Geologically, many authors have studied the area (e.g. [13] [14] [19] [20] [21] [27] [28] [29] [30] [33] [34] ). The area under consideration represents a part of the Nile valley zone of Egypt. Figure 2 is the geologic map of Sohag Governorate

including the study area [6] .

Paleogene sediments and narrow cultivated stretch bordering the Nile River cover most of the area under investigation. This cultivated land has been formed through the flood season of the river Nile since a long time to form the Nile sediments (Pleistocene and Recent deposits).

Several attempts have been done by several authors to discuss the stratigraphy of the Nile Valley, such as (e.g. [1] [2] [7] [10] [11] [12] [17] [18] [23] [24] [25] [26] [30] [32] . The Paleogene rock units in the Nile basin classified into Dakhla Shale and Esna Shale at the base (Paleogene age) followed on the top by Thebes Group, Minia Formation, Mokattam Group and Maadi Group (Eocene) [23] [25] [30] . The Paleogene sediments based on their faunal contentsclassified into the Esna shale at the base overlain by the Assiuti Chalk and the Manfalut Formation at the top; both are the time equivalent of Said’s Thebes Formation [1] [2] . Nine distinctive formations in the Late Early Cretaceous-Early Paleogene succession in the Nile Valleyrecognized by [7] .

The stratigraphic section of new Sohag city, Akmim center has been studied and described as shown in Figure 3 [8] .

The utmost constraint of the resistivity sounding method is that it does not take into consideration the horizontal changes in the subsurface resistivity. The ERT

survey conquers this problem, where the resistivity changes in the horizontal direction as well as in the vertical direction along the survey line. Therefore, ERT technique selected for this survey. While, the Wenner array gives the smallest number of possible measurements compared to the other common arrays [9] , also it competent to work in noisy fields and when good vertical resolution is required. The Wenner array was used in the present work.

The geo-electrical data is collected along thirteen parallel (ERT) profiles using the Wenner electrode arrangement with maximum spread of 160 m, 5 m spacing between the electrodes and 10 m interline distance using the SYSCAL R2 system. Through the ERT survey, the penetrated depth reaches about 20 m. A built-in microcomputer together with an electronic switching unit is used to automatically select the relevant four electrodes for each measurement as shown in Figure 4.

Seismic exploration involves generation of seismic waves and recording the arrival times of these waves from the source to the series of geophones [4] . Seismic refraction is used to evaluate the necessary parameters for constructions, or to solve the problems related to the geologic nature of sub-surfaces, mining works, and the environmental conditions overcame in the site [5] [31] .

Twenty-six seismic refracted profiles (forward and reverse shots) acquired using an exploration seismograph model “DOLANG-Italy”. Thirteen profiles for (P-wave) and thirteen profiles for (SH-wave) conducted parallel to the north direction of the study area as shown in Figure 4. The length of all profiles is about 75 meters, where the geophone interval is 6 meters and the shot points are 4.5 meters far from the first and the last geophones.

Ground penetrating radar (GPR) is a high-frequency electromagnetic technique;

commonly applied to solve most of the engineering and environmental problems. A GPR system radiates short pulses of high-frequency EM energy into the ground from a transmitting antenna. The velocity of EM waves is related to the dielectric permittivity of subsurface materials. When this wave encounters the interface between two materials having different dielectric permittivity, a portion of the energy is reflected back to the surface, where it is detected by a receiver antenna and transmitted to a control unit for processing and display.

Depth of penetration of radar waves is a function of antenna frequency, dielectric constant and the electrical conductivity of the soils. However, low-fre- quency antennas achieve greater depth of penetration than those of high frequency, but they have poor spatial resolution. Conductive soils, such as clays, attenuate the radar waves much more rapidly than resistive soils such as dry sand and resistive rock [3] .

A raw estimation of depth is obtained by multiplying the one-way travel time with the average propagation velocity of the GPR pulse inside the geological formation. The GPR method has been increasingly used for shallow subsurface mapping because of its capability to provide a high-resolution image of the near surface discontinuity and heterogeneity [22] .

Thirteen GPR profiles have been acquired using RAMAC instrument with 100 MHz antenna; their lengths are 250 m. The conducted GPR profiles is measured at the same location of the conducted (ERT) and (SSR) profiles as shown in Figure 4.

The Conducted ERT data were processed using RES2DINV program package edited in 1998, [15] [16] . The measured data were plotted as “Apparent Resistivity Pseudo-sections” to check the data quality and measured point distribution. Applying “Least Square Approach” the measured apparent resistivity is inverted to true resistivity values in the form of modeled 2D Resistivity sections.

The ERT data were used to provide the distribution of electrical properties in the subsurface soil, to outline the high resistivity zones that could be attributed to the hard and dry calcareous sand, and to outline the low resistivity zones attributed to silty clay soil and water saturated soil.

The inspection of the conducted ERT profiles, two major geoelectric layers could classified as the following

・ The top layer exhibits a moderate resistivity values ranging from 101 Ohm・m to 410 Ohm・m with average thickness of 5.0 m along all the conducted profiles. The ERT results correlation with the geologic information displays that this layer classified as gravel accumulation imbedded into the calcareous sandy layer.

・ The bottom layer underlies the top layer which extended down to the end of the ERT sections is characterized by low resistivity values ranging from 15.7 Ohm・m to 39.8 Ohm・m with thick thickness extends to the end of the profiles. This low resistivity value is due to the presence of silt/clay layer intercalation that extends with different lengths and thickness in all the surveyed profiles as shown in Figures 5-8.

The computer software (SEIS-REFA) program is used for estimating the parameters of the time-distance curve (X-T) curves and their corresponding depth-

velocity models. Figures 9-12 are showing example of travel time-distance curves and their depth-velocity models for the two conducted seismic profiles (P3 and P7) for (P-wave) and (SH-wave), respectively.

The Shallow seismic refraction (SSR) was applied to spectacle the areal distribution of the seismic velocities along the study area. The resultant seismic velocities will reflect the condition of solidity of the subsurface soil.

The inspection of the conducted seismic refracted profiles reveals the presence of two geoseismic layer according to their geoseismic velocities as follows:

・ The first geoseismic layeris represented in the all conducted seismic Profiles as shown in Figures 9-12 with slightly variable thickness. It is characterized by P-wave and SH-wave velocities ranging from 800 - 1200 m/s, and 650 - 900 m/s respectively. This layer shows symmetrical thickness across the seismic profiles with an average thickness of 3 m. This layer could be attributed to Calcareous sand (surface layer).

・ The second geoseismic layer follows the surface layer with high seismic velocity for P-wave and SH-waveranges from 2000 - 2600 m/s, and 1800 - 2100 m/s respectively. This layer is extending till the end of the section. This layer is corresponding to hardsilty clay.

The data are processed by using Reflex-win program, which operates under windows environment.

Only one reflector can be seen on the resulted GPR profiles. This reflector

interpreted as the contact surface between the upper gravel and calcareous sand layer and the lower clay layer. The nature of the clay reflections changed from place to place in the study area, which can be interpreted as the presence of different type of clays, most probably due to difference in saturations. Figure 13 and Figure 14 are representing of geo-GPR cross section along Profiles No. (2 and 4).

The attenuation of the electromagnetic waves increases with material conductivity. Materials that have high attenuation include clays, silts, shales and seepage

water, while which have low attenuation include distilled water, air, dry sand and ice.

Electromagnetic waves penetrate to almost 5 m subsurface (surface layer) until reached to the clay layer that attenuating the waves and masking other layers underneath.