by - usgs · 2011-01-14 · u.s. department of the interior u.s. geological survey...

U.S. DEPARTMENT OF THE INTERIOR U.S. GEOLOGICAL SURVEY

AUDIO-MAGNETOTELLURIC DATA COLLECTED IN THE BEATTY, NEVADA AREA

By

Jackie M. Williams

Denver, Colorado

Open-File Report 98-231

1998

This report is preliminary and has not been edited or reviewed for conformity with the U.S. Geological Survey editorial standards. Any use of trade names is for descriptive purposes only and does not imply endorsement by the U.S. Geological Survey.

AUDIO-MAGNETOTELLURIC DATA COLLECTED IN THE AREA OF BEATTY, NEVADA

Jackie M. Williams,U.S. Geological Survey

1997

INTRODUCTION

In the summer of 1997, electrical geophysical data was collected north of Beatty, Nevada. Audio-magnetotellurics (AMT) was the geophysical method used to collect 16 stations along two (2) profiles. The purpose of this data collection was to determine the depth to the alluvial basement, based upon the needs of the geologists requesting the data.

DATA

The data was collected using the MT-1 magnetotelluric system (equipment and computer programs) of ElectroMagnetic Instruments, Inc. This system employs simultaneous orthogonal electric field and magnetic field measurements along with a remote station of either an electrical or magnetic field. We used a local remote that was less than 100 meters from the main station setup. This remote station allows for remote-reference noise cancellation which helps prevent bias of the data from noise created by power lines, radio antenna, or other cultural frequencies. Also, a vertical magnetic coil was used to collect tipper data which allows us to better determine the electrical strike direction.

Data was collected over five (5) ranges of frequency bands. The frequency bands used were, 1-170 Hz, 79-580 Hz, 340-3550 Hz, 885-23370 Hz and 1170-5210 Hz (to collect additional data at the weakest frequencies, the dead band). AMT methods correspond with those used in magnetotelluric (MT) methods (Cagniard, 1953: Vozoff, 1991), but occur at higher frequencies than the lower frequencies of MT . AMT signals originate mainly from atmospheric disturbances and MT signals occur from ionospheric phenomena.

Please, note in the models, that there are gaps in the data at the high frequency end, this is the result of weak signals at some frequencies. Data has not been edited to produce smooth Bostick inversions, but has been edited to eliminate noisy data and repeated data at various frequencies.

Why Use AMT ?

Measurement of earth resistivities can be an effective means of mapping geologic structures because of the large variation in the electrical resistivity of rocks, and in many instances, can be used to determine whether the rocks are intrusive, volcanic, sedimentary, or metamorphic. Alteration and fault zones can also be mapped. The resistivity of geologic units is largely dependent upon their fluid content, porosity, fracturing, temperature, and conductive mineral

1

content (Keller and Frischknecht, 1966).

Unaltered, unfractured crystalline rocks are normally very resistive (typically 1,000 ohm-m or greater), whereas faults will show low resistivity (less tan 100 ohm-m) when they are comprised of rocks fractured enough to have hosted fluid transport. Marine sedimentary rocks and clay-rich alluvium are normally very conductive (a few ohm-m to tens of ohm-m). Metamorphic rocks, including gneiss, schist (non-graphitic), and marble are moderately to highly resistive (hundreds to thousands of ohm-m). Tables of electrical resistivity for a variety of rocks, minerals and geological environments may be found in Keller, 1987; Olheoft, 1980; and Palacky, 1987.

References

Cagniard,L., 1953, Basic theory of the magnetotelluic method: Geophysics, v. 18, no.3,p. 605-635.

EMI, ElectroMagnetic Instruments, Inc., MT-1 Magnetotelluric System Operation Manual, v.3.2.

Keller, G. V. and Frischknecht, F. C., 1966, Electrical methods in geophysical prospecting:Pergamno Press, New York, 517 p.

Keller, G. V., 1987, Rock and mineral properties, in Electromagnetic Methods in AppliedGeophysics - Theory: M. N. Nabighian, Ed., Society of Exploration Geophysicists, Tulsa,Oklahoma, vol. 1, p. 13-51.

Olheoft, G. R., 1980, Electrical properties of rocks, in Physical Properties of Rocks andMinerals: Y. S. Touloukian, W. R. Judd, and R. F. Roy, Eds., McGraw-Hill, New York, 257-330.

Palacky, G. J., 1987, Resistivity characteristics of geologic targets, in Electromagnetic Methodsin Applied Geophysics - Theory: M. N. Nabighian, Ed., Society of Exploration Geophysicists,Tulsa, Oklahoma, vol. 1, 53-129.

Vozoff, Keeva, 1991, The magnetotelluric method; in Electromagnetic methods in appliedgeophysics: Nabighian, M.N., ed., v. 2, Applications, Part B: Tulsa, Society of ExplorationGeophysicist, p. 641-711.

Appendix

AMT data are presented with nine (9) different plots per station. Bostick inversion for station 1 will be Fig. 1 a. The other plots are the Apparent Resistivity, Impedance Phase, Rotation Angle, Impedance Skew, Electrical Multiple Coherency, Tipper Magnitude, Tipper Strike, and Polar Plots proceeding as Figs. Ib, Ic, Id, etc., respectively.

Fig._a. Bostick inversions. Preliminary 1-dimensional inversion models computed using theapparent resistivity and impedance phase.

Fig._b. Apparent resistivity. The relationship of the time-varying magnetic fields and theelectrical fields across frequencies.

Fig._c. Impedance Phase. Represents the ratio of the electric field intensity to magnetic fieldintensity across frequencies.

Fig._d. Rotation angle. Angle between measurement direction and direction of electrical strike,using only the horizontal sensors in the computation.

Fig._e. Impedance Skew. A measurement of the degree of the multi-dimensional resistivitystructure. It should be near 0 for 1-dimensional resistivity structures but larger for 2 or 3-

dimensional structures, and very large for noisy data. Fig._f. E Multiple Coherency. A measure of how well the electrical field correlates with the

magnetic field. High coherency generally means low noise in the data. Fig._g. Tipper Magnitude. A measure of nearby vertical resistivity structure (s). Values close to

0 represents horizontal layering. Fig._h. Tipper Strike, Angle between measurement direction and direction of electrical strike.

Uses both the horizontal sensors and the vertical coil to give a less ambiguous rotation. Fig._i. Polar Plots. Angular variations in impedance. The simpler circular plots often denote 1-

dimensionality; plots that are peanut-shaped denote 2-dimensionality; plots that are four-leafclover shaped denote 3-dimensionality and more complex denote noise at that frequency.

Contour interval 50 meters

0 1 2 3 4 5km l

Figure 1. AMT station locations.

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by - usgs · 2011-01-14 · u.s. department of the interior u.s. geological survey...

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