scholarly journals Determination of the resistivity anisotropy of orthorhombic materials via transverse resistivity measurements

2017 ◽  
Vol 88 (4) ◽  
pp. 043901 ◽  
Author(s):  
P. Walmsley ◽  
I. R. Fisher
Keyword(s):  
Resistivity Measurements ◽  
Resistivity Anisotropy ◽  
Orthorhombic Materials

Determination of Intrinsic Dip and Azimuth From LWD Azimuthal-Propagation Resistivity Measurements in Anisotropic Formations

2010 ◽  
Vol 13 (04) ◽  
pp. 667-678 ◽  
Author(s):  
S.. Fang ◽  
A.. Merchant ◽  
E.. Hart ◽  
A.. Kirkwood
Keyword(s):  
Boundary Effects ◽  
Minimum Amount ◽  
Resistivity Measurements ◽  
Resistivity Anisotropy ◽  
Main Components

Summary With the use of both azimuthal-propagation-resistivity (APR) and main- and cross-component data, the resistivity anisotropy and its dip and azimuth angles of a massive formation (anisotropic shale or laminated sand) can be determined. The accuracy of the determined parameters depends on the amount of available data. The minimum amount of data required is two frequency main components and real and quadrature cross components. The boundary effects will distort the solution eventually; however, the anisotropy-enhanced processing will minimize the effects to extend the algorithm to a certain distance away from a boundary.

scholarly journals Determination of the Activation Energy of Polar Firn by D.C. Resistivity Measurements

1967 ◽  
Vol 6 (48) ◽  
pp. 911-915 ◽  
Author(s):  
M. P. Hochstein ◽  
G. F. Risk
Keyword(s):  
Activation Energy ◽  
Resistivity Measurements ◽  
Temperature Range

The activation energy ϵe1 of polar firn samples determined by D.C. resistivity measurements is a function of temperature and density. In the temperature range −2° C. to −10° C. ϵe1 decreases with decreasing temperature reaching a nearly constant value for temperatures colder than −10°C.; in the temperature range −10°C. to −21°C. ϵe1 was found to decrease with increasing density and to lie between 0.7 eV. and 0.4 eV.

scholarly journals Determination of the Activation Energy of Polar Firn by D.C. Resistivity Measurements

1967 ◽  
Vol 6 (48) ◽  
pp. 911-915 ◽  
Author(s):  
M. P. Hochstein ◽  
G. F. Risk
Keyword(s):  
Activation Energy ◽  
Resistivity Measurements ◽  
Temperature Range

The activation energyϵe1of polar firn samples determined by D.C. resistivity measurements is a function of temperature and density. In the temperature range −2° C. to −10° C.ϵe1decreases with decreasing temperature reaching a nearly constant value for temperatures colder than −10°C.; in the temperature range −10°C. to −21°C.ϵe1was found to decrease with increasing density and to lie between 0.7 eV. and 0.4 eV.

scholarly journals Determination of the resistivity anisotropy ofSrRuO3by measuring the planar Hall effect

2007 ◽  
Vol 75 (12) ◽  
Author(s):  
Isaschar Genish ◽  
Lior Klein ◽  
James W. Reiner ◽  
M. R. Beasley
Keyword(s):  
Hall Effect ◽  
Planar Hall Effect ◽  
Resistivity Anisotropy

A method to determine the magnetotelluric static shift from DC resistivity measurements in practice

Geophysics ◽  
2010 ◽  
Vol 75 (1) ◽  
pp. F23-F32 ◽  
Author(s):  
Simona Tripaldi ◽  
Agata Siniscalchi ◽  
Klaus Spitzer
Keyword(s):  
Electrode Spacing ◽  
Impedance Tensor ◽  
Static Shift ◽  
Data Set ◽  
Resistivity Measurements ◽  
Electromagnetic Methods ◽  
Strike Direction ◽  
Distortion Matrix ◽  
Source Electrode

Many efforts have been made to face magnetotelluric (MT) static shift. Impedance tensor analyses give insight to the presence of this feature and allow the determination of some parameters described by the MT distortion matrix. A quantitative determination of the full distortion matrix is, however, still difficult and needs additional measurements. In addition to MT, other electric and electromagnetic methods also are effected by static shift. Using direct current resistivity techniques, e.g., we can determine the static-shift factors in a simpler way because the sources can be controlled. Generally, because the distortion matrix has four entries, four additional quantities have to be determined to describe the static shift completely. They can be achieved, e.g., through measuring two orthogonal electric field components for two orthogonal source configurations. The source electrode spacing, however, has to be sufficiently large to resemble horizontal currents and match the MT plane-wave analog. The procedure at hand extracts the static-shift factors from multielectrode measurements after this condition is met. For the sake of simplicity and demonstration purposes, only inline measurements orthogonal to the strike direction of a 2D model are considered so that the vectorial problem reduces to a scalar one. This procedure is applied to a MT field data set in a regional 2D environment that shows only two additional quantities are necessary to determine the static shift.

The Effect of Glacial Cross-Section on Vertical Resistivity Depth Soundings

1973 ◽  
Vol 12 (66) ◽  
pp. 375-382
Author(s):  
R. W. Taylor ◽  
R. J. Greenfield
Keyword(s):  
Cross Section ◽  
Field Data ◽  
Apparent Resistivity ◽  
Ice Thickness ◽  
Master Curves ◽  
Glacial Ice ◽  
Resistivity Measurements ◽  
Oriented Parallel ◽  
Wenner Array

The determination of glacial ice thickness by vertical resistivity depth soundings relies upon the use of theoretical curves which neglect the effect of valley walls. To improve the utility of glacial resistivity measurements an analytical expression is derived for the apparent resistivity determined by a Wenner array oriented parallel to the strike of a layered trough embedded in a perfectly conducting half space. Numerical evaluation of this expression allows the effects of glacial cross-section to be determined. It is shown that the presence of valley walls and layering within the glacier can strongly effect the determination of total ice thickness, and a criterion for the reliable use of plane-layered master curves in the interpretation of field data is established. An apparent resistivity curve calculated for a layered trough is shown to give an excellent fit to field data published by Röthlisberger and Vögtli (1967).

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