# Groundwater Potential Assessment Using Vertical Electrical Sounding and Magnetic Methods: A Case of Adilo Catchment, South Nations, Nationalities and Peoples Regional Government, Ethiopia

Authors: Mulugeta Markos; Abel Saka; Leta Tesfaye Jule; N. Nagaprasad; Krishnaraj Ramaswamy
Journal: Concepts in Magnetic Resonance Part A, Bridging Education and Research
 (2021)

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## Abstract

Vertical electrical sounding and magnetic methods were carried out to assess groundwater potential in Adilo catchment, Kembata Tembaro Zone, South Nations, Nationalities and Peoples Regional Government, Main Ethiopian Rift. The data were acquired from eight VES points using Schlumberger electrode arrays with maximum half current electrode spacing (AB/2=500) and 253 magnetic data points were analyzed. The qualitative analysis of VES data was accomplished by using curves, apparent resistivity, and pseudodepths, and the quantitative interpretations of the VES data were constructed by the VES data using IPI-Res3, IPI2Win, and surfer software and constructing geoelectric section along with profiles and lithological information from the borehole and Geosoft interpretation was used for magnetic data. The VES results of the data revealed five geoelectric layers which differ in degree of fracturing, weathering, and formation. The upward continued magnetic field map anomaly to 560 m illustrated northwestern to the southwest; areas have a low magnetic anomaly. Examining the potential aquifer of profile one’s geoelectric section, the horizons of layer four were better potential aquifers as the highly fractured and weathered ignimbrite zone of layer five of VES13 was 219 m deeper than the depths of the other VES points, and along with profile two geoelectric sections, the horizon of layer four VES23 layer five has the lowest resistivity with large thickness at a depth of 253 m. Thus, the low resistivity and the large thickness of these formations are an indication of the high yield of groundwater potential in the study area.


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## Body

## 1. Introduction

In most cases, drinking water comes from two sources: surface water and groundwater. Surface water sources are bodies of water on the earth’s surface, such as rivers, lakes, and reservoirs. Groundwater sources are underground aquifers which are geologic formations containing water underground. Groundwater is accessed by drilling a well into the underground water source and then pumping the well water up to the surface [1–5]. The value of an aquifer as a source of groundwater is a function of the porosity of the geologic stratum or layer, of which it is formed [2, 6–9]. Most of the area is known for the high scarcity of surface water, and due to recurrent drought, a substantial part of the area's water supply coming from groundwater has taken great attention. Although water requirement is increasing very rapidly with the growth of human and animal population in the area, analysis of water resources has been fragmentary. Thus, as a part of filling the gap, in the present study, vertical electrical sounding and magnetic methods were used to systematically assess the importance of each input parameter in the assessment of groundwater potential in the study catchment. Due to the above reasons, the search for groundwater is vital as an immediate and sustainable solution to alleviate the scarcity of water for drinking and other domestic uses in the Adilo catchment. Population growth and economic progress required greater volumes of freshwater [10]. Therefore, the detailed geophysical study for the assessment of groundwater potential is important.


### 1.1. Local Geology of the Study Area

The study area is covered by thick soils, except river cut and road section. The local geologic setup of the study area was described based on the observations of the river cut, boreholes, and drainage network patterns and illustrated in Figure1. Stratigraphy of the study sites is clay, volcanic ash, gravel, and ignimbrite. The ignimbrite found in the southern portion of the study area is highly fractured and weathered.Figure 1
Geological map of the Adilo catchment and its surrounding outcrop from Hosiena geological map (1 : 2,000,000).


## 1.1. Local Geology of the Study Area

The study area is covered by thick soils, except river cut and road section. The local geologic setup of the study area was described based on the observations of the river cut, boreholes, and drainage network patterns and illustrated in Figure1. Stratigraphy of the study sites is clay, volcanic ash, gravel, and ignimbrite. The ignimbrite found in the southern portion of the study area is highly fractured and weathered.Figure 1
Geological map of the Adilo catchment and its surrounding outcrop from Hosiena geological map (1 : 2,000,000).


## 2. Materials and Method

### 2.1. Location and Accessibility

The Adilo catchment, the study area, is situated in the Main Ethiopian Rift. It is located about 130 km north-west of the regional capital city, Hawassa, and 342 km away from Addis Ababa through the asphalt road from Addis Ababa to the Arba Minch town that passes via towns of Shashemane and is depicted in Figure2 Adilo catchment is bounded between UTM coordinates 356496 m–428654 m easting and 799875 m–820483 m northing and about 1938 m above sea level. Locally, the study area is located east-north of Durame town of Kembata Tembaro Zone in Southern Regional State along the Main Asphalt Road, Addis Ababa, to Alaba Kulito-Wolaita Sodo of SNNPR and is situated 13 km from Durame town [11–14].Figure 2
Location map and study area.


### 2.2. Electrical Resistivity Data Acquisition

The Schlumberger array is mostly used in vertical electrical sounding for its better depth penetration, and it is less sensitive for lateral inhomogeneities. The potential electrodes remain fixed during a number of successive measurements with expanding current electrodes. For this study, the symmetrical Schlumberger array, which is the vertical electrical sounding (VES), was conducted along four lines which are about 200 m apart. The VES were carried out with maximum current electrode spacing (AB/2) of 500 m by injecting electrical current into the ground by means of two outer electrodes, and the resulting potential difference was measured by the second pair of potential electrodes situated in the center of the potential electrodes. The current electrode spacing selected for these surveys was AB/2 (in meter): 1.5 m, 2.1 m, 3 m, 4.2 m, 6 m, 9 m, 13.5 m, 20 m, 30 m, 45 m, 66 m, 100 m, 150 m, 220 m, 330 m, and 500 m, and the spacing of the potential electrodes was MN/2 (in meter): 0.5 m, 6 m, and 45 m. The repeated calibrations are taken at 20 m, 30 m, 150 m, and 220 m in order to remove the ambiguity of inhomogeneity. The material used at field survey for data collection of magnetic field and resistivity is described as the following.


### 2.3. Magnetic Field Procedures and Data Acquisition

Before establishing a base station around each profile, the first thing that the researcher does is to look for an appropriate location with less magnetic noise, such as cars and houses with iron roofs. As the survey progresses, the base station must be reoccupied every half of an hour in order to compile a diurnal variation curve for later correction [15]. The magnetic survey was carried out on four parallel profiles, which were nearly 200 m apart, and field magnetic and VES point locations are shown in Figure 3. These parallels were taken on the same profile from which the VES points were taken within the study area, and magnetic data were collected at every 20 m interval of the survey points. The positions of the survey stations and station elevations were determined using the Garmin GPS 72H receiver. Magnetic data collection was started and ended by taking base station readings situated around each profile. Hence, there were four base stations, for the first profile BS1 located at a UTM coordinate 388368 easting and 797906 northing, the second profile BS2 at 387482 easting and 798084 northing, the third profile at 387892 easting and 797686 northing, and the fourth profile at 387542 easting and 798318 northing. At each station, the magnetometer reading, recording time, and its location in the UTM coordinate were recorded.Figure 3
Field magnetic and VES points.The base station reading for all profiles in time of 1 : 00–1:30 hour was done. The magnetic data acquisitions were employed from north to south along with four profiles. From the site survey total of 253, magnetic data readings were taken manually. The photographic view of vertical electrical sounding is illustrated in Figure4. Finally, the collected data were imported into computer Excel software for diurnal correction. The profile line and data point of both vertical electrical sounding and magnetic sounding were mapped by ArcGIS 10.3 software together as the following [16–21].Figure 4
Photographic view of the vertical electrical (a) sounding and magnetic (b) field operation.
(a)(b)


## 2.1. Location and Accessibility

The Adilo catchment, the study area, is situated in the Main Ethiopian Rift. It is located about 130 km north-west of the regional capital city, Hawassa, and 342 km away from Addis Ababa through the asphalt road from Addis Ababa to the Arba Minch town that passes via towns of Shashemane and is depicted in Figure2 Adilo catchment is bounded between UTM coordinates 356496 m–428654 m easting and 799875 m–820483 m northing and about 1938 m above sea level. Locally, the study area is located east-north of Durame town of Kembata Tembaro Zone in Southern Regional State along the Main Asphalt Road, Addis Ababa, to Alaba Kulito-Wolaita Sodo of SNNPR and is situated 13 km from Durame town [11–14].Figure 2
Location map and study area.


## 2.2. Electrical Resistivity Data Acquisition

The Schlumberger array is mostly used in vertical electrical sounding for its better depth penetration, and it is less sensitive for lateral inhomogeneities. The potential electrodes remain fixed during a number of successive measurements with expanding current electrodes. For this study, the symmetrical Schlumberger array, which is the vertical electrical sounding (VES), was conducted along four lines which are about 200 m apart. The VES were carried out with maximum current electrode spacing (AB/2) of 500 m by injecting electrical current into the ground by means of two outer electrodes, and the resulting potential difference was measured by the second pair of potential electrodes situated in the center of the potential electrodes. The current electrode spacing selected for these surveys was AB/2 (in meter): 1.5 m, 2.1 m, 3 m, 4.2 m, 6 m, 9 m, 13.5 m, 20 m, 30 m, 45 m, 66 m, 100 m, 150 m, 220 m, 330 m, and 500 m, and the spacing of the potential electrodes was MN/2 (in meter): 0.5 m, 6 m, and 45 m. The repeated calibrations are taken at 20 m, 30 m, 150 m, and 220 m in order to remove the ambiguity of inhomogeneity. The material used at field survey for data collection of magnetic field and resistivity is described as the following.


## 2.3. Magnetic Field Procedures and Data Acquisition

Before establishing a base station around each profile, the first thing that the researcher does is to look for an appropriate location with less magnetic noise, such as cars and houses with iron roofs. As the survey progresses, the base station must be reoccupied every half of an hour in order to compile a diurnal variation curve for later correction [15]. The magnetic survey was carried out on four parallel profiles, which were nearly 200 m apart, and field magnetic and VES point locations are shown in Figure 3. These parallels were taken on the same profile from which the VES points were taken within the study area, and magnetic data were collected at every 20 m interval of the survey points. The positions of the survey stations and station elevations were determined using the Garmin GPS 72H receiver. Magnetic data collection was started and ended by taking base station readings situated around each profile. Hence, there were four base stations, for the first profile BS1 located at a UTM coordinate 388368 easting and 797906 northing, the second profile BS2 at 387482 easting and 798084 northing, the third profile at 387892 easting and 797686 northing, and the fourth profile at 387542 easting and 798318 northing. At each station, the magnetometer reading, recording time, and its location in the UTM coordinate were recorded.Figure 3
Field magnetic and VES points.The base station reading for all profiles in time of 1 : 00–1:30 hour was done. The magnetic data acquisitions were employed from north to south along with four profiles. From the site survey total of 253, magnetic data readings were taken manually. The photographic view of vertical electrical sounding is illustrated in Figure4. Finally, the collected data were imported into computer Excel software for diurnal correction. The profile line and data point of both vertical electrical sounding and magnetic sounding were mapped by ArcGIS 10.3 software together as the following [16–21].Figure 4
Photographic view of the vertical electrical (a) sounding and magnetic (b) field operation.
(a)(b)


## 3. Results and Discussion

As observed in profile one as follows, this survey consists of four vertical electrical soundings, namely, VES11, VES12, VES13, and VES14. Each VES contains five layers and has different types of curves. It is seen from the interpreted field curves that a very valid correspondence between the field data and the interpreted curves is acquired for all the VES points. The curves of profile one RMS error ranging 0.4–1.56 were obtained from the sounding curves.Figure5 shows the electrical resistivity curve of VES11, VES12, VES13, and VES14: (a) interpretation of VES11 curve. This is a curve type and has the lowest resistivity with a large thickness along with layer four which may be interpreted as an aquifer zone. (b) Interpretation of VES12 curve (c) Interpretation of curve of VES13. This curve has the lowest resistivity layer along with layer five and has high thickness. This may indicate high groundwater potential in the study area. (d) Interpretation of the curve of VES14.Figure 5
(a) Electrical resistivity curve of VES11. (b) Electrical resistivity curve of VES12. (c) Electrical resistivity curve of VES13. (d) Electrical resistivity curve of VES14.


### 3.1. The Pseudosection along with Profile One

The pseudodepth constructed from all VES that lies on profile one is given in Figure5. Low resistivity responses were found at the bottom depth of VES13 with large thickness. This is interpreted as weak zones within the ignimbrite unit that resulted in low resistivity response due to high weathering and fracturing activities. These are essential results for storing and conducting groundwater potential in the study area.


### 3.2. Geoelectric Section along with Profile One

The geoelectric section of profile one was constructed, as shown in Figure6; this profile contains four VES points oriented nearly in the N–S direction. The fourth layer of VES11, VES12, and VES14 and the fifth layer of VES13 profile possess resistivity values ranging from 26–96 Ωm and thicknesses of 60–134 m. These layers may be highly fractured and weathered ignimbrite with scoria (from borehole data, this is the major aquifer zone). This horizon has a lower resistivity part with a large thickness. Thus, structures having low resistivity and large thickness could be considered as good groundwater potential zones. This layer is probably the major aquifer zone [22–27].Figure 6
Pseudosection along profile one.


### 3.3. Curve Interpretation for a Long Profile 2

As observed from Figure7, profile two consists of four vertical electrical soundings, namely, VES21, VES22, VES23, and VES24. Each VES contains five layers and has different types of curves. After iteration correction and the inversion had been done, the VES22 curve model was produced for the resistivity data as follows. This is an HKH curve type, and its RMS error is about 0.766 [28–31].Figure 7
Geoelectric sections along with profile one.


### 3.4. The Pseudosection along with Profile Two

The pseudodepth constructed using VES21 to VES24 that lies on the survey of profile two was described, as shown in Figure8 Very low resistivity zone was observed at the shallow to a middle depth of VES23, and the area is expected as groundwater saturated zone; it is clearly shown in Figure 9.Figure 8
(a) Electrical resistivity curve of VES21. (b) Electrical resistivity curve of VES22. (c) Electrical resistivity curve of VES23. (d) Electrical resistivity curve of VES24.Figure 9
Pseudosections along with profile two.


### 3.5. Geoelectric Section along with Profile Two

The geoelectric section of profile two was constructed from the interpreted layer parameters of VES21–VES24 and is shown in Figure10. The fourth layer of VES21, VES22, and VES23 and the fifth layer of VES23 profile survey possess resistivity values varying from 23–32 Ωm and thickness of 54–151 m. These were layers interpreted as highly fractured and weathered ignimbrite with scoria. This is a low resistivity horizon with a large thickness which is the result of groundwater saturation in the study area [31].Figure 10
Geoelectric section along with profile two.


### 3.6. Total Magnetic Intensity Field Anomaly

The total magnetic field anomaly map was created after diurnal corrections and removal of the IGRF value from the field data. This map shows that a relatively low magnetic response was observed north-northeast towards the northwestern part of the study area, whereas the high magnetic response is observed at the northeastern, east central, and northeast margin of the map. From Figure11, the map observed that the anomaly of total magnetic field intensity variation started from 21229 nT–35491 nT.Figure 11
Total magnetic field intensity anomaly map of the study area.


### 3.7. Analytical Signal Map Anomaly

Analytical signal of the total magnetic field reduces the magnetic data to anomalies whose maximum marks the edges of the magnetized bodies if the sources are resolved. The analytical signal map is very useful for delineating magnetic source location at shallow subsurface levels. The analytical signal is formed through a combination of horizontal and vertical gradients of a magnetic anomaly and has a form over causative bodies that depend on the locations of the bodies but not their directions of magnetization [29]. It can be used to find horizontal locations and depths of magnetic contacts.The analytical signal map of the study area was produced from the total magnetic field anomaly map. From Figure12, the observed analytical signal map low amplitudes were located southwest to vertically going upward north-west and east margin of the map.Figure 12
Analytical signal magnetic field anomaly maps.


### 3.8. Upward Continued Magnetic Field Anomalous Maps

(1)
All the magnetic maps were made when the magnetic fields were corrected.(2)
Upward continuation filters observed that as continuity increases, the shallow features smoothened and enhanced the detection of deep features. The magnetic field data were gridded and filtered at 0 m 140 m, 280 m, 420 m, and 560 m of upward continuation in the stacked figure (because the depth of borehole was 280 meters, upward continuation detected twice of the depth of borehole).From the map, it is observed that the field in upward continuation anomaly map values varies from 20000 to 36000 nT, which is a large variation in the magnetic field, indicating in either lithology or degree of alteration that the study area is located in the main Ethiopia Rift. This, in turn, makes the magnetic field very large (not an abnormal range). This 20000 to 36000 nT is an inclusive number that consists of all gridded and filtered upward continuation.The upward continued map is an enhancement technique that transforms the observed magnetic field data on a surface to a higher level. Near the surface (high frequency), features are attenuated as the magnetic data are virtually upward [2]. The principle of continuation is the mathematical projection of potential field data (magnetic or gravity) from one datum vertically upwards or downwards to another datum. Effectively, the continuation process simulates the anomaly at levels below or above sea level as if the data had been obtained at those levels.The continued upward maps of the study area were produced from the total magnetic field map. From Figure12, upward continuation filters observed that as continuity increases, the shallow features smoothened and enhanced deep features detection. The magnetic field data were gridded and filtered at 0 m, 140 m, 280 m, 420 m, and 560 m of upward continuation in the next stacked Figure 13.Figure 13
Stacked map of upward continuation of magnetic anomaly map.


#### 3.8.1. Zone A

This region can be classified as a high magnetic anomaly that could probably be the responses from rocks that have high magnetic susceptibility. This high magnetic anomaly is observed in the north-east, central-east, and south-eastern parts of the study area. The signature of this anomaly ranges from −1000 nT to 1000 nT.


#### 3.8.2. Zone B

This region is a comparatively low magnetic anomaly, and its magnetic field varies in the range of −1000–1000 nT. This may be caused by the rocks of low magnetic susceptibility that have resulted in fracturing and weathering of rocks. This low magnetic anomaly zone is trending in the southwest to diagonally going upward to the west-central part of the study area.


#### 3.8.3. Zone C

These low magnetic anomaly areas can be interpreted as rocks that have resulted from the oxidation of the magnetic material due to intense weathering of the rocks unit. This anomaly is observed in the northwestern portion of the study areas. These upward magnetic field anomaly values vary in the interval of −1000 to 1000 nT.


## 3.1. The Pseudosection along with Profile One

The pseudodepth constructed from all VES that lies on profile one is given in Figure5. Low resistivity responses were found at the bottom depth of VES13 with large thickness. This is interpreted as weak zones within the ignimbrite unit that resulted in low resistivity response due to high weathering and fracturing activities. These are essential results for storing and conducting groundwater potential in the study area.


## 3.2. Geoelectric Section along with Profile One

The geoelectric section of profile one was constructed, as shown in Figure6; this profile contains four VES points oriented nearly in the N–S direction. The fourth layer of VES11, VES12, and VES14 and the fifth layer of VES13 profile possess resistivity values ranging from 26–96 Ωm and thicknesses of 60–134 m. These layers may be highly fractured and weathered ignimbrite with scoria (from borehole data, this is the major aquifer zone). This horizon has a lower resistivity part with a large thickness. Thus, structures having low resistivity and large thickness could be considered as good groundwater potential zones. This layer is probably the major aquifer zone [22–27].Figure 6
Pseudosection along profile one.


## 3.3. Curve Interpretation for a Long Profile 2

As observed from Figure7, profile two consists of four vertical electrical soundings, namely, VES21, VES22, VES23, and VES24. Each VES contains five layers and has different types of curves. After iteration correction and the inversion had been done, the VES22 curve model was produced for the resistivity data as follows. This is an HKH curve type, and its RMS error is about 0.766 [28–31].Figure 7
Geoelectric sections along with profile one.


## 3.4. The Pseudosection along with Profile Two

The pseudodepth constructed using VES21 to VES24 that lies on the survey of profile two was described, as shown in Figure8 Very low resistivity zone was observed at the shallow to a middle depth of VES23, and the area is expected as groundwater saturated zone; it is clearly shown in Figure 9.Figure 8
(a) Electrical resistivity curve of VES21. (b) Electrical resistivity curve of VES22. (c) Electrical resistivity curve of VES23. (d) Electrical resistivity curve of VES24.Figure 9
Pseudosections along with profile two.


## 3.5. Geoelectric Section along with Profile Two

The geoelectric section of profile two was constructed from the interpreted layer parameters of VES21–VES24 and is shown in Figure10. The fourth layer of VES21, VES22, and VES23 and the fifth layer of VES23 profile survey possess resistivity values varying from 23–32 Ωm and thickness of 54–151 m. These were layers interpreted as highly fractured and weathered ignimbrite with scoria. This is a low resistivity horizon with a large thickness which is the result of groundwater saturation in the study area [31].Figure 10
Geoelectric section along with profile two.


## 3.6. Total Magnetic Intensity Field Anomaly

The total magnetic field anomaly map was created after diurnal corrections and removal of the IGRF value from the field data. This map shows that a relatively low magnetic response was observed north-northeast towards the northwestern part of the study area, whereas the high magnetic response is observed at the northeastern, east central, and northeast margin of the map. From Figure11, the map observed that the anomaly of total magnetic field intensity variation started from 21229 nT–35491 nT.Figure 11
Total magnetic field intensity anomaly map of the study area.


## 3.7. Analytical Signal Map Anomaly

Analytical signal of the total magnetic field reduces the magnetic data to anomalies whose maximum marks the edges of the magnetized bodies if the sources are resolved. The analytical signal map is very useful for delineating magnetic source location at shallow subsurface levels. The analytical signal is formed through a combination of horizontal and vertical gradients of a magnetic anomaly and has a form over causative bodies that depend on the locations of the bodies but not their directions of magnetization [29]. It can be used to find horizontal locations and depths of magnetic contacts.The analytical signal map of the study area was produced from the total magnetic field anomaly map. From Figure12, the observed analytical signal map low amplitudes were located southwest to vertically going upward north-west and east margin of the map.Figure 12
Analytical signal magnetic field anomaly maps.


## 3.8. Upward Continued Magnetic Field Anomalous Maps

(1)
All the magnetic maps were made when the magnetic fields were corrected.(2)
Upward continuation filters observed that as continuity increases, the shallow features smoothened and enhanced the detection of deep features. The magnetic field data were gridded and filtered at 0 m 140 m, 280 m, 420 m, and 560 m of upward continuation in the stacked figure (because the depth of borehole was 280 meters, upward continuation detected twice of the depth of borehole).From the map, it is observed that the field in upward continuation anomaly map values varies from 20000 to 36000 nT, which is a large variation in the magnetic field, indicating in either lithology or degree of alteration that the study area is located in the main Ethiopia Rift. This, in turn, makes the magnetic field very large (not an abnormal range). This 20000 to 36000 nT is an inclusive number that consists of all gridded and filtered upward continuation.The upward continued map is an enhancement technique that transforms the observed magnetic field data on a surface to a higher level. Near the surface (high frequency), features are attenuated as the magnetic data are virtually upward [2]. The principle of continuation is the mathematical projection of potential field data (magnetic or gravity) from one datum vertically upwards or downwards to another datum. Effectively, the continuation process simulates the anomaly at levels below or above sea level as if the data had been obtained at those levels.The continued upward maps of the study area were produced from the total magnetic field map. From Figure12, upward continuation filters observed that as continuity increases, the shallow features smoothened and enhanced deep features detection. The magnetic field data were gridded and filtered at 0 m, 140 m, 280 m, 420 m, and 560 m of upward continuation in the next stacked Figure 13.Figure 13
Stacked map of upward continuation of magnetic anomaly map.


### 3.8.1. Zone A

This region can be classified as a high magnetic anomaly that could probably be the responses from rocks that have high magnetic susceptibility. This high magnetic anomaly is observed in the north-east, central-east, and south-eastern parts of the study area. The signature of this anomaly ranges from −1000 nT to 1000 nT.


### 3.8.2. Zone B

This region is a comparatively low magnetic anomaly, and its magnetic field varies in the range of −1000–1000 nT. This may be caused by the rocks of low magnetic susceptibility that have resulted in fracturing and weathering of rocks. This low magnetic anomaly zone is trending in the southwest to diagonally going upward to the west-central part of the study area.


### 3.8.3. Zone C

These low magnetic anomaly areas can be interpreted as rocks that have resulted from the oxidation of the magnetic material due to intense weathering of the rocks unit. This anomaly is observed in the northwestern portion of the study areas. These upward magnetic field anomaly values vary in the interval of −1000 to 1000 nT.


## 3.8.1. Zone A

This region can be classified as a high magnetic anomaly that could probably be the responses from rocks that have high magnetic susceptibility. This high magnetic anomaly is observed in the north-east, central-east, and south-eastern parts of the study area. The signature of this anomaly ranges from −1000 nT to 1000 nT.


## 3.8.2. Zone B

This region is a comparatively low magnetic anomaly, and its magnetic field varies in the range of −1000–1000 nT. This may be caused by the rocks of low magnetic susceptibility that have resulted in fracturing and weathering of rocks. This low magnetic anomaly zone is trending in the southwest to diagonally going upward to the west-central part of the study area.


## 3.8.3. Zone C

These low magnetic anomaly areas can be interpreted as rocks that have resulted from the oxidation of the magnetic material due to intense weathering of the rocks unit. This anomaly is observed in the northwestern portion of the study areas. These upward magnetic field anomaly values vary in the interval of −1000 to 1000 nT.


## 4. Conclusion

Examining the potential aquifer of profile one’s geoelectric section, the horizons of layer four were better potential aquifers as the highly fractured and weathered ignimbrite zone of layer five of VES13 was 219 m deeper than the depths of the other VES points, and along with profile two geoelectric section, the horizon of layer four VES23 layer five has the lowest resistivity with large thickness at a depth of 252.8 m. Thus, the low resistivity and the large thickness of these formations are an indication of the high yield of groundwater potential in the study area. From total magnetic and upward continuation maps, low magnetic responses are found from southwest to northwestern areas of the study. From this, it may be concluded that the low magnetic anomaly response results from a weak zone and a high degree of weathering and fracturing of rocks formed in the study area. The upward continued magnetic field map anomaly to 560 illustrated that northwestern to the southwest areas have a low magnetic anomaly, which implies the presence of highly fractured and weathered ignimbrite in the depth of investigation.



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*Source: 5424865-2021-12-08.xml*