The Imo State Government has carried out some water projects in the area in which huge sums of money were invested. The Okigwe regional water scheme sited in Onuimo Local Government Area is still not functional in terms of supplying potable water from Imo River channel. There are many failed boreholes in the area in places like Uturu Isukwunato (in old Okigwe District), Umunakanu Ehime and some other areas around Okigwe as the geology of these areas is predominantly clay and shale. Areas around Avutu fall within the transition zone of Benin Formation to Bende Ameki group, Amuzu Ihube in Okigwe falls within the portion of Ajali Sandstones where the clay and shale members are predominant. The complex geological setting of the area especially around the northern part may have accounted for the failure of boreholes. Hence, proper geophysical survey of the study area is required.
MATERIALS AND METHODS
Geology of the study area: Okigwe District is in Imo State of Nigeria. The District is made up of six Local government Areas; Isiala Mbano, Ihitte Uboma, Ehime Mbano, Onuimo, Obowo and Okigwe. The area lies between latitude 5°30-5°57N and longitude 7°04-7°26E (Fig. 1) covering a land area of about 1,824 km2. There is a good network of roads within the area. The major roads include the Umuahia-Enugu express road that passes through Ezinachi, Okigwe and Ihube. The major roads that link the various Local Government Areas include the tarred and untarred roads.
The study area is a complex geological environment in Imo State. The following
stratigraphic units underlie the area: the Benin Formation, the Ogwashi - Asaba
Formation, the Bende-Ameki Formation, Imo Shale Formation, Nsukka Formation
and Ajali Formation (Akaolisa and Selemo, 2009; Nwosu
et al., 2010). The Benin Formation is overlain by lateritic overburden
and underlain by the Ogwashi - Asaba Formation which is in turn underlain by
the Ameki Formation of Eocene to Oligocene age (Mbonu et
al., 1991). The Benin Formation consists of coarse-grained gravelly
sandstones with minor intercalations of shales and clay. The sand units which
are mostly coarse grained, pebbly and poorly sorted contain lenses of fine grained
sands (Onyeaguocha, 1980; Short
and Stauble, 1976). The Southern part of the study area covering Obowo,
Southern part of Ehime Mbano and Isiala Mbano fall within this formation.
The Ogwashi-Asaba Formation is made up of variable succession of clays, sands and grits with seams of lignite. It also forms part of the study area. The Ameki Formation consists of greenish-grey clayey sandstones, shales and mudstones with interbedded limestones. This Formation in turn overlies the impervious lmo Shale group characterized by lateral and vertical variations in lithology. The lmo Shale of Paleocene age is laid down during the transgressive period that followed the Cretaceous. It is underlain in succession by Nsukka Formation, Ajali Sandstones and Nkporo Shales.
Field measurement procedure: A total of 120 Vertical Electrical Soundings
(VES) were carried out in the study area (Fig. 1) using the
Schlumberger electrode configuration and a maximum current electrode spacing
of 900 m. Twelve of the VES stations were sited near existing boreholes to enhance
interpretation. The ABEM Terrameter (SAS) 300 B was used to acquire data. It
has a liquid crystal digital read-out and an automatic signal averaging microprocessor.
Four stainless non polarizable electrode were used, two current electrodes and
two potential electrodes. A freshly charged 12 V DC battery was used to supply
current. The current electrode spacing was increased symmetrically about the
station point, keeping the potential electrode constant until it became necessary
to increase the potential electrode as the recorded signal diminished. The apparent
resistivity values computed were plotted against half of the current electrode
spacing (L/2) on a log-log graph scale. The sounding curves obtained were subjected
to conventional partial curve matching using the Rijks Waterstaat
(1975) master curves to obtain the initial model parameters (resistivities
and thickness) for computer aided interpretation. The software package used
is the Schlumberger automatic analysis version 0.92 (Henker,
THEORETICAL BASIS OF THE STUDY
The two principal quantities used to determine a geoelectric layer are the
resistivity pi and thickness hi where i = the position
of the layer (Zhody, 1965). Other parameters include
longitudinal conductance, transverse resistance and coefficient of anisotropy
all of which are derived from the layer resistivity and thickness.
||Map of study area showing sounding stations and interpretative
geolectirc cross-section (IGCS) traverse
Given a column of unit square cross sectional area cut out of group of layers of infinite extent, the total transverse unit resistance R is given as:
The total longitudinal unit conductance:
where, pi and hi are the resistivities and thickness of the ith layer. The average longitudinal resistivity:
and the average transverse resistivity:
The coefficient of anisotropy is the square root of the ratio of pt to pL.
The longitudinal conductance Si can also be represented by:
where, σi is the layer conductivity which is analogous to the
layer transmissivity, Tri used in groundwater hydrology (Mbonu
et al., 1991), given by:
where, Ki is the hydraulic conductivity of the ith layer of thickness
hi. The parameters R and S are called the Dar Zarouk parameters which
have been proved to be very powerful in enhancing the interpretation of groundwater
surveys (Zhody, 1965).
The relationship between aquifer transmissivity Tr and transverse
resistance R and that between Tr and S have been derived analytically
by Niwas and Singhal (1981) as follows:
Tr = Kσ
In areas where the geologic setting and water quality do not vary greatly the
product Kσ remains fairly constant (Niwas and Singhal,
1981). Hence, if the values of K from the existing boreholes and σ
from the sounding interpretation around the borehole are available, it is possible
to estimate the transmissivity and its variation from place to place from the
determinations of R or S for the aquifer.
Fetter (2007) relation for obtaining storativity from
pumping test data can be written as:
where, u is determined from well function:
||Radial distance from the pumping well to the observation well
Chatterjee (2005) relations for specific capacity of
wells can be modified by appropriate substitution as:
SC = 0.85 kh
RESULTS AND DISCUSSION
The survey revealed multi geoelectric layers. There is marked variation in
resistivity with depth across the entire study area. The geoelectric section
compared with the borehole lithology gave the resistivity of the probable aquifer,
the depth to aquifer, the aquifer thickness as well as aquifer depth which varied
across the area. The aquiferous zones occur most in the fourth and the fifth
geoelectric layers. Typical modeled curve, the geoelectric section and lithology
are shown in Fig. 2 for VES 32 near Anara borehole in the
South and for VES 119 near Ihube Okigwe borehole in the Northern part of the
area (Fig. 3). The curves are a combination of H- type and
K-type (Ekine, 2010) and HKH-type and KQH-type (Oseji
et al., 2005).
The hydraulic properties determined from the boreholes are displayed in Table
1. Parameters 1-6 are determined on the basis of pumping test while 7-15
were determined on the basis of VES results. Although, the computation was based
on the screened portions of the aquifer, the close agreement between parameters
2 and 15 for Madona II borehole attest to the reliability of the VES results.
The table compares aquifer characteristics determine from pumping test data
with those obtained from VES results. Transmissivity and specific capacity values
are least for Umunumo boreholes with magnitude of 25.4950, 21.6707 m3
day-1, respectively. This area falls within the Bende Ameki Formation.
The Formation is aquiferous but groundwater exploitation is sometimes difficult
due to high percentage of shale (Nwosu et al., 2010).
However, the transmissivity values determined from VES results (parameter 14)
are fairly uniform and relatively high for the boreholes sampled.
Table 2 is the summary of aquifer characteristics obtained from VES 101-120. Low aquifer resistivity value of 667 Ωm was recorded for VES 120 near Akpugo. The aquifer is relatively thin in the Northern part but thick in the Southern part aquifer thickness of 9.4 m is recorded for VES 116 near Umuduru while the highest thickness of 104.4 m is obtained in the Southern part of the district.
The transmissivity values obtained for the study area varied from 992.04 m2
day-1 (VES 120) obtained in the Northern area (Table
2) to 10263.65 m2 day-1 obtained in the Southern part
(VES 89). Generally transmissivity values increase southwards.
||Model curve, geoelectric section and lithology of VES 32 near
Anara Borehole (a) Model curve, (b) Geoelectric section and (c) Lithology
The storativity values range from 1.59x10-4 observed in the Northern
part of the Study area around VES 118-7.80x10-3 recorded in the Southern
part at VES 98. The trend in the variation of transmissivity and storativity
values is consistent with the geology of the area. The Southern part where the
higher values of transmissivity and storativity are obtained, fall within the
coastal plain sands (Benin Formation) which is made up of alternating layers
of sands, sandstones and loams of clays (Nwankwo et
||Model curve, geoelectric section and lithology of VES 119
near lhube Okigwe Borehole (a) Model curve, (b) Geoelectric section and
As the sandy components form more than 90% of the sequence of layers, permeability,
transmissivity and storage coefficients are high. The high transmissivity values
recorded in the South and Southwestern area covering Isiala Mbano, Ehime Mbano,
Ihitte Uboma and Obowo where higher values of aquifer thickness are observed
agrees with the expected result as transmissivity is a function of aquifer thickness.
There is little the top layers are generally not continuous and show large variations
in layer resistivity.
||Aquifer characteristics calculated for some boreholes located
in the study area
||Summary of aquifer characteristics for all the sounding stations
showing depth to water table
These layers correspond to the brown to reddish lateritic overburden interspersed
with sandy soils, sandy clay with humus observed around Onuimo area (VES 14,
19, 29) along AB (Fig. 4) and VES 6,11,12 along CD (Fig.
5). Part of the top layers have been greatly weathered which gave rise to
high resistivity as observed around Ndioji (VES 2) and Uboma (VES 74). The deeper
layers are more continuous than the shallow layers.
|| Interpretative geoelectric cross-section (IGCS) along profile
|| Interpretative geoelectric cross-section (IGCS) along profile
The second and third layers are composed of red lateritic soil, coarse to medium
sand and clay. The fourth layer consists of fine medium coarse sands, sandstone
and sandy shale. This layer constitute the major aquifers zone. The cross sections
reveal the presence of shallow and deep aquifers. Along profile AB, the resistivity
of the aquifer varied from 101 Ωm observed around Umuduru Egbeaguru (VES
14) to 13800 Ωm at Ndimoko (VES 8). The aquifer thickness varies from 4.2
m around VES 11-104.4 m around VES 95 where it is thickest.
The aquiferous layer is underlain by conductive layer composed of clays and/lignite
and shale. In some locations the aquifer extends deeper into this layer as observed
in VES 86 and 88 around Avutu (Fig. 5). The geoelectric cross-section
also reveals the presence of confined aquifer around Onuimo (Fig.
6). This agrees with the geology of the area as the aquifer occurs between
impervious clay layers. Oseji et al. (2005) used
this technique successfully to investigate the aquifer characteristics and groundwater
potential in Kwale, Delta State, Nigeria. Table 3 summarizes
the range of values of some hydraulic properties computed for the study area,
their location and their implications.
|| Summary of the range of variation of hydraulic properties
for the study area and their implications
|| Igeolectric cross-section (IGCS) along profile line GH
|| Isopach map of the aquiferous zones in the study area
Isopach map of the aquiferous zone: The Isopach map of the major aquiferous zone constructed from the VES results (Fig. 7) shows that the aquifer thickness varies across the entire area. There are isolated closures suggesting discontinuities in the aquifer systems. The aquifer is thin in the northern part of the area covering Okigwe and parts of Onuimo areas with values of about 9 m recorded at VES 115 and 116 located at Umueze and Umule, respectively. The aquifer thickness increases down the Southern part of the study area. The highest value of aquifer thickness of 104.4 m is recorded at VES 95 located at Amanzo, in Obowo in the South-South part of the district.
Generally, the aquifer is thick enough in the Southeast, Southwest and South-South parts of the study area for drilling productive boreholes.
Layer resistivity contour map of the aquiferous zone: The layer resistivity contour map of the major aquiferous zone constructed for the area (Fig. 8) shows marked resistivity variations across the district. The low aquifer resistivity values ranging from 16-2382 Ωm recorded around the Northern part covering part of Okigwe and Onuimo Local Government Areas in the Central and Northwestern parts is consistent with the nature of the depositional environment. The area is underlain by clay, clay-shale members. Separating this zone from higher resistivity aquifer horizon in the North-eastern part having resistivity values ranging from 11200 Ωm at Ogwuoko (VES 102) to 23160 Ωm observed at Umuduru (VES 116) is resistivity value of about 5000 Ωm. The boundary coincides with the channels of Nterere, Odioma and Alum Rivers that flow into the Imo River. Demarcating these two zones also from the Southern high resistivity aquifer system is also resistivity value of about 5000 Ωm, coinciding with the channels of Efuru and Eze rivers that drain the area.
|| Layer resistivity contour map of the aquifers zone
The sharp variations in resistivity observed in the South-South zone covering
Obowo L.G.A. could be attributed to the inhomogeneous nature of the thick aquifers
in the region and the water quality within the aquifer. Ekine
and Iheonunekwu (2007) obtained similar result in Mbaitoli area of Imo State
which is in the same geological environment with the Southern part of the study
Groundwater potential evaluation: Evaluation of groundwater potential
of an area can be based on the characteristic aquifer geoelectrical parameters
obtained from VES interpretation results and borehole hydrogeological information
(Olorunfemi et al., 1999; Ekwe
et al., 2006). Based on the groundwater yield of the boreholes determined
from pumping test data, aquifer geometry, longitudinal conductance, transmissivity
as well as storativity values, groundwater potential map of the study area was
produced (Fig. 9).
The aquifer system in Zone A in the Southern part has the highest yield; 8292
m3 day-1 recorded at Isinweke (VES 79), 4364 m3
day-1 recorded at (VES 88), 1746 m3 day-1 recorded
at (VES 41) and 5237 m3 day-1 observed at Umuelemai. These
clearly indicate that the southern part of the district is the most prolific
in terms of groundwater exploitation and thus the most promising in sitting
productive boreholes. This zone correspond to the area of high aquifer transmissivity
and thickness. In terms of longitudinal conductance this area is underlain by
thick and high conductance aquifer materials and thus are good prospects for
drilling boreholes. This area also recorded the highest value of storativity.
These results are consistent with the observations made by Ekwe
et al. (2006) around Obowo in a similar study of Imo River basin
aquifers. The study covered Umuahia and part of the South-South part of Okigwe
|| Groundwater potential map of the study area
The Northeastern part of Okigwe (Zone A1) can be classified as Zone A based on the Kä and longitudinal conductance values as well as the transmissivity values. However, the groundwater yield of borehole located at Okigwe gives a value of 327 m3 day-1 which is much lower than that in the zone located in the southern part of the study area. This variation could result from the complex nature of the depositional environment as there is marked difference in the transverse resistance values, aquifer thickness being lower coupled with the lower values for storativity observed in this North-eastern part of Okigwe (Zone A1). Hence, this area is not as prolific in terms of groundwater exploitation as that in the southern part of the district. Zone B is the next promising for groundwater exploitation or medium groundwater potential. Zone C is the low groundwater potential area while part D is a difficult area for groundwater exploitation.
This study has succeeded in evaluating the groundwater potential of the complex geological area of Imo State and mapped the aquiferous zone. It has also delineated sites for productive boreholes from VES results. The Southern and Northeastern parts of the district are more promising for siting borehole with high yield expectations than the North Western part as there is no well defined sand body that constitute aquifer there. The occurrence of aquifer in this area is linked to the presence of fracture in the shale members.
The research group is grateful to the Imo Water Development Authority (IWADA) and the Imo Water Board for supplying the relevant Pumping Test data and hydrogeological information that enhanced this study.