Ijciet 10 02_097

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International Journal of Civil Engineering and Technology (IJCIET)
Volume 10, Issue 02, February 2019, pp. 999-1009, Article ID: IJCIET_10_02_097
Available online at http://www.iaeme.com/ijciet/issues.asp?JType=IJCIET&VType=10&IType=02
ISSN Print: 0976-6308 and ISSN Online: 0976-6316
© IAEME Publication Scopus Indexed
FIELD IDENTIFICATION OF GROUNDWATER
POTENTIAL ZONE BY VES METHOD IN
SOUTH MALANG, INDONESIA
Moh. Sholichin and Tri Budi Prayogo
Water Resources Engineering Department, Brawijaya University, Indonesia
ABSTRACT
In order to solve the water scarcity problem in South Malang, East Java,
Indonesia, we have attempted to investigate groundwater by assessing the subsurface
geology and groundwater potential zones. An attempt had been made to identify the
subsurface lithology and aquifer zones by VES (Vertical Electrical Sounding) method
in Pagak, Kepanjen, Kromengan and Gondanglegi district. The study area consists of
major subsurface litho units like sand, silt, clay, tuff, limestone and andesit. In order
to explore the groundwater resources of the study area with an aerial extent of 100
km2, electrical soundings have been conducted by adopting Schlumberger technique
in 12 locations with AB/2 200 m and 5 resistivity profiles were acquired. The field
data were interpreted and processed qualitatively and quantitatively by using
computer software. Considering the geological, geomorphology and hydrogeological
conditions the VES interpretation was done. The study has shown that the region is
underlain by 5 geoelectric layers within the depth penetrated. The groundwater
potential in South Malang reveals four distinct classes (zones) representing ‘Very
good’, ‘good’, ‘moderate’ and ‘poor’ groundwater potential in the area. From the
interpretation result the VES no. 7 (Pagak), and VES no. 9 (Kepanjen) are found to be
prospective for groundwater. It’s also identified that Groundwater occurs under
water table conditions the depth of water table ranges from 5 to 30 m.
Keywords: Identification, Groundwater and VES Method
Cite this Article: Moh. Sholichin and Tri Budi Prayogo, Field Identification of
Groundwater Potential Zone by VES Method in South Malang, Indonesia,
International Journal of Civil Engineering and Technology, 10(2), 2019, pp. 999-
1009.
http://www.iaeme.com/IJCIET/issues.asp?JType=IJCIET&VType=10&IType=02
1. INTRODUCTION
Ground water is one of the most essential natural resources to support human health,
economic development and ecological diversity. Due to its several inherent qualities (e.g.

widespread and continuous availability, excellent natural quality, limited vulnerability, low
development cost and drought reliability), it has become an important and dependable source
of water supplies in all climatic regions including both urban and rural areas of developed
and developing countries [1].
Study of groundwater geology is much useful for all the activities of human life.
Groundwater is more advantageous than the surface water. Water scarcity problem affects the
human chain and other living things. To meet out the demand of water, people are depending
more on aquifers [2]. There are two end members in spectrum of types of aquifers; confined
and unconfined (with semi confined aquifer being in between them) [3].
The study area is mainly covered by limestone and hard rock formations, and faces acute
water scarcity problem. Occurrence of groundwater in this type of area is limited to fractured
and weathered horizons and upper unconsolidated materials. For identifying the groundwater
potential in the hard rock terrain, the main target is fractured zone. The present study focuses
on identification of fracture zone and its thickness by using geoelectrical resistivity method.
The electrical resistivity method is a geophysical method that has been successfully used
by several researchers for groundwater investigations [4, 5, 6, 7]. Other geophysical methods
used to delineate groundwater potential zones include geotechnical, hydrogeological, remote
sensing, and geographical information systems (GIS) [8, 9]. However, some of these methods
lack the precision of an insitu analysis. The electrical resistivity method is usually preferable
because of the resistivity contrasts obtained when the groundwater zone is reached. Evidence
show that this technique has been successfully employed for delineating/mapping of geo-
materials in the subsurface that guides exploration of groundwater resources [10, 11, 12, 13].
Surface electrical resistivity surveys were conducted at different locations to obtain
subsurface lithological information, identification of horizontal and vertical disposition of
aquifer system [14]. The main objective of the investigation is to delineate the subsurface
lithology and to assess the groundwater resources of the study location. It also aims to focus
on the identification of fracture zone and its thickness by using VES (Vertical Electrical
Sounding) method. It is therefore expected that the results obtained from this work would
produce detailed groundwater condition and recommend areas within the observatory were
deep tube wells could be located.
1.1. Study Area
The present study area has falls in South Malang, East Java, Indonesia (Fig.1). The study area
lies between the latitudes South 8°08’50,8” to 8°13’37,1” and the longitudes East
112°31’22,5” to 112°38’49,2”. The present study area occupies an aerial extent of 100 sq.km
and the relief ranges from 317 m to 531 m above MSL. The study area receives an average
annual rainfall of 1950 mm and the average annual temperature is 26,9°C.

Field Identification of Groundwater Potential Zone by VES Method in South Malang, Indonesia
Figure 1 Location Map of Study Area and Data Collection
The study area is located in the southern slope regional uplift, also known as the southern
mountains. Based upon this limited evidence, the basement has been interpreted to be arc and
ophiolitic rocks of Cretaceous age. A volcanic arc was built upon basement rocks from the
middle Eocene to the Miocene [15, 16]. It constitutes of the old andesite volcanic and
volcaniclastic suite, initially interbedded with and then more completely overlain by Miocene
limestones [16. 17]. These limestones often develop as reefal facies. The limestones show
different depth of weathered zone. In the study area groundwater occurs under water table
conditions in the joints, fractures and weathered rocks. Generally, the limestones of the study
area are highly massive and compact and devoid of joints and fractures making it impervious,
which in turn result in poor potential.
2. MATERIALS & METHODS
Geophysical prospecting of groundwater comes under both surface and subsurface
exploration. Under geophysical prospecting, one of the electrical methods is Schlumberger
array of electrical resistivity method. The Schlumberger array was used to ensure deep
penetration and for logistics of limited man power in the field [2]. Schlumberger
configuration using microprocessor based signal stacking digital resistivity meter of Martiel
Geophysics, Type MGG 020520. Both the survey procedures resistivity profiling and
resistivity sounding (VES) have been carried out. VES has been conducted at 12 locations
with AB/2 200 m and 5 resistivity profiles were acquired. The resistivity data have been
qualitatively and quantitatively interpreted and analyzed by software packages.
2.1. Resistivity Method
The electrical resistivity is the resistance offered by the opposite faces of a unit cube of
material to direct current is called as resistivity. In geophysical literature the unit of resistivity
is taken as the ohm. m. The resistance (R) of the material having a resistivity (ρ) over a length
(L) and surface area of current flow (A) is given by R = ρ L/A. This is governed by Ohms
law. The inverse of resistance is termed as conductance [18].

2.2. Measurement of Resistivity
In general for measuring the resistivity of the sub surface formation four electrodes are
required. The current of electrical intensity (I) is introduced between one pair of electrodes
called current electrodes which can be identified as A & B. The potential difference produced
as a result of current flow is measured with help of another pair of electrodes called potential
electrodes represented as M & N. Let Δr represent the potential difference. The apparent
resistivity measure is K x Δv/I , where K represents geometrical constant, which can be
calculated if we know the electrode arrangements. The basic needs for the resistivity survey
are the power source, meter to measure current and potential, electrodes and cables.
2.3. Schlumberger Configuration
In schlumberger configuration all the four electrodes are kept in a line similar to that of
Wenner but the outer electrode spacing is kept large compared to inner electrode spacing
usually more than five times. For each measurement only the current electrodes are moved
keeping the potential electrodes at the same locations. The potential electrodes are moved
only when the signal become too weak to be measured. The apparent resistivity for this
configuration is computed with the formula:
Ρ = {[(AB/2)2 – (MN/2)2)/MN] x πR}
Figure 2 Schlumberger Configuration
2.4. Vertical Electrical Sounding (VES)
A series of measurements of resistivity are made by increasing the electrode spacing in
successive steps about a fixed point. This method of vertical exploration is known as the
expanding electrode method, “resistivity sounding” or “depth probing” or vertical electrical
sounding (VES). The apparent resistivity values obtained with increasing values of electrode
separation are used to estimate the thickness and resistivities of the subsurface formations.
VES mainly employed in groundwater exploration to determine the disposition of the
aquifers.
2.5. Geoelectrical Parameters
The main objective of the quantitative interpretation of VES curve is to obtain the
geoelectrical parameters. A geoelectric layer is called by its fundamental characters,
resistivity ‘ρ’ and thickness ‘h’. These two parameters are called the primary geoelectrical
parameters. The secondary geoelectrical are also important to describe the geoelectric section
consisting of several layers. The longitudinal (S) and the total transverse (T), transverse
resistivity (T/h) an – isotropy (λ) are called the secondary geoelectrical parameters.

3. RESULT AND DISCUSSION
The field data were interpreted and processed qualitatively and quantitatively by using
computer software to obtain the resistivity values of different subsurface layers and their
corresponding thickness (Table 1).
3.1. Interpretation of Resistivity Data
The interpretation of resistivity data is done in two stages, 1. Processing of data to get the
geoelectric parameters, and 2. These parameters are used to infer the nature of surface
lithology on the basis of the local geological knowledge and correlation studies.
3.2. Quantitative Approach
The quantitative approach is to get the geoelectric parameters i.e., the true resistivity, layer
thickness, etc. The VES data of the study area have been qualitatively and quantitatively
analyzed and interpreted using software IPI2WINTM version 2.6.3, a Russian software
package of Moscow University. By using Surfer 10TM, resistivity contour maps have been
generated for different depth ranges to identify and demarcate the anomaly zones. The
IPI2WIN software is used to prepare the VES curves, pseudo sections, geoelectric profiles
and geoelectric sections [15].
Table 1 Summary of VES data interpretations with positions
VES Location
ρ1
(Ωm)
ρ2
(Ωm)
ρ3
(Ωm)
ρ4
(Ωm)
ρ5
(Ωm)
h1
(m)
h2
(m)
h3
(m)
h4
(m)
Error
(%)
1 Pagak 1 34.7 12.7 73.3 19.4 1500 1.5 27.5 24.5 56.8 9.9
2 Pagak 2 28.1 10.1 22.2 9.2 1257 1.5 16.8 26.0 31.1 8.7
3 Pagak 3 55.9 14.0 56.3 18.0 308 1.4 3.2 3.0 116.0 11.0
4 Pagak 4 30.3 5.7 46.8 23.3 256 7.3 9.6 16.3 18.7 13.2
5 Kepanjen 46.9 13.5 311.0 5.9 126.0 3.6 10.1 7.3 7.8 5.9
6 Kepanjen 24.9 15.8 64.2 4.5 123.0 1.3 11.1 8.8 4.7 4.3
7 Kromengan 20.7 5.3 43.0 2.7 117.0 2.3 1.7 3.4 5.7 9.5
8 Kromengan 21.5 15.4 60.0 12. 553.0 1.3 16.5 4.0 101.0 2.9
9 Gondanglegi 62.5 60.7 8.4 152 6134.0 6.6 0.6 4.2 54.4 7.7
19 Gondanglegi 28.1 14.7 25.7 135.0 9042.0 3.5 4.6 10.6 24.5 10.8

Figure 3 Interpretation of Vertical Electrical Sounding Field Curves
3.3. Isoresistivity Maps
The isoresistivity maps are the resistivity contour maps. Accordingly the layer thickness
contour maps of the study area have been generated incorporating all the 30 VES data for
different formation with their co-ordinates, joining equal layer thickness of the depth of

investigation. The resistivity contour map for first layer, second layer, third layer, fourth layer
and fifth layer were generated (Fig. 5 - 9). The difference between two consecutive contour
lines is termed the contour interval. The contour maps can be generated using Surfer 10TM
software packages. The isoresistivity maps can be used for qualitative interpretation of the
groundwater and by quantity by demarcating the low and high layer thickness anomalous
zones. The method of qualitative and quantitative interpretations helps us identify good
ground water potential zones.
Figure 4 a. Isoresistivity Map of The 1st layer, b. Isoresistivity Map of The 2nd layer, c.
Isoresistivity Map of The 3rd layer, d. Isoresistivity Map of The 4th layer, e. Isoresistivity
Map of the 5th layer
a b
c d
e

3.4. Geoelectrical Profiles
All the 12 VES locations studied were made into 5 profiles covering the entire study area (Fig
A-E) with definite orientations, traversing different geological formations to project a two
dimensional subsurface geoelectric section along that profile. All these geoelectric profiles
have been generated by IPI2WINTM software package. The geoelectric profiles are the
geoelectrical section of each VES locations united into one profile with a definite directional
orientation. Each geoelectric profile has two profiles namely Pseudo section displaying the
apparent resistivities at different depths below ground level from surface to 200 m depth and
the other section with thickness of different geoelectric layers below ground level. The
resistivity sections only reflect the interpreted subsurface lithology. The ordinate ‘X axis’
represent the distance of traverse and the abscissa ‘Y axis’ represent the depth in meters
below ground level.
Figure 5 VES Profile Map of The Study Area
Profile – I
The profile-I located in south side of Brantas River. It belongs to Sumberbening groundwater
basin. The location considered for this profile is Pagak district. The traverse of the profile is
west to eastern part of the study area (Figure 5).
Profile – II
The profile-II located in south side of Sengguruh Reservoir and south side of Lesti River. It
belongs to Sumberbening groundwater basin. The location of this profile includes Pagak and
Bantur district. The traverse of the profile is south to northern part of the study area (Figure
5).

Profile – III
The profile-III located in north side of Sengguruh Reservoir and north side of Brantas River.
It belongs to Brantas groundwater basin. The location considered for this profile is Kepanjen
district. The traverse of the profile is south to northern part of the study area (Figure 5).
Profile – IV
The profile-III located in north side of Sutami Reservoir and north side of Brantas River. It
belongs to Brantas groundwater basin. The location considered for this profile is Kromengan
district. The traverse of the profile is west to eastern part part of the study area (Figure 5).
Profile – V
The profile-III located in east side of Brantas River. It belongs to Brantas groundwater basin.
The location considered for this profile is Gondanglegi district. The traverse of the profile is
east to western part of the study area (Figure 5).
4. CONCLUSION
Vertical Electrical Sounding using Schlumberger electrode configuration was conducted in
South Malang, East Java, Indonesia to determine the underground water potential and the
lithological setting in terms of aquifer distribution. The study has shown that the region is
underlain by 5 Geo-electric layers within the depth penetrated. The groundwater potential in
South Malang reveals four distinct classes (zones) representing ‘Very good’, ‘good’,
‘moderate’ and ‘poor’ groundwater potential in the area. The very good groundwater
potential zone mainly encompasses good be recharged along the river alluvium. The good
groundwater potential zone mainly covered by regions with groundwater in joints & some
quantity of ground water will be recharged held in the weathered zone subsequently fractured
planes. It’s also identified that Groundwater occurs under water table conditions the depth of
water table ranges from 5 to 30 m. Groundwater recharge takes place through precipitation of
rain water aided by morphological features of ground surface around the major river systems.
It’s also demarcated that the areas in the upper part of the study area is not suitable for
groundwater storage and also indicates the deep availability of water very below the ground.
The poor groundwater potential is due to the higher slope and unfavorable geology and
geomorphology in this zone. These prospective groundwater zones can provide a basis for the
detailed hydro-geologic and/or geophysical investigations needed for well sitting and proper
management of scarce groundwater resources.
ACKNOWLEDGEMENTS
I would like to express my appreciation to University of Brawijaya and Malang Regency
officer for providing secondary data and interview season with local community.
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