1. IntroductionThe magnetic method is one of the most commonly used geophysical tools. This stems from the fact that magnetic observations are obtained relatively easily and cheaply and few corrections must be applied to the observations. The aim of a magnetic survey is to investigate subsurface geology based on anomalies in the Earth’s magnetic field resulting from the magnetic properties of the underlying rocks. The magnetization of rocks and associated remanence is affected by deformation, tectonism, magmatism and metamorphism hence they reflet geological processes [1] . The purpose of the application of the aeromagnetic interpretation is to help in solving the problems of regional geological mapping and structure, delineation of buried contacts and basement depth. Different methods, based on the use of the magnetic field derivatives, have been developed to determine magnetic source parameters such as locations of boundaries and depths. Many researchers [2] [3] used source parameter imaging (SPI) to determine the depth to basement surface. The aeromagnetic method has been used in many geophysical studies in Cameroon [4] - [11] to map tectonic structures such as faults, lineaments, fractures and to highlight non-flush geological structures. Such structures may serve as potential hosts for a variety of minerals and may be used as guidance for exploration of the epigenetic, stress-related mineralization in the surrounding rocks [12] . The current study investigates the transition zone between the north margin of the Congo Craton (CC) and the North Equatorial Fold Belt (NEFB). Many authors [13] [14] invoke the thrusting of the NEFB over the CC. Besides, the study area has been affected by some shears that gave rise to many major faults including the Sanaga Fault (SF). This NE lineament is an active fault corresponding that may be to the north margin of the CC [15] [16] . The purpose of the present work is to produce a picture for the basement depth and contact locations, deduced from the available aeromagnetic data. In this paper, different techniques (TDR, HD_TDR, 3D-Euler deconvolution, AS and SPI) have been applied on the Minta area to locate the boundaries and the depths of the magnetic sources given the complexity of the geology of the study area in order to have better results. It is interested to correlate between these edge detection methods to measure the degree of similarity between their results. AS and SPI are used to calculate the depth to basement of the study area. Correlation between them also should be noticed.
2. Geological and Tectonic Setting of the Study AreaThe area that is the subject of our study is east of Yaoundé (Central Cameroon). It covers the portions of the departments of Haute Sanaga (capital city Nanga Eboko) in the central region, Nyong and Mfoumou (capital Akonolinga) in the Central region, and Upper Nyong (capital city Abong-Mbang) in the Eastern Region. The area under study has a relatively monotonous relief, with an altitude which is between 600 m and 700 m. Our survey area is crossed on the north by the Sanaga River flows in a sinisteral ductile fault oriented N70E and corresponds to a westward extension of the Bozoum fault-N’délé located in the Central African Republic [16] . The Mobile zone of Central Africa which limits the Congo Craton to the north and continues in northeastern Brazil by the Sergipano range [17] [18] (Figure 1(a)) is interpreted as a continent-to-continent collision chain involving the Congo craton and the northern Cratonic domain of Adamaoua-Yadé [19] or the active border of northern-central Cameroon [20] . In Cameroon, it is subdivided into supergroup of the north and supergroup of the south by the shear zone of the centre of Cameroon (CCSZ) [21] (Figure 1(b)):
1) The Northern Cameroon Supergroup (NCSG) consists of metase-dimentary rocks known as the Poli Group which is associated with subordinate 830 Ma-old volcanics of fault and alkaline affinities (Figure 1(b)). Widespread 630 - 660 Ma-old calc-alkaline granitoids from Adamawa and West Cameroon Groups were transformed to gneisses. The inherited zircons in the granitoids provide ages up to 2 Ga and may attest a Palaeoproterozoic crustal source in this region [19] .
2) The Southern Cameroon Supergroup (SCSG) is subdivided in two domains by the Sanaga Fault (Figure 1(b)). These large NE-striking transcurrent faults are regarded as possible prolongations of the major shear zones of NE Brazil in a pre-drift Gondwana recon-struction [22] [23] . The northern domain consists of high-grade gneisses, intruded by widespread Neoproterozoic syntectonic plutonic rocks of high-K calc-alkaline affinities [24] [25] [26] . The southern domain comprises Neoproterozoic lithostructural units of metasedimentary rocks, such as the Yaounde, Lom, Dja and Yokadouma Groups [27] . Protoliths of these units were deposited in a passive margin environment at the northern edge of the Congo craton. An alkaline magmatism [28] [29] was also recognized in association with these Neoproterozoic units. The rocks of this southern domain were transported top-to-the SSW onto the Archean Congo craton [29] [30] [31] . The thrust zone continues towards the east, forming the Oubanguides Complex in the Republic of Central Africa [32] [33] .
The study area situated at the east of Yaounde (Figure 1) belongs to the Southern Cameroon Supergroup (SCSG) and the Oubanguide Complex [33] [15] . It is at the limit of the granite formations that occupies the greater part of Adamaoua and the Yaounde group. The Yaoundé group is a huge allochtonous nappe thrusted southward onto the Congo craton. According to recent investigations, it underwent amphibolite- to granulite-facies medium- to high-P-T metamorphism with subsequent retrogression during the Pan-African (616 Ma) orogeny [28] [29] . A major part of the Yaounde Group is composed of metasedimentary rocks with predominant micaschists and paragneisses. The geological map of [34] (Figure 2) shows that the area is covered with granites and the ancient metamorphic series of Nanga-Eboko. The northern part of the newer, less metamorphosed series of Akonolinga is south of the study area. The granite
formations, ancient syntectonic granite, is represented in the north of the region, in Ngobadé. It is a heterogeneous granite, both in structure and texture, and in its mineralogical composition: the dominant type is a calc-alkaline granite. The granodiorite massifs in the south of Nkoambang and north-east of Ovong are well individualized in the middle of metamorphic rocks: the rock is granular and contains, among others, andesine, very ferriferous biotite and hornblende. The metamorphic series of Nanga-Eboko constitutes the substratum of the study area: the series is strongly folded and the dips are very variable, which does not allow to easily reconstruct the stratigraphy and the tectonics of these formations [35] . It is mainly composed of ectinites and migmatics. Among the ectinites, the two-micas gniess form a broad band, from Nkoambang to Angossa through Nguélémendouka: the most frequent facies is garnet and there are some quartzite zones in the gneisses. Biotite gneisses are not well represented: the north-east of Ngobade. The micaschists with two micas are noted in the west part of bibé; in the north-west, between N’Djombé and Nkondon. At the base of these mica-schists is a feldspar facies. Embrechite is the only migmatite represented in the study area. It is found in Minta to Bibé, in contact with the granites and in contact with two micas gneisses in Minta [4] . It also forms a broad band from Bana to Tombo. They are in contact with the northern part of the Akonolinga series and two massifs of granotoides. We distinguish facies with two micas (Tombo) or biotite alone or dominant. Quartzite facies is particularly visible in the Bibé sector. Amphibolites are present in the south of the region in biotite embrechites, but do not form large massifs. The northern part of the less metamorphosed series of the south of Akonolinga in the study area is mainly composed of chlorite-schist and quartzite.
The tectonic evolution of the area was affected by the Pan-African tectonothermal event which is characterized by a polyphase deformation with the stages D1 - D4 as reported by [26] [27] [29] [31] . D1 predated emplacement of calc-alkaline dioritic bodies and caused the formation of nappes that resulted in high-pressure granulite metamorphism of soft sediments. A strong overprinting of these nappes during D2 symmetric extension, probably associated with large-scale foliation socking and (or) gneissic doming and intense magmatic underplating, gave rise to regional flat-lying fabrics. The latter were further buckled by D3 and D4 folding phases defining a vertical constriction occurring with a major east-west to NW-SE shortening direction. The corresponding F3 and F4 folds trend north-south to NE-SW and east-west to NW-SE, respectively, and represent the main regional strain patterns. Based on the east-west to NW-SE maximum shortening orientation indicated by F3 folds, it is proposed that the nappe-stacking phase D1 occurred in the same direction.
3. Materials and Methods3.1. Aeromagnetic DataThe key component of this study involved image enhancement of existing aeromagnetic data sets acquired by the company SURVAIR (contractor) for the CIDA (client) in 1970. The survey was carried out in a nominal field clearance of 235 m which was monitored by a radar altimeter with an accuracy of ±20 m. The line spacing of the flight was 750 m but the real distance rarely went above 1 km and the flight direction was N-S. After correction of the measurements for the temporal variations of the magnetic field, the total magnetic intensity map of the study area is obtained with the inclination and declination angles of the ambient −15.92˚ and −5.73˚ respectively, in January 1970 according to IGRF.
3.2. Total Magnetic Intensity Reduction to the Equator (RTE)In geomagnetic methods the shape of magnetic anomalies due to vertical bodies depends on the inclination and declination angles of the geomagnetic field. In the north and south magnetic poles the main field plunges vertically and magnetic abnormalities have a symmetric shape, with the maximum or minimum located directly over the causative magnetic body. At low magnetic latitude (between 15˚S an 15˚N), it is not very easy to correlate the observed abnormal maxima and the positions of sources since magnetic signature of magnetized bodies at low latitudes always have two extreme values because of their bipolar nature. To remove this effect, as the name suggests, the reduction to the pole (RTP) transforms the data to the signal that would be measured at the magnetic poles [36] . This puts the limits of the magnetic abnormalities directly over their sources, like gravity abnormalities, thus making magnetic interpretation easier and more reliable. In low latitude, it not possible to apply RTP, the north-south direction is accentuated, and it is generally unstable and cannot be very useful. To facilitate the interpretation of the abnormalities at very low latitudes, we transform the analytic maps in the space domain: this is the case for the reduction-to-the-equator (RTE). After [37] , the magnetic data can also be reduced to the equator (RTE) such that the magnetic bodies will appear horizontal at the equator. The TMI grid data were then transformed using the RTE filter, instead of the reduction to the pole filter, since the study area located within the low magnetic latitudes (i.e. areas with geomagnetic inclination less than 15˚) in which a satisfactory reduction to the pole (RTP) of magnetic data is not possible. The TMI-RTE grid data of the area were processed er to transform and enhance magnetic anomalies associated with the edges of surface/near surface geological bodies, structures and depths. The methods used are the tilt angel derivative (TDR) and its total horizontal derivative (TH_DTD), analytic signal (AS) where the first vertical derivative (FDV) has been used. The MAGMAP two-dimensional Fast Fourier Transform (2-D FFT) filters package, EULER3D and SPI of GX’s (Geosoft eXecutable) in the Oasis Montaj v8.4 software was employed in the study.
3.3. The Tilt Angle Derivative (TDR) and Its Total Horizontal Derivative (THDR_TDR)TDR and THDR_TDR are used for mapping shallow basement structures and mineral exploration targets [38] . The tilt filter [39] [40] [41] [42] has also become a popular enhancement with an output given by TDR, used for enhancing features and causative body edge detection in potential field images. [39] suggested the tilt angle filter. It was developed later by others such as [42] and [43] . It showed a considerable interest because of its fundamental and practical simplicity [44] . This filter is defined as:
TDR = tan − 1 VDR THDR (1)
where VDR is the vertical derivative and THDR is the total horizontal derivative.
i.e.:
TDR = tan − 1 ( ∂ f ∂ z ( ∂ f ∂ x ) 2 + ( ∂ f ∂ y ) 2 ) (2)
The Tilt derivative (TDR) is similar to the local phase but uses the absolute value of the horizontal derivative in the denominator. Due to the nature of the arctan trigonometric function, all amplitudes are restricted to values between +π/2 and π/2 (+90˚ and -90˚) regardless of the amplitudes of VDR or THDR [42] . The Tilt derivatives vary markedly with inclination but for inclinations of 0˚ and 90˚, its zero crossing is located close to the edges of the model structures. Positive values are located directly above the sources while negative values are located away from them. Furthermore, the horizontal distance from the 45˚ to the 0˚ position of the tilt angle is equal to the depth to the top of the contact [43] [45] or the half distances between -45˚ and +45˚ [42] .
[41] introduced the total horizontal derivative of the tilt derivative (THDR_TDR) defined as the square root of the sum of the squares of the horizontal derivatives and the tilt derivative of the magnetic field. It is expressed as:
THDR_TDR = ( ∂ TDR ∂ X ) 2 + ( ∂ TDR ∂ Y ) 2 (3)
The total horizontal derivative of the tilt derivative (THDR_TDR) is independent of geomagnetic inclination like to the analytic signal (AS). The difference between these derivatives is that the former is sharper and generates better-defined maxima centered over the body edges. Another advantage of this independence, that it will generate useful magnetic responses for bodies having induced or remnant magnetization, or a mixture of both [46] .
3.4. Analytic Signal (AS) MethodSome authors [47] [48] introduced the concept of the analytic signal for magnetic interpretation and showed that its amplitude yields a bell-shaped function over each corner of a 2D body with polygonal cross section. [49] used the total magnetic gradient, which they called the 3D analytic signal to approximately estimate positions of magnetic contacts and obtain some depth estimates from gridded data. The analytic signal is a complex function formed through a combination of the horizontal and vertical derivatives of the magnetic anomaly. In 3D, the analytic signal of the magnetic anomaly field is defined as:
A ( x , y , z ) = ∂ f ∂ x i → + ∂ f ∂ y j → + ∂ f ∂ z k → (4)
where i ⇀ , j → and k → are unit vectors in the x , y and z directions, respectively, ∂ f ∂ y is the vertical derivative of the magnetic anomaly field intensity, ∂ f ∂ x and ∂ f ∂ y are the horizontal derivatives of the magnetic anomaly field intensity. The amplitude of the analytic signal in 3D is given by:
| AS | = ( ∂ f ∂ x ) 2 + ( ∂ f ∂ y ) 2 + ( ∂ f ∂ z ) 2 (5)
AS simplifies the magnetic signal of anomalies by centering anomalies over the magnetic body as well as, having peaks over the edges of wide bodies. Thus, a simple relationship between the geometry of the magnetic bodies and the transformed data are observed. The magnetic sources depths using the magnetic method are estimated from the ratio of the total magnetic AS to the vertical derivative analytic signal (AS1) of the total magnetic field.
AS1 = ( ∂ f v ∂ x ) 2 + ( ∂ f v ∂ y ) 2 + ( ∂ f v ∂ z ) 2 (6)
On the maximum amplitude:
D = AS AS 1 × N (7)
where f v is the first vertical derivative of the total magnetic field, and D is the depth to the magnetic body, N is known as a structural index and is related to the geometry of the magnetic source. For example, N = 4 for sphere, N = 3 for pipe, N = 2 for thin dike and N = 1 for magnetic contact [50] .
3.5. 3D-Euler DeconvolutionEuler deconvolution’s technique is an equivalent method based on the Euler’s homogeneity equation as developed by [50] following [51] ’s suggestion and operating on gridded magnetic data. [50] , and have explained the Euler deconvolution technique, more details in methodology and wider application regarding the Euler’s source depth solutions. These Euler depth solutions not only estimate the depth, but also delineate the horizontal boundaries [52] . In a general case, scattered data points cannot provide superior solutions [53] [54] . Various researchers have used 3D Euler deconvolution technique for source depth estimations [55] - [61] . The method is based on the concept that anomalous magnetic fields of localized structures are homogeneous function of the source coordinate and, therefore, satisfies Euler’s homogeneity equation. Usually the structural index (SI) is fixed and the locations and depths ( x 0 , y 0 , z 0 ) of any sources are found using the following equation:
∂ f ∂ x ( x − x 0 ) + ∂ f ∂ y ( y − y 0 ) + ∂ f ∂ z ( z − z 0 ) = SI ( B − f ) (8)
where f is the observed field at location (x, y, and z) and f is the base level of the field [regional value at the point (x, y, z)] and SI is the structural index or degree of homogeneity. Therefore, we have assigned a value of 1.0 as a structural index to locate the possible magnetic contacts because it is particularly good at delineating the sub-surface contacts. We used an overlapping moving window of 10 km by 10 km, a tolerance of 15% and a proportioned symbol base of 235.
3.6. Source Parameter Imaging (SPI) Technique (Local Wavenumber Technique)This method developed by [62] also known as local wavenumber technique, all the parameters that make up the source which include depth, dip and susceptibility contrast are computed from the complex analytical signal. [63] related the source depth to the local wavenumber (k) of the magnetic field which can be derived from the calculated total horizontal and vertical gradients of the RTE grid. In this method, the function used is the local wavenumber [61] given by:
k ( x , y ) = ∂ 2 f ∂ x ∂ y ∂ f ∂ x + ∂ 2 f ∂ y ∂ z ∂ f ∂ y + ∂ 2 f ∂ 2 z ∂ f ∂ z ( ∂ f ∂ x ) 2 + ( ∂ f ∂ y ) 2 + ( ∂ f ∂ z ) 2 (9)
For the dipping contact, the maxima of k are located direct over the isolated contact edges and are independent of the magnetic inclination, declination, dip, strike and any remnant magnetization. The depth is estimated at the source edge from the reciprocity of the local wavenumber, as follows:
Depth ( x = 0 ) = 1 k max (10)
where k max is the peak value of the local of number k over the step source.
4. Results and Discussion4.1. Total Magnetic Intensity MapThe present total intensity aeromagnetic (Figure 3) exhibits some different types of positive (mengata and red colors) and negative (light and dark blue colors) anomalies. The first are the strong positive anomalies and the second are the negative anomalies. The map reveals two prominent negative features in elliptical and broad shapes distributed in the north-east (at Nguiwas) and southwestern part (at Bana) and shows the maximum negative of −201.86 nT. These anomalies are trending NE-SW. We also observe some circular magnetics trends, with magnitudes above 111.60 nT. They are found in the south of N’Djombe along
530,000 m and 520,000 m latitudes. These circular trends with large magnitudes suggest the presence of highly magnetized cylindrical intrusive bodies within the basement. The map illustrates a large positive magnetic zone located to central part. Another positive magnetic anomaly is located at the western part of the map (at Bana), which attains amplitude of +120 nT and trends along E-W attitude. The correlation of TMI anomalies map and geological contact is weak. It is noted that the positive anomalies are limited to the west by a weak gradient (quasi-horizontal gradient) showing the intensity of the geological formations overlaping. The Bana-Okaa region is formed by a bipolar anomaly: a negative pole in Bana with a long wavelength of 44.4 km and negative amplitude of −201.86 nT, and a positive pole in Akaa with a high amplitude of +120 nT and wavelength of 54.6 km. In the Minta zone, there is also a horizontal gradient of oblong and NW-SE direction that seems to correspond to the Nkoambang-Nguelemendouka tectonic line highlighted on the geological map.
4.2. Total Magnetic Intensity Reduction to the Equator (TMI-RTE) MapThe total Intensity Magnetic Map (Figure 3) is reduced to the equator (Figure 4) using Oasis Montaj software v8.4. On this map (i.e. TMI-RTE) the examination of the amplitudes of anomalies also reveals that the maximum and
minimum values in the TMI-RTE map have reduced to +66.60 nT and increased to −208.73 nT. From Ovong to Bibé, positive TMI anomalies have shifted slightly vertically to the north. On the other hand, from the southwest to the west of the study area, the anomalies preserve generally their forms compared to TMI. The circular magnetics trends in the south of N’Djombe persist. On the TMI-RTE map, the study area can be subdivided into fourth magnetic zones, each having a unique magnetic anomaly pattern (Figure 4); this magnetic zoning is mainly dependent upon the magnetic properties (e.g. magnetic susceptibilities) of the underlying rock types.
The first zone occupies the north-eastern (at Nguiwass), south-western (at Bana) and south (Ovong) parts of the area and is underlain by the Precambrian crystalline basement rocks (migmatites, especially embrechites, quartzite in embrechite). It is characterised by very low, Broad and elongate wavelength (low wavenumber) anomalies with magnetic intensity amplitude varying from -208.73 to −78.44 nT (light and dark blue colors). The second zone occupies the west (north of Akaa), south-central (Mbaka-Tombo), north-west (Nkondo) parts of the area. It is underlain by the ectinites of the old metamorphic series of Nanga-Eboko (especially quartzites with minerals in the west part, feldspathics micaschists in the north part and schisto-quartz group of Akonolinga in the south-central). It exhibits high (positive) anomalies: amplitudes of the magnetic intensity in this zone range from +66.60 to +90 nT (magenta and red colors). The third zone occurs within the part of the area underlain by gneiss with two micas at Angossa II. It displays relatively low (negative) to moderate (positive) magnetic anomalies. Amplitudes of the magnetic intensity in this zone range from −54.32 to + 4.80 nT (green ligth and yellow ligth) (Figure 4). The fourth zone occupies the central-part (Tombo-Nguelemendouka-Minta) and north-west (Nkoambang-south of Nkondon) of study area. It exhibits intermediate (positive), long-wavelength magnetic anomalies trending mainly in the E-W direction. It is underlain by gneiss with two micas.
4.3. The Tilt Angle Derivative (TDR) Map and Its Total Horizontal Derivative (THDR_TDR)The TDR_TMI-RTE analysis of [39] (Figure 4) exhibits the geologic features like faults, which are depicted as magnetic lineaments. This method facilitates the horizontal location with extended edges. It is suggested that the zero-contour line (the bold black line) in the TDR_TMI-RTE map is the location of abrupt changes in magnetic susceptibilities between positive and negative anomalies which are particularly at the sharp gradient. Therefore, the zero-contour line represents the contact boundary of magnetic sources. Zero contours can be identified as light-yellow color which is separating the green color (negative values) and red colors (positive values) as seen in the color scale bar (Figure 5). Also, positive values are located directly above these magnetic sources while negative ones are located away from them. Generally, the TDR of TMI-RTE magnetic data shows an NE lineament trend in the south-west (Essong-Mbaka-Tombo). Also, the map shows E-W trends in the centre and ENE-WSW trends in the east. According to the TDR map, the study area thus presents the cumulative characteristic features of a brittle tectonic and tangential tectonic, which are materialized by the different trends obtained, probably reflecting the existence of an ancient tectonic heritage taken up in folds and sheared during late tectonic episodes in the Central Africa mobile zone. The tilt map allows for a combined analysis of 2D structure boundaries and depth. [43] showed that for the tilt angle operator, applied to pole-reduced data, for vertical contact, the null value of the angle corresponds to the limit of the structure and the distance between the contours ± π/4 radian (±45˚) and the zero-valued contour is equal to the depth of the structure. By applying the method of [43] , the depth varies from a few hundred to north of the study area to over 3000 meters in the confined area between Nkoambang, Tombo and Lembé in the south-central part of the region.
A total horizontal derivative filter was applied to the tilt derivative of the TMI-RTE grid data to generate the THD_TDR anomaly map (Figure 6). Figure 6 shows the THDR of the TDR. The THDR_TDR preserves the amplitude enhancement by its ability to define edges of well-defined maxima. So, the amplitude of the THDR_TDR is related to the reciprocity of the depth to the top of the
source [64] . The tilt angle overcomes the problem of the shallow and deep sources by dealing with the ratio of the vertical derivative to the horizontal derivative; the tilt derivative will be relatively insensitive to the depth of the source and should resolve shallow and deep sources equally. However, from Figure 6 and its colored bar scale, the depth to the top of the sources ranges from 380 to about 2800 m all over the area except for dark blue area at the confined area in the south of Nguélémendouka, in the eastern part of the study area where its depth exceeds this value.
4.4. Analytic Signal (AS) MapThe amplitude of the analytic signal depends very little on the direction of magnetization [49] and is almost independent when the sources are vertical [65] . One of the advantages of the analytical signal is that it makes it possible to locate the position of the sources in the horizontal and vertical plane. Basement depth calculations were performed in the study area using AS, which was applied to the TMI-RTE data grid. The AS map of (Figure 7(a)) makes it possible to limit the contacts of the geological bodies of strong magnetization on this map. The limits of the intrusive bodies and faults are well highlighted. There is a linear structure at Nkondon while the intrusive bodies are grouped between N’Djombé and
Minta north of the study area, they are found in the south of the area in Bana and Mbaka. The map of the first vertical derivative for the TMI-RTE (Figure 7(b)) shows successively positive and negative anomalies that were almost invisible on the TMI and TMI-RTE, the positions and trends of these anomalies are similar to those of the TDR map (Figure 5). The analytical signal map of the first vertical derivative (Figure 7(c)) is similar to the TMI-RTE AS map. The pseudo-circular shape anomalies have maximum amplitudes. According to equation (8) the AS data grid of the TMI-RTE board (Figure 7(a)) is divided by the data grid of the AS1 board (Figure 7(c)) to estimate the depth of the magnetic contacts of the base of the board the study area (Figure 7(d)). The map in Figure 7(d) highlights the spatial location of various magnetic sources at different depths. In general, the depth varies from 153.45 m to about 2685.24 m below sea level. It is noted that the areas in which the sources of anomalies are the deepest (at more than 2685.24 m) are in Okaa, Efoulan, Lembé and Tombo, in the embroites according to the geological map.
4.5. 3D-Euler Deconvolution (ED) MapEuler’s deconvolution is one of the most reliable methods for obtaining depths under cover. In this investigation, ED solutions were calculated for IS = 1 for
thin-layer boundary (sill, oblique intrusive vein, banded iron formation, etc.) or faults [50] . The size of the window used is 10 km × 10 km with a maximum depth tolerance of 15%. A good grouping of solutions indicates that the location of the source is well resolved, and a dispersion indicates that the solutions must probably be ignored [50] . The Euler depth solution map is illustrated in Figure 8. The analysis of this map shows the linear clustering circles are suggested to be the result of faults and or contacts with depth values ranging between 245.24 m
and 2273.68 m. The non-uniformity of the depths of said contacts in the area suggests that all the outlines of the box do not have the same origin. These solutions are trending in E-W, ENE-WSW and NE-SW directions.
On Euler’s solutions map, the limits of the faults intrusive bodies are perfectly distinguished. To the north, at Ngobadé in the granites; in the center, between Nkoambang and Nguélémendouka; in the south, at Angossas II, the shape of the Euler solution groupings would characterize the limits of the intrusive bodies in the basement, whereas the straight and continuous alignment of the Bibé, Minta, Efoulan and Mbaka solutions would, on the other hand, characterize the normal faults hidden in the covers.
4.6. Interpretative Structural MapAn interpretative structural map has been drawn from maps of Figure 5, Figure 6 and Figure 8 to highlight the different lineaments (Figure 9). The interpretative structural map simply reveals the structural complexity in the basement, this map is characterized by trends of lineaments.
The analysis of the interpretative structural map of study area shows four predominant structural trends having variable intensities and lengths. These are the E-W, ENE-WSW and NE-SW trends, representing the most predominant
tectonic trends affecting the investigated area as deduced from the magnetic point of view. The relationships among these trends suggest that, the area was subjected to more than a single tectonic event. Vertical accidents characterized by nearly rectilinear solutions have NE-SW directions at Okaa, E-W at Nkondon, Ovong. The deepest accidents are of E-W main directions with depths of over 2300 m and are in Efoulan, Lembé and Tombo. The folding system-oriented E-W to NE-SW, are in accordance with the directions highlighted in geological investigations focused the Awaé-Ayos strike-slip shear zones (southern Cameroon): Geometry, kinematics and significance in the late Pan-African tectonics by [66] in adjacent areas situated below the present study area. The ENE-WSW contacts after [67] , is associated to the second deformation D2, characterized by folds (S2), foliation (F2). At the regional scale, the near surface NE-SW contacts who represent the regional deformation events D2 (compression) and D3 (wrenching) may correlate with the development of the Centre Cameroon Shear Zone witness by the Foumban Shear Zone.
The tectonic features put in evidence have linkages with faults and folds lines-oriented E-W, ENE-WSW and NE-SW, as identified by geophysical surveys carried out in gravity [68] [69] [70] [71] , audiomagnetotelluric [6] and aeromagnetic [11] in areas situated around the current study area.
4.7. Source Parameter Imaging (SPI) MapThe Source Parameter Imaging (SPI) module of the Oasis Montaj software was applied to the TMI data of the study area. The SPI (Source Parameter Image) method is a technique for calculating source depths from magnetic data. It is a tool based on the extension of the complex analytic signal to estimate magnetic depths [72] . The derived map (SPI) is illustrated in Figure 10 and highlights the spatial location of various magnetic sources at different depths. This map shows that generally, the north (from Nkoambang to Ngodabe) and south (Angossas II) parts of the study area are shallow. These areas are illustrated in blue, green and yellow colors represent depths ranging from 200 to 766.55 m. They can be characterized by a low magnetic susceptibility. The central part (from Tombo to Nkoambang) is a deep zone and is characterized by orange, red and magenta colors with depths ranging from 988.19 to 2800 m, which may be a high magnetic susceptibility.
The SPI depth map (Figure 10) shows a good similarity with the depth map constructed using the AS technique. However, the depth varies from about 200 m to about 2800 m.
6. ConclusionThis study is based on the analysis and interpretation of aeromagnetic data to define the subsurface basement depth and contacts location’s inference of the study area. First, the Total Magnetic Intensity Map reduced to the equator (TMI_RTE) is used to locate the magnetic anomalies directly above their causative sources. This map reveals various causative sources, as well as varying
depths and compositions, with different anomalies of varying frequencies and amplitudes. The tilt angle derivative (TDR) was used to locate the edges of this TMI-RTE. Positive values should be located above the magnetic sources while negative values are located away from them. The half distance between ±π/4 (±0.785) Radian was used to calculate the depth to these edges. By applying [43] method, the depth of basement surface reaches to 3000 m in the south-west and eastern parts of the study area, while it reaches 227 m in the north and western parts. The total horizontal derivative of the tilt derivative map (THDR_TDR) shows these edges as sharper and its values are the reciprocal of the depth to these contacts. The deduced average depths above them range from 380 to about 2800 m. Euler deconvolution is applied to illustrate the distribution of contacts or faults and to estimate their depths which range from 245.24 to 2273.68 m. Accordingly, the constructed interpretative structural map of study area is configured by a set of these contacts or faults which oriented in E-W, NE-SW and ENE-WSW, directions. The present results of trends agree with gravity studies in adjacent areas which highlight a reseau of faults-oriented W-E, and the audiomagnetotelluric data analysis that puts in evidence a secondary fault line with NE-SW general trend [43] . The orientation of the basement geological structures inferred from the magnetic maps suggests that they are products of the Brasiliano/Pan-African orogeny. Two main techniques were used to calculate the depth to the magnetic basement sources. AS and SPI were used to calculate the depth to the magnetic basement sources. They reflected similar results for estimating the basement depths. For both, the depth ranges from 150 to 2800 m. The 2-D modeling tool was used for the data profile modeling, where more than one anomaly is considered in the process. The models indicate that, the granitic basement rocks range between 550 m and 4100 m. Finally, the methods used in this study (TDR, THDR_TDR, 3-ED, AS and SPI) gave us similar results to the depth of the basement rocks, ranging in depth between 150 and 3000 m as the average range.