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Ozean Journal of Applied Sciences 7(3), 2014
Ozean Journal of Applied Sciences 7(3), 2014
ISSN 1943-2429
© 2014 Ozean Publication
SUBSURFACE STRUCTURAL CHARACTERIZATION USING DC RESISTIVITY
METHOD AT INDUSTRIAL DEVELOPMENT CENTRE (IDC), ZARIA.
S. D. SALEH*, P. O. SULE, A.L. AHMED
K. A. MURANA**
*Department of Physics, Ahmadu Bello University, Zaria, Nigeria
** SLT Department, Abdu Gusau Polytechnic, Talata Mafara, Nigeria
*E-mails for correspondence [email protected]
__________________________________________________________________________________________
Abstract: Electrical resistivity method employing Vertical Electrical Sounding (VES) was carried out at
Industrial Development Centre Zaria. 27 Vertical Electrical Soundings (VES) were conducted along
predetermined profiles at a station interval of 100m. The survey was carried out to investigate geoelectric and
geologic parameters of the subsurface as means of determining the competence of the materials underlie the
premises, in aiding structural and environmental works in the area. Terrameter SAS 300 system was used for
data acquisition using Schlumberger array. Maximum current electrode separation (AB) of 200m was used.
Interpretation was performed using computer software (Ipi2win and surfer 7). The results of the study indicate
that the area is underlain by three to four subsurface layers. The resistivity of the first layer ranges from as low
as 54 ohm–m to as high as 487 ohm-m with an average thickness of 2m. This layer is the superficial cover
composed of sandy, silt, weathered laterite and clays that are confined in the sand in some places. The second
layer has resistivity values between 114 ohm-m to 2518 ohm-m which is the weathered basement rock and fresh
laterite in some places. The third layer has relatively low resistivity value that ranges between 101 ohm-m to
916 ohm-m. This layer is the fractured basement with varying thickness. The fourth layer is the crystalline
basement rock with resistivity values much greater than 1000 ohm-m and an infinite thickness. The
investigations show that the study area is underlain by competent material except towards the northern end that
has clayey sand in the superficial cover, the aquifer in the area which is confined occurs in the weathered and
fractured basement rock. Eastern half of the study area could be favorable for groundwater exploitation.
Keywords: DC Resistivity, Geoelectric and Geologic layers, subsurface structures.
__________________________________________________________________________________________
INTRODUCTION
The knowledge of subsurface structures within the study area will go a long way to assist the centre in knowing
suitable location for structural engineering works, locating suitable areas for refuse dumps, and construction of
artificial lake or dams. The statistics of failure of structures such as roads, buildings, dams, bridges and even
boreholes throughout the nation has increased to an alarming rate. The need for pre foundation study has
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therefore become imperative so as to prevent loss of valuable lives and properties that always accompany such
failure. Moreover, the acute shortage of water especially during the dry season in Zaria and its environs
necessitate the intensive use of groundwater, hence the need for sustainable underground water development and
utilization.
Geophysical techniques can assist the construction industry in many ways: before, during, and after construction
to solve construction problems or to facilitate the construction processes. Resistivity sounding or mapping are
surface geophysical techniques that involve the measurement and interpretation of physical properties of the
earth to determine subsurface condition for engineering and environmental investigations.
The study area Samaru, Zaria, is a semi urban city with increasing population growth and infrastructural
development. The annual rainfall is inadequate; therefore the need for subsurface study becomes imperative.
Subsurface investigation is not an easy task but the advent of technology has made the quest for reliable location
for any structural and/or environmental engineering works easy. Also the need for water for all purposes in life
has drift from ordinary search for water to prospecting for steady and reliable subsurface or underground water
from boreholes. The geoelectric method has been found to be very reliable for environmental and groundwater
studies over the years (Shemang, 1990, Murana et al., 2011)
The area under study lacks detailed geophysical investigations. Most geophysical works carried out around this
area are regional in nature or are localized to specific areas. However, many geophysical and geological works
have been carried out either at Samaru area or at other parts of Zaria. Du Preez (1952) carried out the regional
study of Zaria and reported the presence of prominent steeply dipping joints in some outcrops of granite in
Kubanni Basin; he also affirmed the presence of groundwater in some joints.
Akpoborie (1973) in his study on Kubanni Basin has reported that the older granite icebergs are intensively
fractured giving way for easy recharge of the weathered basement aquifer with rain water. McCurry (1970) has
studied the basement geology of Zaria and has concluded that the deeply weathered areas of crystalline
basement outcrop constitute the useful aquifers; he has affirmed that the aquifers are variable in extent and
thickness ranging from broad areas of deeply weathered to narrow joints and fracture zones. Olugbenga (2009)
from a resistivity investigation of the groundwater potential at Nuhu Bamali polytechnics, Zaria main campus,
has reported that his study area is underlain by rocks of different lithological compositions comprising the top
soil, the weathered basement, fractured and fresh basement rock. The depth to the basement varies from an
average of 12m to 29m. He has further stated that the low resistivity area is the most promising for groundwater
exploitation.
The primary aim of this research work is to characterize the subsurface structures by determining the lithology
within the area under investigation base on the physical parameters measured and also to map the subsurface
rocks, thereby delineating accumulation zones, recharge and drainage pattern. The objectives set to achieve these
aims are:
(1) To produce sounding curves, geoelectric and geologic sections along the profiles.
(2) To delineate the various strata within the subsurface.
(3) To determine depth to basement so as to get a picture of basement topography.
(4) To determine aquifer thickness in order to delineate favourable area(s) where to site boreholes.
Location of the Study Area
The study area, Industrial Development Centre (IDC), Samaru, Zaria, Kaduna state is located approximately on
latitude 110 09’22.9” N and 110 09’58.5”N and between longitude 70 39’E and 70 40’E along Zaria - Sokoto road.
The study area is opposite Ahmadu Bello University, (ABU) main campus. It has a total land area of about 64.80
hectares. The terrain is relatively flat; the area can be accessed by motorable roads see Fig.1 below.
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Ozean Journal of Applied Sciences 7(3), 2014
Figure 1: Location map of the study area (source; Google image 2010 )
Climate, Relief, Vegetation and Ecomonic Activity of Zaria Area
Zaria is located approximately between latitude 11 0 04’N and 110 09’N and between longitude 70 39’E and 70
50’E and is about 686m above sea level. It falls within the tropical savannah climate, according to Koppen’s
world climate classification. It lies in the natural vegetation of the Northern Guinea Savannah, some 80km north
of Kaduna town, along the major highway from Kaduna to Kano state.
The study area, Samaru, is in the tropical wet and dry climate zone, characterized by strong seasonal rainfall and
temperature distribution. The climatic condition is controlled by two air masses, the maritime tropical air mass
and the continental tropical air mass. When the maritime tropical air mass is prevailing, the Zaria area
experiences a rainy season, while the continental tropical air mass controls the dry season with its cold, dry and
dusty air which occasionally limits visibility and reduces solar radiation. Daily maximum temperature shows a
minor one of 23oc in November/ December and major peak of 39oc in April. The rainy season has a short
duration and it is followed by 5-7 months of dry season. The rainy season appears to begin in May and ends in
September while the dry season normally starts from around October to April (Olugbenga, 2009). The prevailing
vegetation of tall grass and big trees are of economic importance during both the wet and dry seasons in the
study area. About 80 percent of the Zaria populations are engaged in peasant farming producing both food and
cash crops. During the dry season, many people in Zaria engage in irrigation farming along some major rivers
and near dams.
General Geology of the Study Area
Zaria area is a dissected portion of the Zaria – Kano plain, belonging to the central basement complex. This has
been described by (Russ, 1952) as comprising older high grade metamorphosed gneiss interspersed by belt of
young metasediments of mainly quartzite and schist. Zaria region is underlain by crystalline metamorphic and
igneous rocks of Precambrian to lower Paleozoic age (Wright and McCurry, 1970) occurring on the basement
complex.
A major part of the rocks is of high grade metamorphism mainly gneisses which suffered intense folding and
granitization and have remained stable for millions of years. Others are migmatites, older granites, and more
recently matasediments (quartz, schist, laterites and alluvium). The nature of parent material and the long period
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of weathering under tropical condition have produced a characteristic topography of peneplain, inselbergs and
domes of resistant basement rocks. A combination of topography and geology more or less control the
groundwater occurrence in this area. Like other parts of Zaria, Samaru area is underlain by differentiated
Pre-Cambrian basement complex formation comprising both igneous and metamorphic rocks. Furthermore,
geological information indicates that undifferentiated basement complex of migmatites, granites, gneisses and
metasediments is overlain by laterites Fig. 2 (Wright and McCurry, 1970).
Figure 2: A generalized geological map of Nigeria (after Kogbe, 1989)
Hydrology and Hydrogeology of the Study Area
The urban Zaria is blessed with abundant water resources both ground and surface and the distribution of these
resources have very little variation in both time and space amongst the sub-settlements (Yusuf et al., 2007).
There are two major river systems; the Kubanni and Saye, joined at a confluence to form river Galma. These
rivers together with their tributaries (Kamacha and Shika) drain the land area of urban Zaria. Du Preez (1952) in
a regional study of Zaria reported the presence of prominent steeply dipping joints in some outcrops of granite in
the Kubanni basin. He also affirmed the presence of groundwater in some joints. Generally, the hydrogeology of
an area is determined by geology and climatic condition of that region, and then geological formations and the
structures underlying the area determine the aquifer that would be developed. Groundwater recharge is the
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process by which aquifers are replenished with water from the surface. Many factors influence the rate of
recharge including the soil type, plant cover, slope, rainfall intensity, and the presence and depth of confining
layers and aquifers. Most of the groundwater recharge in the study area occurs during the wet season when
precipitation is highest.
Choice of Electrode Configuration
Many different electrode spreads have been used in the past but only few are still in use today. These include;
Schlumberger array, Wenner array and double – dipole array. However, the most widely and commonly used
arrays are Schlumberger array and Wenner array.
The choice of array and its dimension largely depend upon the target; its size, depth and resistivity contrast with
its surroundings. For this present study, Schlumberger array was adopted because of the following advantages;
1) The relatively small separation of the potential electrodes reduces noise due to ground current (from
industrial and telluric sources) which may limit the useful depth of penetration.
2) The Schlumberger array has a greater depth of penetration than the Wenner.
3)
In general VES method with Schlumberger array assumes considerable importance in the field of
groundwater exploration because of its ease of operation (only the current electrodes need to be
frequently moved), relatively low cost and its capacity to distinguish between saturated and unsaturated
layers (Hadi, 2009).
Schlumberger array
In Schlumberger symmetrical array the current and potential pairs of electrodes have a common mid- point. All
the four electrodes are arranged collinearly, the current electrodes are usually much further apart than the
potential electrodes, (Fig.3). The smallest current - potential electrode distance is always much greater than the
distance between the two potential electrodes (Telford et al., 1990). In depth probing the potential electrodes are
fixed while the current electrode separation is increased symmetrically about the centre of the spread. However,
when expansion of the current electrodes causes the potential difference to become so small that it cannot be
measured precisely, the potential electrodes are moved further apart, while keeping the current electrodes fixed,
and then further readings are taken by expanding the current electrodes using the new potential electrodes
positions. The apparent resistivity is plotted against electrode spacing on log- log scale to obtain a sounding
curve.
Figure 3: Schematic diagram of Schlumberger Array
Vertical Electrical Sounding (Ves)
Vertical Electrical Sounding (VES) is a geoelectric common method that measures vertical variation of electrical
resistivity (Kelly, 1993). It is well known that resistivity methods can be successfully employed for groundwater
investigations where a good electrical resistivity contrast exists between the water – bearing formation and the
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underlying rocks. Vertical Electrical Sounding (VES) also called depth sounding or sometimes electrical
drilling is used when the subsurface approximates to a series of horizontal layers each with uniform but different
resistivity. The goal is to observe the variation of resistivity with depth. Schlumberger configuration is most
commonly used for VES. The mid-point of the array is kept fixed while the distance between the current
electrodes is progressively increased. This causes the current lines to penetrate to ever greater depth depending
on the vertical distribution of conductivity. A typical subsurface current distribution is illustrated in Fig. 4.
Figure 4: Schematic illustration of Basic Concept of Electrical Resistivity Measurement
METHODOLOGY
Instrumentation
In this survey the instruments used for data collection are; Terrameter SAS 300 system and its components,
magnetic compass, field hammer, cutlass, ranging pole, pegs, electrodes, cables and reels, measuring tape,
global positioning system (GPS), and other accessories. The Terrameter SAS 300 which stands for (Signal
Averaging System) that is consecutive readings are taken automatically and results are averaged continuously
and presented automatically on the display.
Field Procedures and Data Collection
Vertical Electrical Sounding (VES) using D.C resistivity method was carried out in the study area. The data
were acquired using Schlumberger array. Profiles of 400m length that are not necessarily parallel to each other
were established at different locations to cover the whole area under study as shown in Fig. 5.
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Figure 5: Location map of the study area showing positions of profiles
Measurements were taken along the profiles following the technique outlined by (Telford et al., 1990). A station
interval of 100m was used to establish various sounding points. Measurements were taken at each VES point by
expanding the current electrodes symmetrically about the centre of the spread. The maximum exploration depth
(also known as depth of penetration) of the Schlumberger array is 1/4 to 1/3 of the maximum distance of AB
(Frohlich et al., 1996). That is, for AB = 200m the depth probed is about 50m to 60m. This depth is considered
good for subsurface structural investigation and other parameters of interest in the study area.
Data Processing
The data were reduced, and the computed apparent resistivity values were then plotted against their
corresponding AB/2 values on log-log graph paper using computer software (IPi2win). A typical example of
such plots is shown for VES station IDC 20 in Fig. 6. The computer software used (Ipi2Win) is designed for
Vertical Sounding and/or induced polarization data 1D interpretation. Targeting the geological result is the
specific feature distinguishing Ipi2win from other popular programs of automatic inversion. Special attention is
paid to user- friendly interactive interpretation thereby providing low fitting error.
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Figure 6: A Typical resistivity curve and interpreted model for VES station IDC 20
Basis of Interpretation
Available geological controls such as borehole data, resistivity values of earth materials compiled from previous
works were used in order to have a meaningful interpretation. Table1shows the resistivity values of rocks
materials compiled from previous work, while table 2 shows resistivity values adopted for this present study.
Assumption has been made in the interpretation of Vertical Electrical Sounding (VES) data that:
(a) the various geoelectric layers encountered are electrically homogenous and isotropic. However, because of
the existence of lateral variation in resistivity within a layer, possibility of error in interpretation is present.
(b) the principle of equivalence that is non- unique solution for a number of types of a typical three layer curve
which are only distinguished by the resistivity value of their second layer in a relation to the value of either the
first or third layer.
Figure 7: Borehole log data drilled near the study area. (After hydro drilling and engineering ltd
Zaria)
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RESULTS
The data analysis for the Vertical Electrical Sounding (VES) was performed using computer software (Ipi2win)
as stated above. Different geophysical and geologic work carried out in Zaria area were considered in order to
arrive at the resistivity values used for the interpretation of this present work. The work of Hassan (1987),
Shemang (1990) and Olugbenga (2009) were considered, these were compared with resistivity values given by
Telford et al. (1990). Table 1 shows resistivity value from previous work.
Table 1: Resistivity values of rock materials within the Basement area. (Shemang, 1990)
Rock type
Fadama laom
Clay, Silt and sandy
Weathered Laterite
Fresh Laterite
Weathered basement
Fractured basement
Fresh basement
Resistivity Value (Ωm)
20-90
100-200
200-2700
850-3000
20-200
500-1000
> 1000
A comparative Analysis of the soils and rocks materials from north central area of the basement complex
(Zaria, Kaduna, & kano) was carried out in order to arrive at the resistivity values adopted for this work, as
presented in table 2 below
Table 2: Resistivity values adopted for this present study.
Rock type
Fadama Loam
Clay, Sandy silt, Sandy clay,
Fresh Laterite
Weathered Laterite
Weathered basement
Weathered basement (lateritic)
Fractured basement
Fresh basement
Resistivity Value
(Ohm-meter)
30-90
100-200
850-3000
30-300
20-300
300-1500
500-1000
>1000
The resistivity values given in table 2 were used for the interpretation of this present work. The resistivity
models at the sounding points were used to produce geoelectric and geologic sections for the profiles. Example
of such plots for profile EF is shown in Fig. 8.
DISCUSSION
The Geoelectric and Geologic Section along Profile Ef
Figure 8 shows geologic section along profile EF. This profile suggests that the region is underlain by three
layers. The superficial cover (first layer) has resistivity values ranging between 104 ohm-m and 303 ohm-m. The
thickness varies from 1.2m to 2m, this layer probably is made up of sandy – clay and silt (lateritic) soil. The
second layer has resistivity values between 119 ohm-m to 310 ohm-m with an average thickness of 3m. This
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layer probably is the weathered basement that is mostly lateritic. The third later has resistivity value of 2072
ohm-m which is the crystalline basement rock.
Figure 8: A geoelectric and geologic section for a profile EF
Maps Produced from Interpreted Data
In order to look at some subsurface structural trends in the study area, and to reveal the lithological sequence of
the subsurface formation, specialized maps were produced from the interpreted resistivity data obtained for all
the VES stations with the aid of computer software (surfer 7). These are the isoresistivity map, aquifer thickness
map and depth to the basement (overburden thickness) map. The essence of these maps is to show the lateral
variation of resistivity over a horizontal plane at certain depths. In other words these maps indicate the
distribution of resistivity in the study area.
Iso Resistivity Map of the Suface Layer (Top Soil)
The map has been produced in order to see the major composition of the top soil and to know if there is water
saturation in the superficial cover. The map was produced by contouring the resistivity of the surface layer
obtained at all VES points within the study area. Fig. 9
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Resistivity value (ohm-m)
11.158
idc 27
idc 26
latitude
11.156
11.154
idc 25
idcidc
2322
idc 21
11.152
idc 20
idc 17
idc 16
idc 19
idc 15 idc 12
idc 18
idc 11 idc 08
idc 14
idc 04
idc 10 idc 07
idc 13
idc 03
idc 09 idc 06
idc 05
7.662
7.664
7.666
idc 02
7.668
longitude
0
0.002
0.004
0.006
N
460
440
420
400
380
360
340
320
300
280
260
240
220
200
180
160
140
120
100
80
60
40
20
0.008
Figure 9: Iso- resistivity map of the surface layer
Aquifer Thickness Map
The Aquifer thickness map was produced by subtracting the thickness of the first layer from the total depth to
the basement. The thickest part of the aquifer was found to be region around VES points IDC 04, 16 and26 with
thickness of 22.41m, 19.51m and 15.36m respectively. These points were recommended for drilling of borehole.
Fig. 10 shows the aquifer thickness map.
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Ozean Journal of Applied Sciences 7(3), 2014
N
Thickness(m)
21
20
11.158
19
18
idc 26
17
11.156
16
idc 25
15
idc 22
idc 23
idc 20
idc 17
idc 16
idc 19
idc 21
11.154
idc 15
idc 18
11.152
13
idc 12
11
idc 04
idc 07
idc 10
idc 06
idc 09
12
idc 08
idc 11
idc 14
idc 13
14
idc 03
10
9
8
idc 05
idc 02
7
6
7.662
7.664
7.666
7.668
5
4
3
0
0.002
0.004
0.006
0.008
Figure 10: Aquifer thickness map
Depth to The Basement Map (Overburden Thickness Map)
The overburden thickness map was produced from the interpreted depth to the basement at each sounding point
(Fig. 11). This map was prepared to view the geometry or topography of the basement under the study area in
order to enable a general view of the variation in the overburden thickness. The map suggests that the depth to
the basement in the study area range from about 4.72m to 21.3m around VES IDC 25 and 16 respectively. The
deepest part is the region already suggested for groundwater exploitation in this work.
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N
Depth (m)
21
11.158
idc 27
19
idc 26
11.156
17
latitude
idc 25
idcidc
23 22
idc 21
11.154
11.152
idc 09
idc 06
idc 05
7.664
7.666
13
idc 04
idc 07
idc 10
idc 13
7.662
15
idc 20
idc 17
idc 16
idc 19
idc 15
idc 12
idc 18
idc 11 idc 08
idc 14
idc 03
11
9
idc 02
7.668
7
longitude
5
0
0.002
0.004
0.006
0.008
Figure 11: Depth to the basement (overburden thickness) map.
Fresh Basement Rock Map
The resistivity values of the fresh basement obtained in the course of the interpretation were used to plot the iso
resistivity map of the fresh basement rock underlying the study area (Fig. 12). This map was produced by
contouring the resistivity values af the fresh basement. The map was produced to veiw the distribution of
fractured and unfractured rocks underlying the weathered basement. The map shows that the north- western
part of the study area is underlain by unfractured granitic rock mostly at shallow depth.
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Resistivity(ohm-m)
N
8500
8000
11.158
idc 27
7500
7000
idc 26
6500
latitude
11.156
6000
idc 25
idcidc
2322
idc 21
11.154
11.152
5500
idc 20
idc 17
idc 16
idc 19
idc 15 idc 12
idc 18
idc 11 idc 08
idc 14
idc 04
idc 10 idc 07
idc 13
idc 03
idc 09 idc 06
idc 05
7.662
7.664
7.666
5000
4500
4000
3500
3000
2500
idc 02
2000
7.668
1500
1000
longitude
500
0
0.002
0.004
0.006
0.008
Figure 12: Iso resistivity map of the fresh basement
DISCUSSION & CONCLUSIONS
The geoelectric and geologic sections for the profiles suggest that the study area is underlain by three to four
layers of different lithological compositions; namely the superficial cover consisting of clayey sand, silt,
weathered laterite with an average thickness of 2m. The second layer which mainly composed of fresh laterite /
weathered basement has varying thicknesses ranging from 1.86m to 22.4m, the thickness of the fractured
basement ranges between 4.0m to 19.0m, depth to the basement ranges between 4.72m to 21.3m, and the fourth
layer is the fresh basement rock with an infinite thickness. The investigation shows that the area is underlain by
competent material, however, the superficial cover is loose and humus which contained clayey sand in some
places thus need to be totally excavated in any structural and engineering works in the study area. The fresh
basement rock map (fig. 12) indicates that the north - western part of the study area could be used for refuse
dump because of unfractured / unfissured nature of granitic rock underlying the area at shallow depth.
The laterite in the first layer as shown in some locations is of great importance as it reduces surface run off and
aids infiltration into the underlying aquifer. The thickness of the weathered basement in the eastern half of the
study area is large enough to harbour substantial quantity of water; therefore, this area could be suitable for hand
dug wells or boreholes.
The drainage pattern in the study area corresponds with the basement topography (towards the depressed area)
this result in the effective recharge of the aquifer in the areas recommended in this study.
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RECOMMENDATION
The study area lack detailed record of any geophysical investigation and no borehole log is available; as a result
of this conclusion derived cannot be compared with any previous results. It is recommended therefore; that
further geophysical and geological investigations employing other methods should be carried out in the study
area so as to have detailed information about the subsurface.
ACKNOWLEDMENT
The authors acknowledge the permission given by the authority of Industrial Development Centre, (IDC) Zaria,
to carry out this research work on IDC and for the assistance rendered during the fieldwork. The authors equally
thank Physics Department of Ahmadu bello university, Zaria for providing the equipment for the study. The
contribution of Late Mr. B. Nwosu of Physics department, Ahmadu Bello University Zaria, during Data
acquisition is also acknowledged.
REFERENCES
Akpoborie, I.A. (1973). Hydrological Control of Structures along Samaru Creek. Unpublished B.Sc. Thesis,
Geology Department, Ahmadu Bello University, Zaria, Nigeria
Du Preez, J.W. (1952). The Regional Rechnical College Site Zaria Water Supply. Unpublished Report,
Geological Survey of Nigeria, No. 1005.
Frohlich. R.K., Fisher, J.J. and Summerly, E. (1996). Electric- hydraulic conductivity correlation in fractured
crystalline bedrock: central landfill, Rhode Island, USA. Journal of Applied Geophysics,
35: 249259.
Hadi, T.N. (2009). Geoelectric Investigation of the Aquifer Characteristic and Groundwater Potential in
Behbahan Azad University Farm, Khuzestan Province, Iran. Journal of Applied Sciences, ISSN 18125654, Asian Network for Scientific Information.
Hassan, M. (1987). Geoelectrical Investigation of Western half of Kubanni Basin. Unpublished M.Sc Thesis,
Physics Department, Ahmadu Bello University, Zaria.
Kelly, W.E. (1993). Applied Geophysics in Hydrogeological and Engineering Practice. Elsevier, Amsterdam.
292 Pp.
Kogbe, C.A. (1989). Geology of Nigeria: RockView (Nigeria) Limited:Jos. Pp 348-358.
McCurry, P. (1970). Geology of Degree Sheet 21 Zaria. Unpublished M.Sc. Thesis, Department of Geology,
Ahmadu Bello University, Zaria.
Murana, K.A., Sule, P., Ahmed, A.L., Abraham, E.M and Obande, E.G (2011). Subsurface Stratigraphic
Mapping using Geoelectric Method and its Impact on Development in Federal College of Education
(Technical) Gusau, Zamfara State. Nafta Scientific Journal 62(11-12) 389-395, Croatia.
Olugbenga, A.F. (2009). Two Dimensional shallow resistivity investigation of the groundwater potential at
Nuhu Bamalli Polytechnics. Pacific Journal of Science and Technology, 10(1), 602-613.
Russ,W.(1952). The Geology of Parts of Nigeria and Zaria Province, Northern Nigeria. Geological Survey of
Nigeria, Bulletin, 29.
101
Ozean Journal of Applied Sciences 7(3), 2014
Shemang, E.M. (1990). Electrical Depth Sounding at Selected Well Sites within Kubanni River Basin Zaria,
Unpublished M.Sc Thesis, Department of Physics, Ahmadu Bello University, Zaria.
Telford, W.M., Geldart L.P. and Sheriff R.E. (1990). Applied Geophysics. Cambridge University Press, London.
www.googleearth.com/image (2010) digitalglobe.
Wright, J.B, and McCurry, P.(1970). A Reappraisal of Some Aspects of Precambrian Shield Geology Discussion. Bull. Geol. Soc. Am., 81, 3491-3492.
Yusuf Y.O., Iguisi, E.O, and Bello, A.C. (2007). A comparative Analysis of the use of Velocity Area Method
and the Weir Technique in Assessing the Discharge of River Kubanni, Zaria, Nigeria. Journal of
Geography, Environmental and Planning, Vol.3, No. 1.
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