Obtaining Chemical Properties through Soil Electrical Resistivity

The electrical resistivity of soil is significantly influenced by shape of the particle of soil, presence of moisture in soil, chemical properties of soil and presence of organic materials in soil. Chemical p roperties of soil such as Soil pH, Cation exchange capacity (CEC), soil salinity can be efficiently determined by electrical resistivity of soil. The basic principal of obtaining chemical resistivity of soil through electrical resistivity is either to measure the current that flows between the probes which is inversely proportional to the resistance of the soil when a constant voltage is applied to one of the two probes placed in the soil o r to d irectly measure the electrical resistivity using electromagnetic waves of different frequencies into soils. For this purpose methods of selfpotential (SP), four electrode probe method, electrical p rofiling (EP), vertical electrical sounding (VES), and non-contact electromagnetic profiling (NEP) was used to measure the electrical properties of soil.


Introduction
Determination of soil chemical properties is very essential for both construction and agricultural purpose. To adequately characterize different types of soil for foundation of structures it is necessary to accumulate sufficient data regarding soil chemica l properties. Conventional methods of soil analysis mostly require disturbing soil, removing soil samples, and analysing them in a laboratory. Electrical geophysical methods, such as self-potential (SP), four electrode probe method, electrical profiling ( EP), vertical electrical sounding (VES), and non-contact electromagnetic profiling (NEP) allow rapid measurement of soil electrical properties, such as electrical conductivity, resistivity directly fro m soil surface to any depth without soil disturbance.

pH
Soil p H is known as "soil reaction" it indicates of the acidity or alkalin ity of soil. pH of water effects on the ion solubility of soil, which d irectly affect the microb ial and plant growth. The typical range of ph for soil is 4.0-9.0 but 6.0-6.8 is ideal for most of the crops because it is the pH

Electrical Resistivity of Soil
Soil resistivity is a crit ical factor in design of systems that measure of how much the soil resists the flow of electricity. Depending on moisture, temperature and chemical content the soil resistivity value can vary within wide ranges .Typical values are: 1). Usual values: fro m 10 up to 1000 (Ω m) 2). Exceptional values: fro m 1 up to 10000 (Ω m) Electrical resistivity of soil may be made with low frequency alternating current in which the current is applied at two locations, and the potential d ifference is measured between two points where the term potential d ifference, as used in physics, means voltage difference. Along this same method, a direct cu rrent may be applied in lieu of an alternating current thus causing an induced polarizat ion in subsurface features wherein, the operator times how long the potential d ifference lasts after the current is removed for the purpose of identify ing large subsurface conductors. These aforementioned means are considered active as the operator is inducing a current into the ground for the purpose of measuring a potential difference. The resistivity of soil varies widely throughout the world and changes dramat ically within s mall areas. Soil resistivity is mainly influenced by the type of soil (clay, shale, etc.), moisture content, the amount of electrolytes (minerals and dissolved salts) and finally, temperature.

Basic Formul as for Measuring the Electrical Resistivity of Soil
There are four basic formulas emp loyed when discussing electrical resistivity and these are current, current density , Oh m"s law, and resistivity. Current is determined by charge in colu mbs over a given period of time in seconds where current is represented as I, colu mbs in q, and time as t.
(1) Current density is the amount of current flowing through a particular area in wh ich the current density is represented by a j, and the area is represented by an A.
Oh ms law is the relation of voltage, resistance, and current. This was first presented by the German physicist Georg S. Oh m. In this formu la the term V represents voltage and R represents resistance. (3) Resistivity is the relation of resistance, area, and current and is written as:

Suitable Location for Testing Electrical Resistivity of Soil
Soil electrical resistivity testing should be conducted as close to the proposed grounding system as possible, taking into consideration the physical items that may cause erroneous readings. There are two issues that may cause poor quality readings: 1). Electrical interference causing unwanted signal noise to enter the meter.
2). Metallic objects "short-cutting" the electrical path fro m probe to probe. The rule of thumb here is that a clearance equal to the pin spacing should be maintained between the measurement traverse and any parallel buried metallic structures.
Testing in the vicinity of the site in question is obviously important; however, it is not always practical. Many electric utility co mpanies have rules regard ing how close the soil resistivity test must be in order to be valid. The geology of the area also plays into the equation as dramat ically different soil conditions may exist only a short distance away.
When left will little roo m or poor conditions in which to conduct a proper soil resistivity test, one should use the closest available open field with as similar geological soil conditions as possible.

Methods
For obtaining chemical properties of soil using electrical resistivity, few processes can be effectively used. They are: 1). Self-potential (SP) 2). Four-electrode probe method 3). Vertical electrical sounding (VES) 4). Electrical profiling (EP) 5). Non-contact electro magnetic profiling Vertical electrical sounding (VES) and electrical p rofiling (EP) methods measure electrical resistivity or conductivity of soil to any depth when a constant electrical field is artificially created on the surface. VES and EP methods as well as laboratory method of measuring electrical resistivity in soil samples are based on four-electrode principle, but vary considerably in electrode array lengths and arrangements, wh ich makes the methods suitable for different applicat ions. The VES, EP, and SP methods evaluate parameters of the stationary electrical fields in soils. All the methods of stationary electrical fields require grounding electrodes on the soil surface; therefore, measurements with these methods can be made only in agricultural fields, rural areas, or in the laboratory in soil samples. Electro magnetic induction methods (EM), non-contacted electromagnetic profiling (NEP), and ground penetrating radar (GPR) introduce electro magnetic waves of different frequencies into soils. The EM, NEP, and GPR evaluate properties of the non-stationary electromagnetic fields in soils. All the methods of non-stationary electro magnetic fields are mobile. The methods do not require a physical contact with the soil surface and can measure electrical resistivity or conductivity in soils covered with firm pavement. The NEP method, which we used in this study, has been specifically designed in Russia for shallow-subsurface environmental studies [2].

Self-Potenti al Method (SP)
Method of self-potential (SP) measures the naturally existing stationary electrical potentials in the soil. It is based on measuring the natural potential differences, which generally exist between any two points on the ground. These potentials are associated with electrical currents in the soil. In our study we are especially interested in the measurement of electrical potentials created in soils due to soil-forming process and water/ion movements. The electrical potentials in soils, clays, marls, and other water saturated and unsaturated sediments can be explained by such phenomena as ionic layers, electro-filtration, pH differences, and electro-osmosis. The soil-forming processes can create electrically variab le horizons in soil profiles. Another possible environ mental and engineering application of self-potential method is to study subsurface water movement [3]. The SP method utilizes t wo electrodes (trailing and leading), a potentiometer, and connecting wire. Two measuring techniques, fixed-base (or total field) and gradient (or leapfrog), are suggested in conventional geophysics. We used the fixed-base technique to obtain distributions of electrical potentials in soil profiles. Measurements were conducted on the walls of open soil p its. The base or trailing electrode was permanently installed in the place of high potential, usually in alluvial, wet, fine-textured, o r salty soil horizon. To obtain maps of electrical potential the gradient technique was imp lied. The usage of non-polarizing electrodes is mandatory when the SP method is applied in soil and environmental studies. The non-polarizing electrode consists of a metal element immersed in a solution of salt of the same metal with a porous memb rane between the solution and the soil (Corwin and Butler, 1989). Because of easy breakage of the memb rane and leakage o f the electrode solution we adopted firm non-polarizing electrodes (carbon cores from the exhausted electrical cells.

Four-Electrode Probe Method
All the electrical resistivity methods applied in geophysics and soil science are based on the standard four-electrode principle suggested by Wenner in 1915 to min imize soil-electrode contact problems. The four-electrode princip le is illustrated in the laboratory conductivity cell (Figure 1). The cell is a rectangular plasticbo x with the current electrodes A and B as brass plates on the smaller sides. The potential electrodes M and N are the brass rods in the middle of the long side of the cell. A cons tant current (I) is applied to the two outer electrodes (A and B) and the arising difference of potential (Δu) is measured between the two inner electrodes (M and N). The electrical resistivity (ER) is calculated fro m the Oh m"s law as, where K is a geo metrical factor (m) depending on the distance among electrodes, ΔU is difference of potentials (mV), and I is magnitude of current (mA). The geometrical factor for a cell is obtained from the calibration solutions of a known resistivity (conductivity). The sample of soil paste or suspension is placed in a cell to measure electrical resistivity fro m the readings of voltage and current. The cell construction shown in Figure 1 ensures the induction of static uniform electrical field in the cell. The field is imposed on the homogeneous soil samp le to measure an accurate electrical resistivity of a sample. The time variat ion and the difference in electrical resistivity are less than 0.5% when measured in the same soil samp le by the cells with different distances between electrodes. The measurements in four-electrode laboratory cell were utilized to develop the relationships between various soil properties and electrical resistivity. There is another process for obtaining ER of soil where four electrode probes are used but in different configuration.

Figure 2.
Schematic showing the electrical resistivity method with an array of four electrodes: two current electrodes (c1 and c2) and two potential electrodes (p1 and p2) modified from Rhoades and Halvorson 1977 [6]. when electrodes are equally spaced at distance a, as shown, the electrode array is called a Wenner array Frank Wenner in the United States for the evaluation of ground ER [4]. The electrode configuration is referred to as a Wenner array when four electrodes are equidistantly spaced in a straight line at the soil s urface with the t wo outer electrodes serving as the current or transmission electrodes and the two inner electrodes serving as the potential or receiving electrodes ( Fig. 2; [5]). The depth of penetration of the electrical current and the volu me o f measurement increase as the inter-electrode spacing, a, increases. For a homogeneous soil, the soil volu me measured is roughly πa3.
Electrical resistivity and EM techniques are both well suited for field-scale applicat ions because their volu mes of measurement are large, wh ich reduces the influence of local-scale variability. However, ER is an invasive technique that requires good contact between the soil and four electrodes inserted into the soil; consequently, it produces less reliable measurements in dry or stony soils than the non-invasive EM measurement. Nevertheless, ER has a flexib ility that has proven advantageous for field application, i.e. the depth and volume of measurement can be easily changed by altering the spacing between the electrodes. Furthermore, the EC a measurement with ER is linear over depth unlike EM measurements of EC a , wh ich are a function of a depth-weighted response function. This allows the EC a for a discrete depth interval of soil to be easily calculated with a Wenner array by measuring the EC a of successive layers for increasing inter-electrode spacing and using the following equation [6]: where a i is the inter-electrode spacing, which equals the depth of sampling, a i − 1 is the previous inter-electrode spacing, which equals the depth of previous sampling, and EC x is the apparent soil electrical conductivity for a specific depth interval. Electro magnetic induction can also measure EC a at variable depths determined by the height of the EM instrument above the soil surface, but the depth of penetration is not as easily determined as for ER. Un like ER, depth profiling of EC a with EM is mathematica lly co mplex ( [7], [8], [9]). Measurements of EC a at variable depths with EM are usually achieved by positioning the EM instrument at the soil surface in the vertical (EMv) or horizontal (EMh) dipole mode, which measures to depths of 0.75 and 1.5 m, respectively.

Electrical Profiling (EP)
The uniform static electrical field can be created in field conditions to measure soil electrical resistivity or conductivity in-situ. .However, most modern geophysical methods, such as four-electrode profiling and vertical electrical sounding apply non-uniform electrical field to soils through the point electrodes ( Figure 2). The electrical resistivity measured with these methods is termed apparent or bulk electrical resistivity, to distinguish it from the resistivity measured in laboratory in ho mogeneous samples with unifo rm electrical field. The electrical profiling method is based on the same four-electrode principle as the conductivity cell ( Figure 2). The electrical field is distributed in a soil volu me, which s ize can be estimated fro m the distance among AMNB electrodes. The geometric factor (K) can be precisely derived fro m the array geometry based on the law of electrical field distribution. Using the Laplace's equation in polar coordinates, Keller and Frischknecht (1966) derived the electrical potential functions around the source (A and B) and measuring (M and N) electrodes. The geometric factor K can be obtained for central symmetric four-electrode array of AMNB configuration ( Figure 2) as (7) where  Results may be p lotted as profile lines or contour maps (isopleths resistivity map), or in other presentations according to the specific needs. The method is more accurate than electro magnetic pro filing although slower and more labour-effective.

Vertical Electrical Soundi ng (VES )
Vertical electrical sounding (VES) .It is similar to the method of electrical profiling is based on the four-electrode principle. The VES array consists of a series of the electrode combinations AMNB with gradually increasing distances among the electrodes for consequent combinations. The depth of sounding increases with the distance between A and B electrodes. The result of VES measurements with central-symmetric arrays is apparent (bulk) electrical resistivity as a function of half of the distance between the current electrodes, i.e. ER = f (AB/2) (Beck, 1981). The relationship between ER and AB/2 can be converted into a relationship between electrical resistivity and actual soil depth through a computer interpretation.
Pozdnyakov et al. (1996a) developed programs for soil VES interpretations based on an updated R-function [10]. We modified the conventional VES method for adequate 1

Non-Contact Electromagnetic Profiling
Traditional EM methods have difficu lty focusing on targets buried at the depths less than 5 m and can provide only local measurements of electrical conductivity or resistivity. At the other extreme, most ground-penetrating radar systems, although generate continuous electrical profiles, can only investigate the top meter or so when salts or clay minerals are present in the soil. Hence, in many applications there is a depth range where neither traditional EM nor GPR systems are adequate. The advantages of NEP method are that it automatically records continuous profiles of electrical resistivity and allows easy changing inter-coil spacing to survey different soil depths. A generator constantly excites electro magnetic field through the two radiating antennas. The antennas form the transmitting coil through the soil. Parameters of a secondary electrical field created in the soil are received by the receiving co il and automatically recorded in a graphical fo rm of continuous electrical resistivity profile in the receiver-register block. The NEP equip ment operates on user-defined frequencies of the primarily electro magnetic field within the range from 12.5 to 14.5 kHz. Due to the low frequency, the properties of the created electromagnetic field are similar to those of the stationary electrical field created by the methods of constant current (VES and EP). Thus, we can easily vary the depth of electro magnetic profiling by changing the distance between radiating and receiving antennas. The minimal depth of 0.4 m can be investigated with the method at a 5-m.
All the methods used in this study have different advantages and limitations. Therefore, no single method could be a p riori reco mmended as universal for all soil applications. Three methods of the stationary (SP, EP, and VES) and one methods of the non-stationary electrical fields (NEP) were tested in different applications in soil genesis studies, civil and environmental engineering, agriculture, and soil mon itoring.

Results and Discussion
The study was conducted in the laboratory using seven different types of soil, co llected fro m different construction site. Electrical resistivity of soil is measured for every compacted soil sample with changing of percentage of water contents in soil.
The table below shows percentage of soil particles (such as gravel, sand silt and clay), soil pH value and soil electric resistivity at optimu m mo isture content which is obtained by pH value testing and soil electrical resistivity testing in laboratory. The soil resistivity measurements of co mpacted soil are done in this work using Fluke 8846A precision digital mu ltimeter with Mega-Oh m scale for easier reading. Using four point arrangements of Fluke dig ital mu ltimeter has increased the accuracy of resistivity measurements of compacted soil. By the observations of different types of soil characteristics assessment at optimu m mo isture content it can be concluded that : 1). High acid pH value in soil with mo re courser particles such as gravel, sand etc. and less clay part icles have mo re electrical resistivity.
2). When high organic content present in the so il, decaying of organic contents is responsible for the increase of H + value of soil wh ich supposed to cause high acidic pH value, but in practical organic soil with less courser particles and high clay particles have low acid p H value. This is because change of particle sizes has more effects changes of pH value.
Vo lu me density of electrical charges is proportional to the number of electrically charged particles in an elementary volume of media. Volu me density of mobile electrical charges designates the content of ions, which neutralize charges on a free surface. As surface charge in soils is formed by orbed (exchange) cations and anions (Sparks, 1997), the ion exchange capacity is equivalent to the density of exchange surface charges. The ion exchange cap acity of the soil is the product of the soil specific surface and surface charge density [11]. Soil charge is determined by an ion exchange, which in turn depends on three factors: 1). iso morphic substitutions in clay minerals 2). breakage of ionic bonds in o rgan mineral co mplexes and 3). Alterat ion of charge distribution in macro molecu les of soil organic matter.
Therefore, soil chemical propert ies, such as humus content, base saturation, cation exchange capacity (CEC), soil mineral co mposition, and the amount of soluble salts influence the ion exchange in soils. These soil properties are related with the volu me density of mob ile electrical charges in soils and, in turn, with the soil electrical parameters. So il chemical properties, responsible for the formation of soil ion exchange capacity, are related with the total amount of available charges in soils. Soil physical properties, such as water content and temperature, influence the mobility of electrical charges in soils. Fro m our studies of the relationships between electrical resistivity and soil bulk density or soil water content (Figure 4) in laboratory conditions using four-electrode probe method, the mobility of electrical charges exponentially increases with the increase in those properties [12]. Other soil physical properties, such as soil structure, texture, and bulk density, alter the d istribution of mob ile electrical charges in soils. Thus, the volume density of mobile electrical changes is related to many soil physical and chemical properties. i is the valence of the i-th ion, e is the electronic charge, k is the universal gas constant, and T is the absolute temperature. Therefore, fro m Eq. [8] the volu me density of the mobile electrical charges is exponentially related to the electrical potential. According to Oh m"s law the electrical potential is in direct proportion to the electrical resistivity. If the change of a soil property, such as water content, bulk density, or salt content causes a proportional change in the volume density of the mobile electrical charges, a relationship between electrical parameters and soil property (SP) can be exp ressed as (9) Where a 1 , a 2 , b 1 , and b 2 are emp irical parameters; ϕ is the electrical potential, and ER is the bulk electrical resistivity of the soil. So me relat ionships between soil properties and volume density of mob ile electrical charges may not obey a single exponential equation on the whole range of property variation. For examp le, the relat ionship between soil water content and electrical resistivity was appro ximated with different exponents at different ranges of soil water content due to the influence of soil water retention [13].
While measuring electrical parameters in-situ, it is difficult to study separately the relationship between a soil property and electrical parameters. Therefore, the relationship of Eq. [4] may be less strong when measured under the simu ltaneous variations of many soil properties. Nevertheless, the general exponential relationships were obtained for many soil properties, such as total soluble salts, CEC, base saturation, humus content, etc. both in laboratory and field conditions.
Considering the qualitative structure of mobile electrical charges soils can be broadly subdivided into two groups. The first group is soils with lo w soluble salts and CEC filled by Ca +2 , Mg +2 , Al +3 , and H + . These soils are formed by the processes of podzolizat ion, lessivage, eluviation-illuviat ion, humification, mineralizat ion, and gleization in humid areas (Wild ing et al., 1983). Spodosols, Alfisols, Gelisols, Histosols, Ult isols, and Mollisols can be considered as soils of the first group. The processes of calcification, salin izat ion, alkan izat ion, pedoturbation, humification, and mineralizat io n in arid and semiarid areas form the second group of soils with CEC filled by Ca +2 , Mg +2 , and Na + and, in some soils, high salinity. Soils of the second group represented by Aridosols, Vert isols, and some Mollisols. Inseptosols and Entisols can be assigned to either the first or second group depending on the primarily soil processes dominating in the soils.
For the soils of first group the strongest exponential relationships were obtained for the exchange capacity and base saturation. The correlation coefficients for the relationships with base saturation were as high as 0.90 and 0.88 for soil and collo id suspensions, respectively. The correlation coefficients of the relationships between cation exchange capacity and electrical resistivity were 0.89 for soil suspension and 0.87 for collo id suspension. These two properties characterize the amount of exchange cations in soils. Since soils in hu mid areas have a low amount of soluble salts, the exchange cations play an important role in soil electrical conductivity. The soil base exchange cations are relatively mob ile and primarily conduct electricity in soils of hu mid areas. Hu mus content also increases the cation exchange ability of the soils. Therefore, the relat ively strong relationship (r = -0.78) was found for the total humus content and electrical resistivity of the collo id suspension. A high correlation coefficient   0.78 r  was also obtained for the field water content and electrical resistivity of the collo id suspension. The water content in the soils o f hu mid areas is not limited by precipitation and usually determined by the water retention ability of soils. Therefo re, soils with high clay and hu mus contents tend to have high base saturation and high field water content. Thus, for soils in humid areas the basic source of mobile electrical charges is fro m soil exchange and retention capacity. Electrical resistivity has strong exponential relationships with soil properties characterizing soil exchange capacity, such as base saturation, water and humus contents, and cation exchange capacity. Similar relat ionships were obtained for the electrical resistivity measured in-situ along open soil pits and on the soil surface with the EP and VES methods. The relationships were not as strong as those, measured in soil and collo id s uspensions, but nevertheless appeared exponential. Since CEC and organic matter are the predominant sources of mobile electrical charges in soils of the first group, there is general exponential relationship between those properties and electrical parameters (such as V and ER), measured in-situ ( Figure 5) The exchange capacity of soils in arid areas (second group) is filled with calciu m, magnesium, and odiu m cations and the same cations dominate in the soil solution. Therefo re, the electrical parameters show strong relationships with these cations. A strong exponential relat ionship was obtained between electrical potential, measured on soil surface with the self-potential method and the sum of Ca, Mg, and Na (r = 0.810). For the sodium content alone and electrical potential, the relationship is also exponential with r = 0.599. The Na/(Ca+Mg+Na) ratio is related with the electrical potential by the linear relationship with r = 0.543. Electrical potential decreases with the increase of relative amount of sodium in Aridosols. The same type of linear relat ionship with r = 0.356 was obtained for Al/(Ca+Mg+Al) ratio and the electrical potential in Alfisols of humid areas. Such ratios are important for soil genesis studies, since they indicate the degree of sodicity in Aridisols, and the degree of eluviation (podzolizat ion) in Alfisols and Spodosols. The obtained relationships can be used to study the soil-forming processes in these soils. Since soil salin ity in soils of the second group is the summary characteristics of the available electrical charges, the electrical parameters are strongly related with the total soil salinity. (Figure 6) shows the schematic curvilinear relationship between electrical resistivity or potential and soil salinity for the soils of second group.
Electrical parameters measured with geophysical methods in-situ are related with d ifferent soil properties, easily measured, and can be used to study many soil problems. Different princip les of applications should be considered for three types of problems. The first-type problems are the monitoring of a soil property, which is only one to vary during the measurements. In such problems the measured electrical resistivity or potential can d irectly indicate the change in the soil property in-situ. Such principle was utilized for measuring differences in peat soil co mpaction under seasonal road and monitoring soil melt ing in spring .  The second-type problems include investigations of soil properties, which predominantly influence the measured electrical parameters. Therefore, the measured electrical parameters sually show strong relationships with such properties even in field conditions. For examp le, since the variation in stone content influences the soil electrical resistivity much stronger than ariation of any other properties in soils of Crimea Peninsula, the VES method was able to accurately utline the layers with different stone contents in these soils and estimate the vo lu metric content of stones. Pollution by petroleum products highly increases the electrical resistivity of Gelisols in northwest Siberia, wh ile salty min ing solutions decrease resistivity of the soils. Therefore, methods of EP, VES, and NEP could be used to map pollut ion in these soils . Ext reme d ryness of Histosol in some seasons highly increases the electrical resistivity at the top of the profile, whereas variation of soil water content around field capacity usually does not alter the typical profile distributions of electrical resistivity in the soils . Disturbance of soils changes of the measured electrical resistivity in soils of humid area significantly enough to detect hidden burial places for forensic and archaeological applications The third-type problems require careful considerations of the relationships between many soil p roperties and electrical parameters measured in-situ. A lthough soil electrical parameters depend simultaneously on many soil properties, such as salt, water, humus or stone content, CEC, texture, and temperature, in many situations the influence of some soil properties can be considered neglig ible if they vary around their maximu m, based on Boltzmann"s distribution law. For examp le, soil water content close to the field capacity does not practically influence the change in electrical resistivity ( Figure 3). Therefore, in-situ measurements of the electrical parameters of soils in humid areas is not influenced by water content variation and can be used to evaluate elluvial-illuvial horizons in soil profile and more stable soil properties, such as CEC, soil texture, and humus content (Figure 4). On the other hand, the high variation of soil water content within the whole possible range in the profiles of alluvial soils in Astrakhan" area allo ws locating the groundwater table (Po zdnyakova et al.,  2001). The simu ltaneous influence of various soil properties on the measured electrical conductivity were successfully studied with the methods of geostatistics, which consider not only inter-variable but also spatial relationships.
Fro m the point of view of the field of civ il engineering soil electrical resistivity can be used to estimate soil co mpactions characteristics

Conclusions
Different laboratory testing programs on soil characterizat ions is carried out to determine the effect of chemical characteristics through electrical resistivity. Many types of physical factors have considerable effect on obtaining chemical properties through electrical resistivity of soil such as particle sizes, mo isture content etc.In investigation of soil for both construction and agricultural purpose it requires quick and, when possible, non-disturbing estimations of numerous soil properties, such as salinity, texture, stone content, groundwater depth, and horizon sequence in soil profiles; however, conducting soil measurements with a high sampling density is costly and time-consuming. Trad itional methods of soil analysis is badly harmfu l for present soil condition as it mostly require disturbing soil, removing soil samp les, and analysing them in a laboratory. By the help of these electrical resistivity methods for soil investigation wee can easily analysis the required properties of soil in construction sites or fields for without disturbing and removing soil sample fro m its actual condition. This study would help to conduct further research of obtaining chemical propert ies of soil without disturbing soil at sites.