2 & 3 Dimensional Geo-Electrical Resistivity Imaging Survey Of The Subsurface Structure Of Capitol Gate Area Of University Of Benin Edo State Nigeria
2D and 3D resistivity imaging methods are simple, fast, inexpensive, and relatively accurate techniques used in geophysical exploration. In this study, 2D and 3D resistivity imaging methods were used to produce images of the subsurface structure of the capitol gate area of the University of Benin, Edo state Nigeria where orthogonal set of 2D geo-electrical resistivity field data were collected using the conventional Wenner array configuration. The observed 2D apparent resistivity data were processed and then collated into 3D data set which was processed using a 3D inversion code. The 3D model resistivity images obtained from the inversion are presented in horizontal and vertical depth slices in contour and block images. This study was carried out to show the effectiveness of 3D geo-electrical resistivity imaging using parallel 2D profiles.
TABLE OF CONTENTS
Title Page —————————————————————————————-i
Table of Content ——————————————————————————-ii
List of Figures ———————————————————————————-v
List of Tables ———————————————————————————-vii
Abstract ————————————————————————————— xiii
1.1 Introduction ——————————————————————————-1
1.2 Location and Geology of The Study Area ——————————————-4
1.3 Resistivity Imaging Technique ——————————————————— 5
1.4 Electrical Properties Of Earth Materials ———————————————-7
1.5 Aims And Objectives Of Study ——————————————————-10
Literature Review —————————————————————————-11
3.1 Theory Of Geoelectrical Resistivity Survey —————————————-20
3.2 The General Four Electrode Configuration —————————————— 23
3.3 Electrode Configuration —————————————————————-28
3.3.1 Wenner Array ————————————————————————-28
3.3.2 Dipole-Dipole Array —————————————————————— 30
3.3.3 Schlumberger Spread —————————————————————-31
3.3.4 Wenner-Schlumberger Array ——————————————————-31
3.3.5 Pole-Pole Array ———————————————————————— 33
3.3.5 Pole-Dipole Array ——————————————————————— 34
3.4 2D Modelling Program —————————————————————-35
3.5 3D Modelling Program —————————————————————-37
3.5 3D Data Grid Format ——————————————————————-40
4.1 Result ————————————————————————————-43
4.1.1 2-D Werner Array Electrical Resistivity Field Record————————-43
4.1.2 2-D Imaging of the Survey Area —————————————————-49
4.1.3 3-D Imaging of the Survey Area —————————————————-52
4.2 Discussion of Result ——————————————————————-56
5.1 Conclusion ——————————————————————————-58
5.2 Recommendations ———————————————————————-58
The purpose of electrical surveys is to determine the subsurface resistivity distribution by making measurements on the ground surface. From these measurements, the true resistivity of the subsurface can be estimated. The ground resistivity is related to various geological parameters such as the mineral and fluid content, porosity and degree of water saturation in the rock. Electrical resistivity surveys have been used for many decades in hydrogeological, mining and geotechnical investigations. More recently, it has been used for environmental surveys.
The goal of geo-electrical resistivity surveys is to determine the distribution of subsurface resistivity by taking measurements of the potential difference on the ground surface. For a typical inhomogeneous subsurface, the true resistivity distribution is estimated by carrying out inversion on the observed apparent resistivity values. In environmental and engineering investigations, the subsurface geology is usually complex, subtle and multi-scale such that both lateral and vertical variations in the petrophysical properties can be very rapid. Two dimensional (2D) geo-electrical resistivity imaging has been widely used to map areas with moderately complex geology (Griffiths and Barker 1993; Griffiths et
al.1990; Dahlin and Loke 1998; Olayinka 1999; Olayinka and Yaramanci 1999; Amidu and Olayinka 2006). In the 2D model of interpretation, the subsurface resistivity is considered to vary both laterally and vertically along the survey line but constant in the perpendicular direction. The major limitation of the 2D geo-electrical resistivity imaging is that measurements made with large electrode spacing are often affected by the deeper sections of the subsurface as well as structures at a larger horizontal distance from the survey line. This is most pronounced when the survey line is placed near a steep contact with the line parallel to the contact (Loke 2001).
Geological structures and spatial distributions of sub-surface petrophysical properties and/or contaminants commonly encountered in environmental, hydrogeological and engineering investigations are inherently three dimensional (3D). Thus, the assumption of the 2D model of interpretation is commonly violated. Images resulting from 2D geo-electrical resistivity surveys can contain spurious features due to 3D effects. This usually leads to misinterpretation and/or misrepresentation of the observed anomalies in terms of magnitude and location; and the 2D images produced are only along the survey lines and not the entire investigation site. Thus, geometrically complex heterogeneities cannot be adequately characterized with vertical electrical sounding or 2D electrical resistivity imaging alone. Hence, a 3D geoelectrical resistivity survey with a 3D model of interpretation, where the resistivity values are allowed to vary in all the three directions, namely vertical, lateral and perpendicular directions, should in theory give a more accurate and reliable results.
In this research, measurements of the orthogonal 2D profiles were made using the conventional Wenner electrode configuration with the aid of an automatic electric imaging device, terrameter SAS 1000.
The observed orthogonal set of 2D apparent resistivity data were collated into 3D data set and then inverted using a 3D inversion code, RES3DINV (Loke and Barker 1996b ). The resistivity sounding was conducted to obtain 2D layering information which aids the interpretation of the 3D geo-electrical resistivity imaging. The survey was conducted, as part of experimental studies to determine the effectiveness of using parallel or orthogonal sets of 2D profiles to generate 3D data set in geo-electrical resistivity imaging, with the aim of determining the subsurface structures of the location of study.
1.2 LOCATION AND GEOLOGY OF THE STUDY AREA
Figure 1.1: A picture of the study area. (Source: Google-Earth)
This work was carried out at the capitol gate region of the University of Benin, Benin City, Edo State Nigeria. This area of study is overlain by different materials which range between loose sandy to very coarse sand. The color of the sediment in this area is brownish or blackish which is of the Benin formation that overlies the entire Niger delta basin.
The Agbada formation underlies the Benin formation and consists primarily of sand and shale. It is of fluviomarine origin. It is the main hydrocarbon-bearing window. A nearby formation, the Akata formation, is composed of shale, clays and silt at the base of the known sequence. They contain a few streaks of sand. The thickness of this sequence is not known for certain, but may reach 700m in the central part of the Delta.
1.3 RESISTIVITY IMAGING TECHNIQUE
Most surveys on modern electrical resistivity aim to obtain the true resistivity values of subsurface structures because true resistivity is geologically significant.
Resistivity imaging technique depends on Ohm‟s law, which states that the electric current (I) in a material is proportional to the potential difference across it. The linear relationship between these two variables is expressed by the following equation:
Where (I) is the current, (V) is the potential difference, and (R) is the resistance. The above equation is the linear relationship between (V) and (I). For a given material, resistance is proportional to length (L) and inversely proportional to the cross-sectional area (A) of the conductor. These relationships are expressed in the following equation:
The proportionality constant (ρ) is the resistivity of the conductor. Resistivity, a physical property of materials, is the ability to resist flow of charges. It is the measurement of how strongly a material resists the flow of electric current (Denchik and Chapellier, 2005). Ohm‟s Law states that, “For many materials (including most metals), the ratio of the current density to the electric field is a constant, σ, that is independent of the electric field producing the current” (Serway and Jewett, 2007)
The constant of proportionality (σ) is the conductivity of the material, (J) is the current density, and (E) is the electric field. The inverse of conductivity is resistivity (ρ)
For a homogeneous area with one electrode, the potential separates radially away from the current source, where the area (A) is a half sphere (2πr²) with radius (r). Equation (1.2) is rewritten as
ρ = R K (1.5)
Where K = 2πr for a half sphere. Equation 5 consists of two parts. The first part is resistance (R) and the second part is geometric factor (K), which describes the geometry of the electrode configuration.
The geological structures of the ground are inhomogeneous, and the obtained values of resistivity represent apparent resistivity instead of true resistivity (Lowrie, 2007; Reynolds, 1997). Therefore, the resistivity (ρ) in Equation (1.5) changes to apparent resistivity (ρa) in an inhomogeneous area:
ρa= R K (1.6)
Equation (1.6) is used to calculate apparent resistivity, which depends on the type of subsurface structure and the arrangement of current electrodes and voltage poles. True resistivity can be calculated from apparent resistivity with the use of RES2DINV, a commercial software that uses numerical methods to estimate true resistivity and plot a 2D or 3D image (Loke, 2011).
1.4 ELECTRICAL PROPERTIES OF EARTH MATERIALS
Electric current flows in earth materials at shallow depths through two main methods. They are electronic conduction and electrolytic conduction. In electronic conduction, the current flow is via free electrons, such as in metals. In electrolytic conduction, the current flow is via the movement of ions in groundwater. In
environmental and engineering surveys, electrolytic conduction is probably the more common mechanism. Electronic conduction is important when conductive minerals are present, such metal sulfides and graphite in mineral surveys. (Loke, 2013)
Resistivity surveys give a picture of the subsurface resistivity distribution. To convert the resistivity picture into a geological picture, some knowledge of typical resistivity values for different types of subsurface materials and the geology of the area surveyed, is important.
Table 1 shows the resistivity values of common rocks, soil materials and chemicals (Keller and Frischknecht 1966; Daniels and Alberty 1966).
Resistivity values have a much larger range compared to other physical quantities mapped by other geophysical methods. The resistivity of rocks and soils in a survey area can vary by several orders of magnitude. In comparison, density values used by gravity surveys usually change by less than a factor of 2, and seismic velocities usually do not change by more than a factor of 10. This makes the resistivity and other electrical or electromagnetic based methods very versatile geophysical techniques.
Table 1: Resistivity‟s of some common rocks, minerals and chemicals.
MATERIAL RESISTIVITY (Ωm) CONDUCTIVITY(Siemen/m) IGNEOUS AND METAMORPHIC ROCKS
Shale 20-2 5-0.05
Limestone 50-4 2.5-0.02
SOILS AND WATERS
Clay 1-100 0.01-1
Alluvium 10-800 1.25-0.1
Groundwater 10-100 0.01-0.1
Sea water 0.2 5
Iron 9.074 1.102
0.01M Potassium 0.708 1.413
0.01 M Sodium 0.843 1.185
0.01 M acetic acid 6.13 0.163
Xylene 6.998 1.429
1.5 AIMS AND OBJECTIVES OF STUDY
This study is aimed at using electrical resistivity data obtained from the capitol gate region of the University of Benin, Benin City in Edo state Nigeria to locate the subsurface geologic features underneath the ground. The specific objective of this study is to show the 3D geo-electrical resistivity imaging of the subsurface of the area under study.