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Original Scientic Article • DOI: 10.2478/rmzmag-2021-0015 Received: March 05, 2022
Accepted: March 24, 2022
Moussa Diallo1,2, Ahmed Amara Konaté1,2,*, Mory Kourouma1,2, Fassidy Oularé1,2, Muhammad Zaheer3
1Laboratoire de Recherche Appliquée en Géoscience et Environnement, Institut Supérieur des Mines et Géologie de Boké,
BP84, Boké, Baralandé, Republic of Guinea
2Centre Emergent Africain Mines et Société, Institut Supérieur des Mines et Géologie de Boké, BP 84, Baralandé,
Republic of Guinea
3Department of Earth & Environmental Sciences, Hazara University Mansehra 21300, Khyber Pakhtunkhwa,
Republic of Pakistan
*Corresponding author: E-mail: konate77@yahoo.fr
Clean drinking water supply is a major concern to the
population of the urban municipality of Boké, Repub-
lic of Guinea. This study is aimed to investigate the
favourable geological structure for the accumulation
of groundwater in Boké. Apparent resistivity data was
collected by using the Schlumberger-type vertical
electrical sounding technique. The apparent resistiv-
ity values were obtained on a bi-logarithmic scale in
which the distances AB/2 were plotted on the abscis-
sa and the resistivities are on the ordinate. It found the
number of terrains and their characteristics (resistiv-
ity and thickness) in the area and the behaviour of the
current in the soil through a curve. The results show
that the structures favourable to the accumulation of
groundwater were fractured dolerites, cracked shales
and cracked or crushed sandstones. The sandstones
were the most important in terms of the amount of
water. They are located at a depth of more than 100
metres. It was also found that dolerites and shales are
located at shallower depths (less than 100 m).
Groundwater, geo-electric method, litho-
logical section, fracture zones, Prefecture of Boké
podzemna
-
Diallo et al.
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RMZ – M&G | 2022 | Vol. 69[2] | pp. 1–17
Several studies of different methods have
been carried out in the area for the research of
groundwater in order to ensure the supply of
drinking water to the population. [3] conduct-
ed a study of the groundwater research project
on the Boffa geological sheet and examined the
characteristics of the different aquifers by us-
ing geophysical methods composed of seismic
refraction, electrical sounding, profiling by the
two-spaced device and resistivity logging. In
the same vein, [2] carried out studies to deter-
mine the best geophysical method and stated
that the most suitable were electrical meth-
ods (electrical drag and sounding), the seismic
method (seismic refraction), and the magnet-
ic method (magnetic profile). In addition, the
National Water Point Development Service
(SNAPE) carries out village hydraulic boreholes
each year in the Boké region to fill the void of
drinking water. These boreholes are carried out
based on classical methods supported by the
interpretation of aerial photos and geomorpho-
logical observations (talweg line, valley, slopes,
etc.). As a result, it records a rate of failure or
low flow boreholes of around 25% [4].
The electrical resistivity survey such as
the Schlumberger configuration enables the
changes of apparent resistivity with depth to
identify the water-saturated bodies, which are
characterized by lower resistivity zones [5].
The resistivity value is changed corresponding
to water content in the geological materials.
The fracture’s features are usually filled with
groundwater and have a lower resistivity val-
ue of the rock layer than water-bearing strata
[6]. According to [7], the four-electrode quad-
rupole (AMNB) of Schlumberger is considered
satisfactory by technicians in previous studies
and remains the most widely used.
From the analysis of the aforementioned
studies, it appears that they rarely use meth-
ods to decrease the failure rate and obtain
high-throughput boreholes; others propose
very complex and expensive methods that do
not take into account certain important pa-
rameters (depth of aquifers, types of aquifers
with high flow rates, the forms of the anomalies
sought, lead time, etc.).
When proposing a method or a complex of
methods for investigating groundwater, several
factors must be taken into account, including
The urban municipality of Boké which is the
subject of this study, like the rural municipal-
ities of Boké, benefits from significant mining
investments due to the presence of several
bauxite deposits in its surroundings. In recent
years, a dozen mining companies have settled
there. This also justified its designation as
a special economic zone of Guinea through
the decree of April 25, 2017. The presence
of companies has led to a population growth
in recent years. The population of the prefec-
ture increased from 760,119 inhabitants in
1996 to 1,092,291 inhabitants in 2014 before
reaching 1,157,540 inhabitants in 2016 [1].
This exponential population growth has had
consequences on the socio-economic activ-
ities of local populations. Access to basic
social services (electricity, water and health)
is a real problem these days. Referring to
[1], compared to previous years and to other
regions of the country, the population of Boké
has experienced a decline in its accessibility
to drinking water. Its water accessibility rate
fell from 71.3% in 2007 to 48.3% in 2012.
However, the country average was 67.8% in
2012. Regarding domestic consumption in the
Boké region, the rate is 8.3% against 10.6% in
the country. The rate of village hydraulic bore-
holes in the region is 25.5% against 35.3% for
the country [1].
Groundwater is found below the surface of
the earth within the saturated layers of sand,
gravel and pore spaces in sedimentary as
well as crystalline rocks. Surface water (riv-
ers, lakes) and superficial aquifers (perched
aquifers), which constitute the current main
sources of supply, are rapidly drying up due
to climate change (drought), human activities
(deforestation, salt extraction, charcoal pro-
duction, aggregate extraction, etc.), and mining.
In addition to rapidly drying up, these waters
are affected by pollution in the vicinity of large
cities and mining facilities [2]. Hence the need
to seek out and exploit new sources of drinking
water for the population, such as water from
deep fractures. Being deep, sufficient in quan-
tity, and less polluted, these waters are suitable
for supplying agglomerations and industrial
installations.
Identication of favourable geological formations for the determination of groundwater
3
ease of use, reliability, speed and cost. With
this logic, [8] used the geophysical method to
determine the productivity of boreholes in
the Toumodi region (Côte d’Ivoire). At the end
of this study, it was found that the coupling of
geomorphological and geophysical methods
reduces the negative drilling rate and optimiz-
es the exploitation of positive drilling. A study
carried out by [9] in Burkina Faso on the op-
timization of the geophysical implantation of
boreholes in the base area and focused on the
drilling and electrical drag improved the over-
all success rate by more than 10%. According
to [8] the geophysical investigation through
the survey and electric train carried out in
Côte d’Ivoire (Center-North) made it possible
to identify the structures and characterize the
aquifers (thicknesses of the alteration and the
depth of the cracked horizon) of this region.
In another study by [10] carried out in Tanda
(eastern part of the Ivory Coast), the use of geo-
physical prospecting by electrical resistivity for
the search for groundwater made it possible to
determine with good precision the exact posi-
tion of conductive anomalies and several frac-
tures of a different direction.
[11] found that the geoelectric survey of
Schlumberger types gives good results in the
characterization of subsurface structures.
Similarly, [12–15] have each in the context of
their studies demonstrated the reliability of
geoelectric soundings in determining the nature
of geological layers and aquifers. Geophysical
methods were proved to be the most active
technique in the exploration of groundwater
resources. With a support borehole parame-
ter and their interpretation from the resistiv-
ity imaging method, consistent information
regarding the groundwater can be produced.
From the above development, it appears that
geophysical methods are appropriate for the
siting of boreholes to decrease the failure rate
and achieve high throughput boreholes. This
work, therefore, aims to precisely locate areas
or structures favourable to the accumulation of
groundwater in the urban municipality of Boké.
The first part of this work will focus on the
overall presentation of the study area; the ma-
terials and methodology used will be described
in the second part; the results obtained will be
presented and interpreted in the third part, and
a conclusion accompanied by perspectives will
bring this work to a close.
Study area
Our study area is located between 14°00’ and
15°00’ West longitude; 10°00’ and 11°00’ North
latitude. Figure 1 shows the location map of the
study area.
In terms of relief, soil, vegetation, climate
and economy, the study area is characterized
by plains, plateaus, hills and lowlands with an
elevation ranging from -5 m to 217 m. The relief
map is shown in Figure 2.
The soil is lateritic skeletal, hydromorphic
and alluvial; the soil texture is: clay 0–45%,
sand 20% approximately, silt 30% approxi-
mately; the soil is permeable and porous in
places [16].
Most of the area is covered with wooded sa-
vannah. Trees characteristic of the tropical for-
est are located in a narrow band along the river
valleys, both on the slopes and on the tops of
the hills. The plateaus are characterized by her-
baceous and tree vegetation [17].
The Boké area has a tropical climate with
two seasons, each of which lasts six months
(the dry season from May to October, and the
rainy season from November to April). With 0
millimeters of precipitation, December is the
driest month. With an average of 613 mm, the
month of August records the heaviest rainfall.
The inter-annual average of precipitation is
2,227 mm [17].
March is the hottest month of the year with
an annual temperature of 33.5 ° C in 2019 and
the coldest month is January with an average
temperature of 22.2 ° C in 2019 [16].
The main economic activities in the study
area are mining, agriculture, fishing, livestock,
transport and trade.
From the hydrographic point of view, the
urban municipality of Boké is watered by two
main rivers. They are the Cogon River, termi-
nated by the Rio Compony with a length of
390 km, and the Tinguilinta River, which forms
from the city of Boké the Rio Nuñez. In addition
to these two main rivers, many rivers water our
study region such as the Kassongony, Sangui,
Diallo et al.
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RMZ – M&G | 2022 | Vol. 69[2] | pp. 1–17
Figure 2: Elevation map of urban municipality of Boké (Boké centre).
Figure 1: Location map of urban municipality of Boké (Boké centre).
Identication of favourable geological formations for the determination of groundwater
5
of the North African platform occurred in our
study area. These Mesozoic intrusions are rep-
resented by dolerites, gabbro-dolerites, Congo-
diabases and gabbro-quartzes [18].
The Boké zone belongs to the West African
craton and its lands occupy part of the Bowé
syneclise. In Boké, the base does not outcrop
[18]. The Boké area is affected by two tectonic
faultts. Namely: the deep faults which served
for the rise of the basic magma, and the sec-
ondary faults developed on the cover. These
two faults constitute the current hydrographic
network.
According to [19], the study region is located
within the limits of three major morphological
zones: Fouta-Djalon plateau, coastal plain and
shelves.
From the hydrogeological point of view, our
study area belongs to the northwestern part
of Guinea which abounds in significant wa-
ter reserves fed by atmospheric precipitation
and by rivers [3]. The geological conditions
of the region make it possible to distinguish
two groundwater sampling environments:
bedrock and the superficial formations that
cover them. Mesozoic doleritic rocks and
healthy shales constitute the bedrock. In
Dolonkhi, etc. The hydrographic map is shown
in Figure 3.
Several major basins are shared in the study
area. In particular, the Batafon basin (7,478
hectares), the Tinguilinta basin (4,812 ha) and
the Nunez basin (2,761 ha) [17]. Based on the
nature of the slopes, the altitude of the sources,
the nature of the terrain and the seasons, the
regime of the waterways is irregular.
Geologically, our study area belongs to the
sedimentary cover. It was relatively calm with
great magmatic activity in the Mesozoic [18].
The terrigenous terrains of the Ordovician
(argillites, aleurolites and sandstones), Silurian
(quartz sandstones, schists, argillites, etc.),
and Devonian (sandstones, coarse-grained
aleurolites, etc.) are developed in the urban
municipality of Boké. These terrains are all
covered by unconsolidated deposits of marine
or lacustro-fluvial origin from the Paleogene
(represented in our region by clays, argillites
and quartz sands) and from the Quaternary
(the Quaternary formations are represent-
ed by different facies: Marine, continental,
lacustro-fluvial) [3].
An intense eruptive activity dating from the
Mesozoic and due to the tectonic movements
Figure 3: Hydrographic map of urban municipality of Boké (Boké centre).
Diallo et al.
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these formations, water is linked to cracking
or crushing zones [2].
In the study area, the waters of tectonic frac-
tures are generally attached to doleritic mag-
matic rocks and argillites which are fractured
and crushed by tectonic movements. These
areas are not well known, but they can be one of
the main sources of good quality water supply.
The study area contains several nappes in the
weathering crust. This is evidenced by the high
number of artisanal wells in all settlements and
the presence of groundwater sources in the
area [2]. The geological map of the urban com-
mune of Boké is shown in Figure 4.
Materials
For the collection of geophysical data, a com-
pact RSP6 resistivity meter of the SCINTREX
Canada type and its accessories were used
to determine the resistivity of the sites; a
Garmin-type GPS was used as a tool for the
geo-referencing of the measurement points;
and WINSEV software (version 6.4) was used
for data processing.
Methods
To achieve our objective, a geophysical sur-
vey was conducted on six sites (see Figure 5)
which were: Kissassi; Abattoire Palmeraie;
Tamakènè; Nema school complex; Kadiguira;
and Ballaya.
According to [20], in practice, the choice of
geophysical methods depends on:
−The nature of the sought target which
must cause an anomaly sufficient to be
measured;
−The quality of precision sought which must
correspond to the resolving power of the
method and the device used;
−The objective of prospecting work and in
particular the scale at which it is undertaken,
which determines the framework for imple-
menting field measurements.
In the context of groundwater research, the
parameters sought concern the reservoir: its
position, its geometry and the quality of the
water it contains [20].
For the present work, since it is a question
of the survey for groundwater, our choice takes
into account not only the capacity of a method
to locate the zones of fractures or crushing con-
sidered as zones of accumulation of groundwa-
ter, but also the cost, the implementation time
and the ease of use in the field. This justifies the
Figure 4: Geological map of urban municipality of Boké (Boké centre).
Identication of favourable geological formations for the determination of groundwater
7
choice of the geo-electrical method (electrical
sounding) of the Schlumberger type.
•Work device: Several devices are envisaged
to determine the distribution of resistivities
in the subsoil. The choice of device depends
on the depth of investigation. Any measur-
ing device has in fact four electrodes, two
electrodes A and B, for sending currents
(transmission circuit) and two others M and
N, for measuring the potential ∆V (measur-
ing or receiving circuit). The Schlumberger
configuration is shown in Figure 6.
•Measurement technique: The measurement
technique consists of separating the injec-
tion circuit from the measurement circuit.
Four electrodes are used for this in practice,
AMNB (the measuring quadrupole). From
Figure 5: Location map of study sites.
Figure 6: Schlumberger device.
Diallo et al.
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RMZ – M&G | 2022 | Vol. 69[2] | pp. 1–17
two electrodes, called injection electrodes
A and B, an electric current of intensity I is
sent into the ground and the potential differ-
ence (∆V) is measured between two other
electrodes, called measurement electrodes
MN [21].
•Processing: The results of the resistivity
measurements are entered into the software,
and after processing, the apparent resistivity
values are obtained on a bi-logarithmic scale
whose distances AB/2 are reported on the
abscissa and the resistivities are on the ordi-
nate. The petro-geophysical model defining
the number of terrains and their character-
istics (resistivity and thickness) in the area
and the physical-geological model which
highlights the behavior of the current in the
ground through a curve are finally obtained.
Knowing the geology of the area, the nature
of the terrain is defined by analogy with the
resistivity values of the rocks in the region.
The results and their interpretation, the
coordinates of the points and the parameters
of the measuring device on the sites are as
follows:
A- Kissassi site
1) Curve of electrical positioning sounding
1 (SEP1): the geometric characteristics of
the device at this point are: AB/2 = 40 m;
MN/2 =10 m; k = 275. The geographic coor-
dinates are:
X = 57,448; Y = 1,208,604; and Z = 36 m.
At this point, the petro-physical model
reveals an area of three layers. Taking into
account the geology and the physical prop-
erties of the rocks of the area, the lithology
is presented from top to bottom as follows
(Figure 7):
−A layer of cuirass having a resistivity of
5,851 Ωm and a thickness of 1.6 m;
−An alteration crust with a resistivity of
2,517 Ωm and a thickness of 2 m, and;
−A formation of low resistivity (820 Ωm)
compared to the first and second which
is fractured clays. It is beyond 3.6m deep
and this layer constitutes the superficial
aquifer.
Figure 7: Lithological section of SEP1. Ep = Thickness.
Identication of favourable geological formations for the determination of groundwater
9
2) Electrical Test Sounding 1 (SET1): the geo-
metric characteristics of the device at this
level are: AB/2 = 30 m; MN/2 = no mea-
surement = 10 m; and k = 275.
Compared to the first survey, the electrical
test survey specifically intersected four lay-
ers including (Figure 8):
−A layer of cuirass having a resistivity of
4,623 Ωm and a thickness of 1.1m;
−A layer of crust altered having a resistiv-
ity of 3,349 Ωm;
−A thick layer of fractured argillites with
an average resistivity of 836 Ωm and a
thickness of 45 m;
−A last layer having a high electrical
resistivity (9,195 Ωm); it is the bedrock
(healthy argillites).
B- Abattoire Palmeraie site
The geometric characteristics of the device on
this site are: AB/2 = 40 m; MN/2 = 10 m. The
geographic coordinates are: X = 576,652; Y =
1,207,919; Z = 7 m.
1) Curve of electrical positioning sounding 2
(SEP2).
The petro-physical model of the survey
(SEP2) presented the lithology from top to
bottom as follows (Figure 9):
−A thin surface layer having a thickness
of 0.64 m and a resistivity of 543 Ωm
(sandy clays soil);
−A layer of altered crust with a thickness
of 1.3 m and a resistivity of 1602 Ωm;
−Thin layer of clay with a resistivity of
758 Ωm and a thickness of 1 m;
−A layer of fractured shale 45m thick and
a resistivity of 378 Ωm; The water table
is at this level;
−A healthy layer of shales.
The bedrock roof was cut to a depth of
35 m.
2) Test electrical sounding 2 (SET2):
The lithological section of this survey is as
follows (Figure 10):
−A layer of cuirass which has a thickness
of 1.7 m and a resistivity of 4,410 Ωm;
−A weakly altered layer (altered crust);
−A layer of weakly fractured dolerites
is located beyond 5.7 m depth. This
zone admits an electrical resistivity of
453 Ωm.
The top of the bedrock (fractured doler-
ites) of this hole was intersected at a depth
of 35 m.
C- Tamakènè site
The characteristic parameters of the device
are: AB/2 = 40 m; MN/2 = 10 m; k = 275. The
geographic coordinates are as follows: X =
580,265; Y = 1,203,704; Z = 57 m.
1) Electrical positioning sounding curve
(SEP3):
Figure 8: Lithological section of SET1. Ep = Thickness.
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Figure 9: Lithological section of SEP2. Ep = Thickness.
Figure 10: Lithological section of SET2. Ep = Thickness.
Identication of favourable geological formations for the determination of groundwater
11
The lithological section revealed by the lat-
ter is as follows:
From top to bottom (Figure 11):
−A superficial formation having a
thickness of 1.4m and a resistivity of
1,741 Ωm;
−A layer of slightly altered crust
with a resistivity of 2,379 Ωm and
3.65 m thick;
−A thin layer of clay with a thickness of
1.5 m and a resistivity of 1,008 Ωm;
−A thick layer (199 m) of highly frac-
tured shale characterized by an electri-
cal resistivity of 261 Ωm. The aquifer is
located at this level. Below this layer is
bedrock (healthy shale).
2) Electrical Test Sounding 3 (SET3).
The geographical coordinates of this site
are mentioned in Figure 12.
At this level (SET3), the lithology is pre-
sented from top to bottom as follows
(Figure 12):
−A layer of cuirass which extends over a
thickness of about 2.12 m and an aver-
age resistivity of 5,000 Ωm;
−A layer of altered crust with an aver-
age resistivity of about 1,300 Ωm and a
thickness of about 6 m;
−A thick layer of sandstone beyond 21 m
characterized by an electrical resistivity
of 41,201 Ωm.
D- Nema school complex site
The geometric characteristics of the device on
this site are: AB/2 = 40 m; MN/2 = 10 m; and
K = 275.
1) Curve of electrical positioning sounding 4
(SEP4):
The lithology at this point is, from top to
bottom, as follows: (Figure 13):
−A layer of cuirass which has a resis-
tivity of 5,345 Ωm and a thickness
of 1.5 m;
−A layer of altered crust with a resistivity
of 1,115 Ωm is beyond 1.5 m.
2) Electrical sounding test 4 (SET4):
The electrical test sounding performed
shows the following lithology (Figure 14):
−A layer of altered crust with a thickness
of 5.8 m and a resistivity of 1,278 Ωm;
−A layer of wet clay located about 13 m
deep with a resistivity of 829 Ωm;
−Beyond 10 m depth, there is a layer of
fractured and wet clay. It has a resistiv-
ity of 121 Ωm.
E- Kadiguira site
The geometric characteristics of the device are
like the previous sites (Nema school complex,
Tamakènè).
1) Curve of the electrical positioning sound-
ing (SEP5).
The lithological section of SEP5 gave us the
following, from top to bottom:
−A layer of altered crust which extends
over a thickness of 7.5 m and a resistiv-
ity of 908 Ωm;
−A thick layer of wet clay constituting the
aquifer with a thickness of 52 m and a
resistivity of 290 Ωm;
−A last layer which constitutes the bed-
rock (healthy clay). It is located beyond
60 m deep and has a resistivity of
3397 Ωm
2) Electrical sounding test 5 (SET5).
The lithologic section of SET5 is pre-
sented from top to bottom as follows
(Figure 15):
−Altered crust with a thickness of 6.05 m
and a resistivity of 814 Ωm;
−A layer of fractured clay located at a
depth of 6.05m, characterized by a
resistivity of 367 Ωm and a thickness of
18 m (this is the aquifer);
−Beyond 24 m, we have the upper part of
the bedrock (healthy clay).
F- Ballaya site
1) Curve of electrical positioning sounding 6
(SEP6).
The lithological section of SEP6 is presented
from top to bottom as follows (Figure 16):
−An altered and wet (altered crust) layer
2.3 m thick with a resistivity of 262 Ωm;
−A layer of fractured argillites, character-
ized by levels, with a thickness of 29.1
m and an average resistivity of 167 Ωm;
−A layer of healthy argillites located
more than 31 m deep with a resistivity
of 2,418 Ωm.
Diallo et al.
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Figure 11: Lithological section of SEP3. Ep = Thickness.
Figure 12: Lithological section of SET3. Ep = Thickness.
Identication of favourable geological formations for the determination of groundwater
13
Figure 13: Lithological section of SEP4. Ep = Thickness.
Figure 14: Lithological section of SET4. Ep = Thickness.
Diallo et al.
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RMZ – M&G | 2022 | Vol. 69[2] | pp. 1–17
Figure 15: Lithological section of SET5. Ep = Thickness.
Figure 16: Lithological section of SEP6. Ep = Thickness.
Identication of favourable geological formations for the determination of groundwater
15
2) Electrical sounding test (SET6):
The lithologic section of SET6 is presented
from top to bottom as follows (Figure 17):
−A layer of altered crust with two levels,
the upper part resistant and the lower
part less resistant; it has an average
resistivity of 1,508 Ωm and a thickness
of about 6 m;
− A thick layer of fractured argillites with
a resistivity of 288 Ωm and a thickness
of 25 m;
−Beyond 31 m, we have healthy substra-
tum (argillites). It has a resistivity of
4,226 Ωm.
The analysis and interpretation of the results
of the electrical soundings carried out at
the six sites studied in the area enabled us
to highlight three superimposed zones or
layers in such a way that the comparison
of the resistivities is presented as follows:
ƍ1 > ƍ2 < ƍ3.
The first layer of the study area extending
over approximately 40 m corresponds to the
covering of the sedimentary cover; the second
constitutes an arena of low resistivity and be-
ing on a depth of surroundings 5 m; the third
layer is the very resistant and fissured in plac-
es bedrock. Several authors, in the context of
hydrogeological studies with different objec-
tives, have determined the lithology of the sites
using electrical soundings. This is the case of
[22], [9–10] who, in their studies, succeed-
ed in highlighting the geological structures,
increasing the production of the drillings and
decreasing the negative drilling rate. This
supported our choice of the method and the
results obtained.
At the end of this study, we find that our area
has a lithology of several terrains arranged
from top to bottom:
−A layer of weathering crust covered in places
by a thin layer of the cuirass or topsoil. The
average thickness of this layer is 40 m;
−A thin layer of wet clay with an average thick-
ness of 4.5 m which is intercalated between
Figure 17: Lithological section of SET6. Ep = Thickness.
Diallo et al.
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RMZ – M&G | 2022 | Vol. 69[2] | pp. 1–17
the weathered crust and the top of the fis-
sured bedrock;
−A layer of cracked shales, dolerites or sand-
stones (roof of the substratum) follows the
layer of clays. It is at this level that the most
important fractures for the accumulation
of groundwater are located. This zone is
located at more than 40 m depending on the
location;
−A healthy formation which constitutes the
substratum. It consists of healthy shales, dol-
eritic intrusions and sandstones.
Structures favourable to the accumulation of
groundwater are fractured shales, fissured dol-
erites and fissured or crushed sandstones. The
latter (sandstone) has a significant thickness
and is generally located at a great depth (100
to 150 m).
Despite the efforts, it must be recognized
that like any other study, this one has limita-
tions. They are: ignorance of the direction of
groundwater flow and lack of knowledge of the
physicochemical properties of the waters in the
area. These shortcomings are justified by the
lack of material and financial resources neces-
sary during the works.
[1] INS Guinée (2018): Rapport annuel. Conakry.
Institut National de la Statistique de Guinée, 28 p.
[2] Kourouma, M. (2016): Choix d’un complexe rationnel
de méthodes géophysiques pour la recherche des
eaux souterraines au Nord-Ouest de la Guinée. Thèse.
CERESCOR, Centre de Recherche Scientifique de
Guinée: Guinée, 176 p.
[3] Diallo, I. (1979): Projet de recherche des eaux
souterraine sur la Boffa en vue de l’adduction de la
population en eau potable. Mémoire de fin d’étude
supérieure. Boké, Institut Supérieur des Mines et
Géologie de Boké (ISMGB), Guinée, 102 p.
[4] SNAPE (2018): Rapport annuel. Conakry, 18 p.
[5] Kim, M.K.J.K.N., Jeong, G. (2011): Surface geo-
physical investigations of landslide at the Wiri
area in southeastern Korea. Environmental Earth
Sciences, 63(5), pp. 999–1009, DOI: 10.1007/
s12665-010-0776-z.
[6] Kadri, M., Nawawi, M.N.M. (2010): Groundwater
exploration using 2D Resistivity Imaging in Pagoh,
Johor, Malaysia. In: AIP Conference Proceedings,
pp. 151–155.
[7] Morad, M.D. (2012): Utilisation des dispositifs de
géophysique électrique non classiques pour l’étude
des couches géologiques profondes: cas des chotts
el Gharbi et chergui (Algérie). Thesis. Université
d’Oran: Algérie, 198 p.
[8] Michel, K.A., Coulibaly, D., Koffi, Y.B., Biemi, J.
(2013): Application de méthodes géophysiques
à l’étude de la productivité des forages d’eau en
milieu cristallin: cas de la région de Toumodi
(Centre de la Côte d’Ivoire). International
Journal of Innovation and Applied Studies, 2(3),
pp. 324–334.
[9] Dieng, B., De Heusch, K.A., Bakyono, B. A. (2004):
Optimisation de l’implantation géophysique des
forages en zone de socle au Nord du Burkina Faso.
Groupe des Ecoles EIER-ETSHER, Ouagadougou 03,
Burkina Faso.
[10] Kouakou, E.G.K. (2012): Utilisation de la prospec-
tion géophysique par résistivité électrique pour la
recherche d’eau souterraine dans le département de
Tanda (Est de la Côte d’Ivoire). European Journal of
Scientific Research, 83(2).
[11] Falco, P. (2013): Sondages géoélectriques ‘’Null-
Arrays’’ pour la caractérisation des structures de
subsurface. Thesis. Université Neuchatel.
[12] Njueya A.K., Kengni, L., Fonteh, M.F., Dongmo, A.K.,
Ntankouo., R.N., Nkouathio, D.G., Tazo, C. (2016):
Apport des Sondages Électriques Verticaux à la
Localisation et la Caractérisation des Aquifères en
zone Volcanique au Cameroun: Cas d’Ebone et ses
Environs. European Journal of Scientific Research,
pp. 54–65.
[13] Kouakou, E.G.K., Dosso, L., Kouame, L.N., Sombo,
A.P., Sombo, B.C. (2015): Contribution des méth-
odes de résistivité électrique a la recherche d’eau
en milieu cristallin: cas de Yakassé-Attobrou
et d’Abié, région de la Mé, Côte d’Ivoire. La
Revue Ivoirienne des Sciences et Technologie, 26,
pp. 194–211.
[14] Koussoubé, Y., Nakolendoussé, S., Bazié, P.,
Sawadogo, A.N. (2003): Typologie des courbes de
sondages électriques verticaux pour la reconnais-
sance des formations superficielles et leur incidence
en hydrogéologie de socle cristallin du Burkina
Fasso. Pangea infos, Société Géologique de France,
1999, 31/32, pp. 33–36.
[15] Bernardi, A., Detay, M., De Gramont, H.M.
(1988): Recherche d’eau dans le socle africain.
Corrélation entre les paramètres géoélectriques
Identication of favourable geological formations for the determination of groundwater
17
et les caractéristiques hydrodynamiques des
forages en zone de socle. Hydrogeology Journal, 4,
pp. 245–253.
[16] INS Guinée (2020): Annuaire des statistiques de
l’environnement, 256 p.
[17] Dansoko, K. (2019): La mise en œuvre d’un proto-
cole suivi-évaluation environnementale et sociale du
permis Alliance Minière Responsable (AMR). Rapport
de fin d’études supérieures, Institut Supérieur des
Mines et Géologie de Boké (ISMGB), Guinée, 68 p.
[18] Mamedov, V.I., Bouféév, Y.V., Nikitine, Y.A. (2010):
Géologie de la République de Guinée. Geoprospects
Ltd: Université d’état de Moscou, 166 p.
[19] Nabé, L. (2017): Géologie et étude des faciès baux-
ite de la feuille Boffa. Rapport de fin de d’étude
supérieur, Institut Supérieur des Mines et Géologie
de Boké (ISMGB), Guinée, 97 p.
[20] Soro, D.D. (2017): Caractérisation et modélisation
hydrogéologique d’un aquifère en milieu de socle
fracturé: cas du site expérimental de Sanon (région
du plateau central au Burkina Faso). PhD Thesis.
Université Pierre et Marie Curie-Paris VI, Institut
international, 303 p.
[21] Cissé, O., Kourouma, A. (2006): Utilisation des méth-
odes géophysiques pour la recherche des eaux sou-
terraines à Lambanyi dans la commune de Ratoma.
Rapport de fin d’études supérieures. Institut
Supérieur des Mines et Géologie de Boké (ISMGB),
Guinée, 51 p.
[22] Lavoie, A.C. (1998): Application de la méthode
des sondages électriques à la caractérisation des
aquifères et des dépôts meubles, Basses-Terres du
St-Laurent, région Nord de Montréal. Mémoire de
maitrise, 210 p.
