were located between approximately 

lat 40°40’ and 41°30’ N. and long 117°00’ and 118°45’ W. and are distributed across parts of the Vya, 

McDermitt, Lovelock, and Winnemucca 1o x 2o (1:250,000 scale) USGS topographic-quadrangle maps. 

New gravity data were reduced by using standard methods (Blakely, 1995) and include the 

following corrections: (1) an earth-tide correction, which corrects for tidal effects of the Moon and Sun; 

(2) an instrument-drift correction, which compensates for drift in the instrument’s spring; (3) a latitude 

correction, which accounts for variation in the Earth’s gravity with latitude; (4) free-air correction, 

which accounts for the variation in gravity due to elevation relative to sea level; (5) a Bouguer 

correction, which corrects for the attraction of material between the station and sea level; (6) a curvature 

correction, which corrects the Bouguer correction for the effect of the Earth’s curvature; (7) a terrain 

correction, which removes the effect of topography to a radial distance of 167 km from the station; and 

(8) an isostatic correction, which removes long-wavelength variations in the gravity field related to the 

compensation of topographic loads. 

LaCoste and Romberg gravity meter G614 and a Scintrex CG-5 gravity meter were used in this

survey. Gravity meter readings were converted to gravity units for LaCoste and Romberg gravity meter 

G614 by using factory calibration constants, as well as a secondary calibration factor (1.00036) 

determined by multiple gravity readings over the Mount Hamilton calibration loop east of San Jose, 

Calif. (Barnes and others, 1969). For the Scintrex CG-5 gravity meter, the factory meter-calibration 

constant was also checked and redetermined over the Mount Hamilton calibration loop. Observed 

 

1

U.S. Geological Survey, 345 Middlefield Road, Menlo Park, CA 94025, ponce@usgs.gov, 

http://geomaps.wr.usgs.gov/gump/. 
2

gravity values were based on a time-dependent linear drift between successive base readings and 

referenced to the International Gravity Standardization Net 1971 (IGSN 71) gravity datum (Morelli, 

1974, p. 18). Free-air gravity anomalies were calculated by using the Geodetic Reference System 1967 

formula for theoretical gravity on the ellipsoid (International Union of Geodesy and Geophysics, 1971, 

p. 60) and Swick’s (1942, p. 65) formula for the free-air correction. Bouguer, curvature, and terrain 

corrections were added to the free-air anomaly to determine the complete Bouguer anomaly at a 

standard reduction density of 2,670 kg/m3

. Finally, a regional isostatic gravity field was removed from 

the Bouguer field by assuming an Airy-Heiskanen model for isostatic compensation of topographic 

loads (Jachens and Roberts, 1981), with an assumed nominal sea-level crustal thickness of 25 km, a 

crustal density of 2,670 kg/m3, and a density contrast across the base of the crust of 400 kg/m3. Gravity 

values are expressed in milligal (mGal), a unit of acceleration or gravitational force per mass equal to 

10-5 m/s2. 

Station locations and elevations were obtained by using a Trimble GeoXH differential Global 

Positioning System (GPS) instrument. The GeoXH receiver uses the Wide Area Augmentation System 

(WAAS) which, in combination with a base station and postprocessing with a Continually Operated 

Reference Station (CORS), results in submeter vertical accuracy. 

Terrain corrections, which account for the variation in topography near a gravity station, were 

calculated using a combination of manual and digital methods. Terrain corrections consist of a three-part 

process: an innermost or field-terrain correction, an innerzone-terrain correction, and an outerzoneterrain correction. The innermost-terrain correction, which was estimated in the field, extends from the 

station to a radial distance of 68 m and is equivalent to the outer radius of Hayford and Bowie’s (1912) 

zone B. The innerzone-terrain correction, which was estimated from a digital elevation model (DEM) 

with 10- or 30-m resolution derived from USGS 7.5’ topographic maps, extends from 68 m to a radial 

distance of 2 km (D. Plouff, unpub. data, 2006). The outerzone-terrain correction, which was calculated 

by using a DEM derived from USGS 1:250,000-scale topographic maps and an automated procedure 

based on geographic coordinates (Plouff, 1966; Plouff, 1977; Godson and Plouff, 1988), extends from 2 

km to a radial distance of 167 km. Digital terrain corrections were calculated by computing the gravity 

effect of each grid cell in the DEM, using the distance and difference in elevation of each grid cell from 

the gravity station. 

New gravity data were combined with preexisting gravity data (Ponce, 1997) from the 

surrounding area in Nevada (fig. 2). All gravity data were gridded by using a minimum curvature 

algorithm at an interval of 500 m and displayed on a color-contoured isostatic gravity map (fig. 3). 

Observed gravity values are accurate to about 0.05 mGal, and calculated gravity anomalies to about 0.5 

mGal. Principal facts of new gravity data are listed in table 1 in an Excel workbook. 

Magnetic Data

Aeromagnetic Data 

Aeromagnetic data were derived from a State-wide compilation for Nevada (Kucks and others, 

2006) and displayed with a 0.5-km grid on a color-contoured aeromagnetic map (fig. 4). The 

aeromagnetic data for the state of Nevada were compiled and adjusted by Kucks and others (2006) for 

diurnal variations in the Earth’s magnetic field, either upward or downward continued, if necessary, to a 

flightline elevation of 305 m above the ground, leveled, adjusted to a common datum, and merged to 

produce a uniform map that allows interpretations across survey boundaries. 

In general, the aeromagnetic data in the study area (fig. 4) are of poor to fair resolution. Most 

coverage of the study area consists of surveys flown at a high barometric elevation of 2,700 m, with 

flightlines oriented east-west and spaced 1.6 to 3.2 km apart. Although the flightline spacing and, in 

general, high flightline elevation of some of these original surveys used in the State-wide compilation 
3

may not resolve some magnetic sources lying at shallow depths beneath the surface, the effect is 

negligible at the scale of our investigations. 

Truck-Towed Magnetic Data 

About 100 line-km of truck-towed magnetometer data (figs. 5,6) was collected along Jungo Road 

(line 1, fig. 5) and selected traverses on the west side of Blue Mountain, a known gold deposit and 

geothermal area (fig. 5). Magnetic and GPS data were collected simultaneously at 1-s intervals, using a 

GeometricsG858 Ce-vapor magnetometer attached to an aluminum carriage connected to the vehicle by 

aluminum tubing and towed about 9 m behind the vehicle. The height of the magnetometer above the 

ground surface was about 2 m. A portable GeometricsG856 proton-precession base-station 

magnetometer located just south of Blue Mountain was used to record diurnal variations in the Earth’s 

magnetic field during the truck-towed magnetometer surveys. 

During field operations, truck-towed magnetic data were recorded and viewed in real time, using 

GeometricsMagLog software. Raw magnetic data were downloaded and processed by using Geometrics

MagMap2000 software, where magnetometer and GPS data were merged. The location of the 

magnetometer was recorded by using a Trimble nonmagnetic Ag132 GPS receiver mounted on an 

aluminum frame attached to the magnetometer. The receiver has real-time differential-correction 

capabilities with an Omnistar satellite system, resulting in submeter horizontal accuracy. Diurnal 

variations recorded by the base-station magnetometer were removed, and the data were edited to remove 

cultural “noise”, such as passing cars, culverts, fences, and powerlines. The locations of truck-towed 

magnetic traverses are shown in figure 5, magnetic profiles are plotted in figure 6, and the data are listed 

in table 2 in an Excel workbook. In general, the accuracy of the magnetometer is about 1 nanoteslas 

(nT). The data are presented as geographic coordinates (NAD83 datum) and magnetic-field values 

(in nT). 

Physical-Property Data

Rock samples were collected from outcrops throughout the study area and from two cores from 

drillholes DB-1 and DB-2 at Blue Mountain. Drill-hole data were previously reported by Ponce and 

others (2009). Additional data are listed in table 3, in an Excel workbook, and a summary of selected 

density and magnetic susceptibility measurements by rock type is listed in table 4. Digital data include 

station identifier, geographic coordinates (NAD27), rock type, density, and magnetic susceptibility. 

Densities were determined by the buoyancy method, and weights were measured on an electronic 

balance with an accuracy of ±0.01 g. Magnetic susceptibility was measured with a Kappameter model 

KT-5 with an accuracy of 0.01 x10-3 SI unit. Grain, saturated-bulk, and dry-bulk densities were 

calculated for each sample by weighing the sample in air (Wa), saturated and submerged in water (Ww), 

and saturated and weighed in air (Was), using the following formulas, where all weights are measured in 

grams:

Grain density = 1,000 kg/m3

 * Wa/(Wa-Ww),

Saturated-bulk density = 1,000 kg/m3

 * Was/(Was-Ww), and 

Dry-bulk density = 1,000 kg/m3 * Wa/(Was-Ww). 
4

Discussion

In general, once gravity data are reduced to isostatic gravity anomalies, they reflect lateral 

density variations in the mid to upper crust. Thus, gravity anomalies can be used to infer the subsurface 

structure of known or unknown geologic features provided a density contrast occurs across the geologic 

boundaries. Gravity anomalies can, for example, reveal variations in lithology and delineate such 

features as calderas, deep sedimentary basins, and faults, all of which play an important role in defining 

the geologic framework of a given area.

An isostatic gravity map of the study area (fig. 3) is dominated by a series of gravity highs and 

lows that generally reflect dense pre-Cenozoic outcrops and low-density basin fill, respectively. The 

gravity highs that occur over Blue Mountain, the Slumbering Hills, the Bloody Run Hills, the Eugene 

Mountains, and the East Range reflect relatively denser Paleozoic rocks and Triassic to Jurassic 

metasedimentary rocks. Relatively lower-amplitude gravity highs over parts of the Slumbering Hills and 

the Bloody Run Hills probably reflect lower-density plutonic rocks that compose the central parts of the 

ranges and extend to some depth (figs. 1,2). The lowest gravity values reflect moderately deep 

sedimentary basins in Desert, Silver State, Grass, Paradise, and Pumpernickel Valleys. On the basis of 

the amplitudes of these gravity lows, these basins reach depths of about 2 km, which is typical of most 

basins in Nevada. 

Magnetic anomalies, which reflect changes in the Earth’s magnetic field are generally used to 

infer lateral variations in rock magnetization. In general, the magnetic anomalies observed throughout 

the study area (fig. 1) are explainable by variations in exposed rock types and their magnetic properties. 

Short-wavelength, high-amplitude magnetic anomalies are generally caused by volcanic rocks that are 

moderately to strongly magnetic. Owing to the dipolar nature of magnetic sources, magnetic highs (or 

lows) are typically accompanied by an associated magnetic low (or high), whereas isolated magnetic 

lows, may be associated with altered volcanic rocks or weakly magnetic silicic and sedimentary rocks. 

The aeromagnetic map of the study area (fig. 4) is dominated by broad, long-wavelength, highamplitude anomalies associated with moderately magnetic plutonic rocks mapped throughout the area 

(Stewart and Carlson, 1978). High-amplitude, short-wavelength anomalies, such as in the northwest 

corner of the map, are associated with volcanic rocks. Magnetic anomalies are particularly useful for 

delineating the subsurface extent of plutonic rocks because plutons are commonly more magnetic than 

the basement rocks they intrude. For example, the pluton in the central block of the Slumbering Hills 

Table 4. Summary of selected physical-property data by rock type.

Rock Number Grain Saturated- Dry-bulk Magnetic

type of density bulk density density susceptibility

samples kg/m3 kg/m3 kg/m3 x10-3 SI

Granitic Rocks

 Granite 6 2658 2624 - 2683 2627 2548 - 2664 2608 2501 - 2653 5.20 0.15 - 9.75

 Granodiorite 83 2670 2560 - 2777 2629 2527 - 2757 2604 2475 - 2745 4.80 0.11 - 14.6

 Diorite 82 2814 2613 - 2930 2777 2566 - 2913 2756 2495 - 2905 9.54 0.10 - 28.4

 Gabbro 3 2871 2866 - 2878 2860 2855 - 2863 2854 2850 - 2858 8.28 6.39 - 10.5

Volcanic Rocks

 Basalt 2 2496 2496 - 2497 2420 2401 - 2440 2369 2336 - 2402 1.94 1.87 - 2.0

 Tuff 5 2608 2572 - 2643 2512 2437 - 2589 2452 2351 - 2565 0.06 0.04 - 0.09

Sedimentary Rocks

 Argillite 4 2705 2655 - 2766 2668 2628 - 2709 2647 2610 - 2676 0.08 0.01 - 0.17

 Mudstone 7 2645 2522 - 2733 2610 2454 - 2717 2588 2409 - 2708 0.11 0.05 - 0.21

 Metasediment 13 2721 2602 - 2923 2688 2563 - 2906 2668 2537 - 2897 0.19 0.02 - 0.42

 Slate 5 2708 2661 - 2782 2647 2560 - 2725 2611 2499 - 2694 0.10 0.07 - 0.18

Range Range Range Range
5

may extend well beyond the range and beneath Desert Valley. In addition to these features, the 

prominent arcuate aeromagnetic anomalies referred to as the western and central Northern Nevada Rifts 

(NNRW, NNRC, figs. 1,4), that are similar to the Northern Nevada Rift (NNRE; inset, fig. 1) east of 

Winnemucca, reflect crustal-scale mafic-dike intrusions that occurred during the inception of the 

Yellowstone Hotspot (Zoback and others, 1994; Ponce and Glen, 2002). Indeed, the mafic dike swarm 

along the west flank of Blue Mountain (Wyld, 2002; Ponce and others, 2010), with its associated 

aeromagnetic anomaly and its better defined truck-borne magnetic anomaly (figs. 4-6), is the surface 

manifestation of one of these rift zones. 

The diverse physical properties of the rocks that underlie the study area (fig. 1) are well suited to 

geophysical investigations. The contrasts in density and magnetic properties between pre-Cenozoic 

crystalline basement and the overlying Tertiary volcanic rocks and unconsolidated alluvium, for 

example, produce a distinctive pattern of gravity and magnetic anomalies that can be used to infer 

subsurface geologic structure and aid in understanding the geologic framework and geothermal potential 

of northern Nevada. 

Acknowledgments

We thank Bob Morin and Janet Watt for their assistance in collecting or processing gravity, 

truck-towed magnetic, and physical property data. We thank Nevada Geothermal Power for granting 

access to their properties and especially John Casteel and Kim Niggeman who helped facilitate our 

efforts. We also thank Bruce Chuchel and Vicki Langenheim of the USGS for their reviews and George 

Havach and Carolyn Donlin for editing the report. 

References Cited 

Barnes, D.F., Oliver, H.W., and Robbins, S.L., 1969, Standardization of gravimeter calibrations in the 

Geological Survey: Eos, American Geophysical Union Transactions, v. 50, no. 10, p. 626–627. 

Blakely, R.J., 1995, Potential theory in gravity and magnetic applications: New York, Cambridge 

University Press, 441 p. 

Godson, R.H., and Plouff, D., 1988, BOUGUER version 1.0, a microcomputer gravity-terrain-correction 

program: U.S. Geological Survey Open-File Report 88-644-A, 22 p. 

[http://pubs.er.usgs.gov/publication/ofr88644A accessed October 10, 2012] 

Hayford, J.F., and Bowie, W., 1912, The effect of topography and isostatic compensation upon the 

intensity of gravity: U.S. Coast and Geodetic Survey Special Publication 10, 132 p. 

International Union of Geodesy and Geophysics, 1971, Geodetic reference system 1967: International 

Association of Geodesy Special Publication 3, 116 p. 

Jablonski, H.M., 1974, World relative gravity reference network North America, Parts 1 and 2, with a 

supplementary section on IGSN 71 gravity datum values (rev. ed.): U.S. Defense Mapping 

Agency Aerospace Center Reference Publication 25, 1261 p. 

Jachens, R.C., and Roberts, C.W., 1981, Documentation of a FORTRAN program, ‘isocomp’, for 

computing isostatic residual gravity: U.S. Geological Open-File Report 81-574, 26 p. 

[http://pubs.er.usgs.gov/publication/ofr81574, accessed October 10, 2012]. 

Kucks, R.P., Hill, P.L., and Ponce, D.A., 2006, Nevada magnetic and gravity maps and data—a website 

for the distribution of data: U.S. Geological Survey Data Series 234

[http://pubs.usgs.gov/ds/2006/234, accessed April 13, 2012].

Morelli, C., ed., 1974, The International Gravity Standardization Net 1971: International Association of 

Geodesy Special Publication 4, 194 p. 

Plouff, D., 1966, Digital terrain corrections based on geographic coordinates [abs.]: Geophysics, v. 31, 

no. 6, p. 1208. 
6

Plouff, D., 1977, Preliminary documentation for a FORTRAN program to compute gravity terrain 

corrections based on topography digitized on a geographic grid: U.S. Geological Survey OpenFile Report 77-535, 45 p. [http://pubs.er.usgs.gov/publication/ofr77535, accessed October 10, 

2012]. 

Ponce, D.A., 1997, Gravity data of Nevada: U.S. Geological Survey Digital Data Series DDS-42, 27 p., 

CD-ROM. [http://pubs.usgs.gov/dds/dds-42/, accessed October 10, 2012]. 

Ponce, D.A., and Glen, J.M.G, 2002, Relationship of epithermal gold deposits to large-scale fractures in 

northern Nevada: Economic Geology, v. 97, no. 1, p. 3–9. 

Ponce, D.A., Glen, J.M.G., Watt, J.T., and Casteel, J., 2010, Geophysical setting of the Blue Mountain 

geothermal area, north-central Nevada and its relationship to a crustal-scale fracture associated 

with the inception of the Yellowstone Hotspot: Geothermal Resources Council Transactions, v. 

34, p. 881–885. 

Ponce, D.A., Watt, J.T., Casteel, J., and Logsdon, G., 2009, Physical-property measurements on core 

samples from drill-holes DB-1 and DB-2, Blue Mountain geothermal prospect, north-central 

Nevada: U.S. Geological Survey Open-File Report 2009-1022, 18 p. 

[http://pubs.usgs.gov/of/2009/1022/, accessed October 10, 2012]. 

Swick, C.A., 1942, Pendulum gravity measurements and isostatic reductions: U.S. Coast and Geodetic 

Survey Special Publication 232, 82 p. 

Stewart, J.H., and Carlson, J.E., 1978, Geologic map of Nevada: U.S. Geological Survey and Nevada 

Bureau of Mines and Geology, scale 1:500,000. 

Wyld, S.J., 2002, Structural evolution of a Mesozoic backarc fold-and-thrust belt in the U.S. Cordillera; 

new evidence from northern Nevada: Geological Society of America Bulletin, v. 114, no. 11, p. 

1452-1468. 

Zoback, M.L., McKee, E.H., Blakely, R.J., and Thompson, G.A., 1994, The northern Nevada rift; 

regional tectono-magmatic relations and middle Miocene stress direction: Geological Society of 

America Bulletin, v. 106, p. 371-382. 
7

Figure 1. Index and simplified geologic map of Winnemucca and vicinity (from Stewart and 

Carlson, 1978). The stock mapped in the western part of Blue Mountain is now considered 

to be a mafic dike swarm (Wyld, 2002; Ponce and others, 2010). DB-1, DB-2, drill holes on 

west side of Blue Mountain; NNRW, NNRC, NNRE, western, central, and eastern Northern 

Nevada Rifts (Ponce and Glen, 2002); WIN, Winnemucca. Geology: yellow, Quaternary 

alluvium (Qa); pink, Tertiary volcanic rocks (Tv); orange, Tertiary basalt (Tb); red, 

undivided granitic plutons (gr); forest green, Triassic metasediments (Trs); green, Triassic

volcanic rocks (Trv); purple, undivided Paleozoic rocks (Pz); brown, Cambrian rocks (Cu).
8

Figure 2. Locations of gravity and physical property data in the study area. Red circles, 

gravity stations collected during this study; gray circles, pre-existing gravity stations 

(Ponce, 1997); blue triangles, physical property locations. See figure 1 for explanation. 
9

 Figure 3. Isostatic gravity map of the study area. See figures 1 and 2 for explanation.

 
10

 Figure 4. Aeromagnetic map of the study area showing location of NNR’s and mafic dike 

swarm at Blue Mountain. See figure 1 for explanation.
11

 Figure 5. Location of truck-towed magnetic traverses 1 through 10 (black lines) near Blue 

Mountain and their magnetic anomalies. See figure 1 for explanation.
12

 Figure 6. Truck-towed magnetic profiles near Blue Mountain. Vertical scale is the same for all profiles. 

Horizontal scales are the same, except for Line 1 which is at 1/3 the scale. Profiles are from west to east, 

except for Lines 5 and 8 which are from north to south.
13

Appendix. Gravity Base Stations
14