Towards Understanding the Source of Brine Mineralization in Southeast Nigeria: Evidence from High-Resolution Airborne Magnetic and Gravity Data

: Investigation into understanding the genesis of brines in southeast Nigeria was carried out utilizing high-resolution potential ﬁeld (HRPF) data. This study reveals that igneous intrusions and associated hydrothermal ﬂuids are responsible for brine generation. The obtained result of the analytic signal revealed the locations and spatial distribution of short- and long-wavelength geologic structures associated with igneous intrusions. The low pass ﬁltering, upward continuation, and 2D modelling procedures showed key synclinal structures which coincided well with the location of brine ﬁelds. The results showed that salt ponds are common in the neighborhood of igneous intrusions. To validate this ﬁnding, a conceptual model describing igneous-related hydrothermal circulation systems that are driven by convective cells of the hydrothermal ﬂuid and overburden loads was generated. This model ﬁts reasonably well into the overall stratigraphic and geologic framework of the study area.


Introduction
Since the early twentieth century, the origin of brine fields in the Benue Trough and adjacent sub-basins has been a point of contention [1,2]. Brines can be found in ponds, springs, drilled water boreholes, and hand-dug wells [3]. In terms of their genesis in the Benue Trough (BT), [3,4] summarized three possibilities proposed by previous studies. They include formation or a connate water source [5][6][7], evaporite or a solid source [8][9][10], and a hydrothermal source [8][9][10][11][12][13][14]. Most of the prior studies have been focused on a single occurrence or projections, and some lack relevant hydro-chemical data [3]. In general, these studies determined that the brines in the Trough came from either connate water or evaporite.
Hydro-geochemical investigation of the Middle and Lower Benue Trough reveals that brines are the result of halite dissolution and fossil seawater sources [4]. In [15,16], the authors conducted similar research that linked brines to a marine source. In [17], on the other hand, the authors suggested that connate water was the primary source of brines in the BT. Although [1] suggested an evaporite source, [4] stated that ''there was no proof of evaporites in the BT". In the western Qaidam basin, meteoric water was identified as

Geology
The study area covers some geologic regions of the Abakaliki Anticlinorium (AA), Ikom-Mamfe Rift (IMR), and Obudu Plateau (OP) (Figure 2). The OP occupies the northeastern flank. It is edged in the west by AA and southeast by IMR. The IMR which intruded the study territory at the southeastern flank is bounded by the AA in the west, northwest, and north, and the OP in the northeast. The AA occupies southwestern, western, northwestern, and northern domains.

Geology
The study area covers some geologic regions of the Abakaliki Anticlinorium (AA), Ikom-Mamfe Rift (IMR), and Obudu Plateau (OP) (Figure 2). The OP occupies the northeastern flank. It is edged in the west by AA and southeast by IMR. The IMR which intruded the study territory at the southeastern flank is bounded by the AA in the west, northwest, and north, and the OP in the northeast. The AA occupies southwestern, western, northwestern, and northern domains.
The Bamenda Massif is an extension of the OP, which is one of the Nigerian basement outcrops in southeast Nigeria [68,69]. The region's lithological differences include highgrade metamorphic rocks, primarily gneisses, and schists, intruded by un-metamorphosed dolerites, granites, aplites, and quartzo-feldspathic veins, and they are heavily migmatized [68]. Rocks from this area have been dated to be Eburnean, Archaean, and Pan-African in age [70]. Workers concluded that the evolutionary history of the southeast basement in Nigeria is related to the mobile Pan-African belt in central Africa, after comparing the lithologies and ages of rocks from the central African Fold Belt, northern Cameroon, and southeast Nigeria basement complexes [68,70]. The Pan-Central-African belt is the result of a continent-continent collision, with the Congo craton's northern edge acting as a passive margin, while the western Cameroon domains and Adamawa-Yade acted as active margins [2,68]. The OP is associated with migmatitic gneisses, which are classified as garnet-hornblende gneiss, garnet-sillimanite gneiss, or simply migmatite gneiss [68,71].
The IMR is an eastern extension of the Lower Benue Trough that runs into Cameroon, and terminates below the Tertiary-Recent cover of the Cameroon Volcanic Line (CVL) [72]. Igneous intrusions in the IMR, which were caused by Tertiary-Recent tectonic processes related to the CVL, resulted in extensive deformations and metamorphisms of the geologic materials in the region. As a result, the covering sedimentary sequences became severely fractured, baked, deformed, and domed [63].
The Asu River Group (ARG), which includes conglomeratic sandstones, conglomerates, mudstones, shales, calcareous, and carbonaceous rocks, is the first sedimentary group in the IMR [73]. The ARG sits on highly fractured Precambrian basement rocks [73]. The Eze-Aku Formation (EAF) was deposited during the Turonian regression period. The post-Santonian Nkporo-Afikpo Shale Formation overlies the EAF. The sandstone, mudstone, and shale strata are the foremost rock components of this formation [29]. The Bamenda Massif is an extension of the OP, which is one of the Nigerian basement outcrops in southeast Nigeria [68,69]. The region's lithological differences include highgrade metamorphic rocks, primarily gneisses, and schists, intruded by un-metamorphosed dolerites, granites, aplites, and quartzo-feldspathic veins, and they are heavily migmatized [68]. Rocks from this area have been dated to be Eburnean, Archaean, and Pan-African in age [70]. Workers concluded that the evolutionary history of the southeast basement in Nigeria is related to the mobile Pan-African belt in central Africa, after comparing the lithologies and ages of rocks from the central African Fold Belt, northern Cameroon, and southeast Nigeria basement complexes [68,70]. The Pan-Central-African belt is the result of a continent-continent collision, with the Congo craton's northern edge acting as a passive margin, while the western Cameroon domains and Adamawa-Yade acted as active margins [2,68]. The OP is associated with migmatitic gneisses, which are classified as garnet-hornblende gneiss, garnet-sillimanite gneiss, or simply migmatite gneiss [68,71].
The IMR is an eastern extension of the Lower Benue Trough that runs into Cameroon, and terminates below the Tertiary-Recent cover of the Cameroon Volcanic Line (CVL) [72]. Igneous intrusions in the IMR, which were caused by Tertiary-Recent tectonic processes related to the CVL, resulted in extensive deformations and metamorphisms of the geologic materials in the region. As a result, the covering sedimentary sequences became severely fractured, baked, deformed, and domed [63]. The Campanian Nkporo Shale, Coniacian Awgu Shale, Turonian Eze-Aku Shale, and Albian Asu River Group are among the strata found in the AA [74]. The Albian ARG is made up of fissile, heavily fractured, bluish-black shales with very few sandstone strata [74]. The EAF is made up of calcareous sandstones, calcareous siltstones and shales, and thin sandy and shelly limestones [75]. Grey bluish shales, marine fossiliferous limestones, and calcareous sandstones from the Coniacian period make up the Awgu Shales [74]. The Awgu Shales are overlain by the Campanian Nkporo Shales, which are predominantly marine with some arenaceous sandstone units ( Figure 3).
The folding of the overlying layers was caused by massive Santonian tectonic processes that occurred in two periods [29,74]. The Abakaliki Anticlinorium arose from the dominantly compressional nature of the forces. In [76], the authors compared the geological development of the Abakaliki province to that of a complete orogenic cycle encompassing sedimentation, magmatism, metamorphism, and compressive tectonics in thorough research on the geology of the province. According to [76], the compression that caused the large-scale folding and cleavage was directed at N 155 • E. As a result of the magmatism, multiple intrusive masses were injected into the Eze-Aku and Asu River Group shales [74].
The Campanian Nkporo Shale, Coniacian Awgu Shale, Turonian Eze-Aku Shale, and Albian Asu River Group are among the strata found in the AA [74]. The Albian ARG is made up of fissile, heavily fractured, bluish-black shales with very few sandstone strata [74]. The EAF is made up of calcareous sandstones, calcareous siltstones and shales, and thin sandy and shelly limestones [75]. Grey bluish shales, marine fossiliferous limestones, and calcareous sandstones from the Coniacian period make up the Awgu Shales [74]. The Awgu Shales are overlain by the Campanian Nkporo Shales, which are predominantly marine with some arenaceous sandstone units ( Figure 3). The folding of the overlying layers was caused by massive Santonian tectonic processes that occurred in two periods [29,74]. The Abakaliki Anticlinorium arose from the dominantly compressional nature of the forces. In [76], the authors compared the geological development of the Abakaliki province to that of a complete orogenic cycle

Data Acquisition
The Nigerian Geological Survey Agency (NGSA) provided the airborne gravity and magnetic data used in this investigation. Between 2005 and 2010, Fugro Airborne Surveys, Canada, measured, reduced, and compiled the high-resolution geophysical datasets, which were then submitted to the NGSA in digitized and gridded forms. The data were collected along 826,000 lines using the Flux-Adjusting Surface Data Assimilation System (FASDAS) with tie-line spacing, flight-line spacing, and terrain clearance of 0.5 km, 0.1 km, and 0.08-0.1 km, respectively.
The tenth (10th) generation of the International Geomagnetic Reference Field (IGRFversion 4.0) and International Gravity Standardization Net 1971 (IGSN71) algorithms were used to subtract regional fields from observed HRPF data. The IGSN71 and IGRF, both of which are widely used and approved, provide consistency in potential field exploration techniques [69]. The employed HRPF data in this study were reduced and processed to total magnetic intensity (TMI) and Bouguer gravity gridded (BG) maps ( Figure 4).
were used to subtract regional fields from observed HRPF data. The IGSN71 and IGRF, both of which are widely used and approved, provide consistency in potential field exploration techniques [69]. The employed HRPF data in this study were reduced and processed to total magnetic intensity (TMI) and Bouguer gravity gridded (BG) maps ( Figure  4).

Methodology
Local datum transformation and projection technique were used to record the potential field data in the World Geodetic System 84 (WGS-84) and Universal Transverse Mercator coordinate system at zone 32 of the northern hemisphere (UTM-32N). Using the Oasis montaj "add grid" menu, the gridded data were loaded into the toggle project explorer platform. The data were loaded into the MAG-MAP, source parameter imaging (SPI), Euler deconvolution, and GM-SYS tools, which generated control files for the various enhancement and modelling methods.
Filtering algorithms deliberately enhance anomalies from a certain set of geologic sources relative to anomalies due to other geologic sources and they are used in potential field data enhancements [77]. The main igneous intrusions in the research area were delineated using typical potential field (PF) data enhancement methods such as the analytic signal (ASig) [78][79][80][81], low pass filter [82], and upward continuation (UPWC) method [53,54]. In addition, 2D forward modelling was operated to map igneous intrusions, estimate sediment thicknesses, and define basement topography.
The ASig filter [83,84] generates maximum responses over magnetic/gravity anomalies and detects the edges of magnetic/gravity source bodies. This filter is commonly applied at low-magnetic latitudes due to the in-built complication associated with the RTP technique. The most important advantage of the analytical signal is that, in 2D cases, it does not depend on the direction of magnetization, but this is incorrect in 3D case [78]. In [78], the authors demonstrated that the ASig amplitude can be obtained from the three orthogonal derivatives of the potential field as: where, A is the measured PF. The low pass filter is based on the method proposed by [82], and the filter cut-off wavelength is the only variable parameter [85]. Although it passes low-frequency signals, and weakens signals with frequencies above the cut-off frequency, low-pass filtering is used to eliminate unwanted short-wavelength anomalies [86]. The rectangular low-pass filter in a 1D Fourier transform is provided by: where L(k) is the amplitude spectrum of the transfer function of the rectangular filter and k c is the cut-off frequency. In analyzing regional magnetic/gravity structures originating from deep-seated PF sources, UPWC is used. The upward continuation filter transforms the observed magnetic/gravity field on a surface to a higher level. In comparison to deep causative sources, this enhancement reduces the effect of near-surface bodies [53]. The wavenumber domain approach for UPWC [41] is expressed as follows: where, h is the height of continuation. This procedure decreases progressively with increasing wavenumber, reducing the higher wavenumbers more severely, thus generating a map in which more regional anomalies predominate [87]. The 2D modelling method involves developing a geologic hypothetical model and computing magnetic/gravity responses, applying [88][89][90]. Every crustal block has a certain susceptibility and/or density value. The anomaly across the entire profile is the sum of all the crustal block contributions. The interpretation of PF anomalies is based on identifying the probable structures, locations, and physical properties of the geologic features that created the anomaly. Two profiles in the east-west direction were obtained from the TMI and BG data. The PFs for the sedimentary top and basal basement structural cross-section were estimated iteratively until acceptable matches between the observed and synthetic curves were achieved. Using programs found in Oasis montaj version 7.0.1 (OL), potential field data enhancement, automatic depth estimation, and 2D forward modelling operations were carried out (2008). The inverse problem normally associated with potential field data is ill-posed thus making the solution unstable and non-unique [27,91]. A consistent solution for such a problem can be acquired by having sufficient geologic knowledge and the use of improved techniques in data corrections, enhancements and interpretations [92]. Tight folds, cleaves, and igneous intrusions such as basic sills and sub-volcanic intrusions characterize the Cretaceous depositions in the study area [93]. In the Middle and Lower Benue Trough, [3] documented shallow volcanics and intrusions in the vicinity of salt ponds. PF methods can be operated to investigate magmatic intrusions, mineralization, and related geologic structures [8,20,43]. Enhanced PF data showed variable gravity and magnetic disparities from numerous causative sources caused by short-and long-wavelength anomalies [31]. According to [27], mineralization is typically associated with locations characterized by complex geologic formations, created by tectonic processes. Low-frequency structures on the improved maps were greatly highlighted to demarcate areas marked by long-wavelength anomalies. To map the main tectonics and depocenters in the research area, these anomalies were mapped using ASig, low pass, and UPWC filters.

Results
The highest and lowest magnetic (pink = 0.0891 nT/m and blue = 0.0026 nT/m) and gravity (pink = 0.00215 mGal/m and blue = 0.00040 mGal/m) intensities can be easily identified ( Figure 5). The eastern section of the investigated area ( Figure 5) is dominated by basement biotite-gneiss and granite rocks of OP, where Kakube, Iso-Bendegheg, and Odumekpang fall. This region is characterized by basement rocks. They are believed to be the principal origin of high magnetization and density observed in the OP. Edor, Obubra, and Agbaragba regions that correspond with IMR have high magnetization and density believed to be caused by the Tertiary-Recent igneous intrusions related to the CVL [63]. Sparsely distributed high, moderate, and low potential field signatures occupy the remaining parts of the investigated area. This region is part of the AA, which is characterized by a post-depositional tectonic event [27]. Low gravity and magnetic strengths are also present in isolated locations denoted by various blue colors (indicating depocenters). The main synclinal structures (defined by a blue color) were delineated using the low pass [82] (Figure 6) and UPWC (Figure 7) [78] filters, which roughly overlap with the zones of Obubra (southern), Uburu (southwest) and Okpoma (northeast) areas that fall under the Ikom-Mamfe Rift, Afikpo and Ogoja Synclines, respectively [58,94]. These structures sandwiched the main Santonian [93] and Tertiary-Recent [63] tectonic intrusions (red-pink color) of the AA and IMR, respectively. Some geophysical studies have reported the coexistence of intrusions and troughs in the BT [74,95]. The OP eastern part, which is dominated by magnetite, is characterized by intrusions and outcrops of igneous basements [9]. The main synclinal structures (defined by a blue color) were delineated using the low pass [82] (Figure 6) and UPWC (Figure 7) [78] filters, which roughly overlap with the zones of Obubra (southern), Uburu (southwest) and Okpoma (northeast) areas that fall under the Ikom-Mamfe Rift, Afikpo and Ogoja Synclines, respectively [58,94]. These structures sandwiched the main Santonian [93] and Tertiary-Recent [63] tectonic intrusions (red-pink color) of the AA and IMR, respectively. Some geophysical studies have reported the coexistence of intrusions and troughs in the BT [74,95]. The OP eastern part, which is dominated by magnetite, is characterized by intrusions and outcrops of igneous basements [9].  To view the lithologic units of the underlying basement based on their susceptibilities and densities, the high susceptibility (0.00057 in cgs units) and density (2.91 g/cc) values are due to basic rocks, whereas lower susceptibility (0.0003 in cgs units) and density (2.81 g/cc) values are due to acidic rocks. The models (Figures 8 and 9) reveal that the Cretaceous deposits are severely fractured, folded, and baked [26,57]. Again, normal fault blocks associated with the intrusions were delineated by the models. Profile 1 (Figure 8) that cuts across part of AA and ends at OP (Figure 4) is characterized by two prominent igneous intrusions related to the Santonian AA [58,93]. The location of the igneous intrusion at the western end of profile 2 ( Figure 9) seems to match closely with the position of the intrusion in Figure 8. This indicates the elongated nature of the anticlinal structure of the AA that trends in the N-S direction (Figures 6 and 7). Towards the eastern part of profile 2 (Figure 9), the intrusion is outcropped in Agbaragba. Within this area and neighborhood, there are several reported extrusive rocks such as syenites, basalts, and trachytes [96,97] related to the CVL [63]. Because of the proliferation of intrusions [93] and basement rocks in outcrop sections in the OP [68,98], the investigated area is characterized by depths generally <3000 m. This depth estimate coincides relatively well with previous findings in the area [27,31,32,35,37]. To view the lithologic units of the underlying basement based on their susceptibilities and densities, the high susceptibility (0.00057 in cgs units) and density (2.91 g/cc) values are due to basic rocks, whereas lower susceptibility (0.0003 in cgs units) and density (2.81 g/cc) values are due to acidic rocks. The models (Figures 8 and 9) reveal that the Cretaceous deposits are severely fractured, folded, and baked [26,57]. Again, normal fault blocks associated with the intrusions were delineated by the models. Profile 1 (Figure 8) that cuts across part of AA and ends at OP (Figure 4) is characterized by two prominent igneous intrusions related to the Santonian AA [58,93]. The location of the igneous intrusion at the western end of profile 2 ( Figure 9) seems to match closely with the position of the intrusion in Figure 8. This indicates the elongated nature of the anticlinal structure of the AA that trends in the N-S direction (Figures 6 and 7). Towards the eastern part of profile 2 (Figure 9), the intrusion is outcropped in Agbaragba. Within this area and neighborhood, there are several reported extrusive rocks such as syenites, basalts, and trachytes [96,97] related to the CVL [63]. Because of the proliferation of intrusions [93] and basement rocks in outcrop sections in the OP [68,98], the investigated area is characterized by depths generally <3000 m. This depth estimate coincides relatively well with previous findings in the area [27,31,32,35,37].

Discussion of Results
The LBT is relatively well known because of geoscience investigations for natural resources. Hydrocarbon, lead, zinc, barite, and brine are commonly explored in southeast Nigeria [3,63,93]. The occurrence of brines and genesis in the LBT have been investigated by several geoscientists [1,3,4,[15][16][17]65,66,99] with contrasting reports. In [17,65,66], the authors stated from their various geophysical studies that brine fields are characterized by multi-layered saline zones in the subsurface. In [4,15], the authors suggested that these brines are products of the dissolution of halite and palaeo/fossil seawater. In [16], the authors also opined marine rather than a continental source for these brines. While [1] suggested evaporite minerals and chalcophile element sources, [3] suggested that brines originated from connate water.

Discussion of Results
The LBT is relatively well known because of geoscience investigations for natural resources. Hydrocarbon, lead, zinc, barite, and brine are commonly explored in southeast Nigeria [3,63,93]. The occurrence of brines and genesis in the LBT have been investigated by several geoscientists [1,3,4,[15][16][17]65,66,99] with contrasting reports. In [17,65,66], the authors stated from their various geophysical studies that brine fields are characterized by multi-layered saline zones in the subsurface. In [4,15], the authors suggested that these brines are products of the dissolution of halite and palaeo/fossil seawater. In [16], the authors also opined marine rather than a continental source for these brines. While [1] suggested evaporite minerals and chalcophile element sources, Ref. [3] suggested that brines originated from connate water.
Modern investigations by [10,[20][21][22][23][24][25][100][101][102][103] connected the origin of brines in a rift environment, such as LBT, to igneous intrusions. Previously, sodium chloride and hydrochloride acid were detected by [104] in the emanations of volcanoes. In addition, Refs. [105,106] discussed the volcanic origin of salt. In [3,26,100], the authors reported the occurrence of brine in the neighborhood of igneous intrusions in the BT. Figures 6 and 7 indicated the locations of the Afikpo syncline (Uburu and the surrounding area), Obubra (in the c), and the Ogoja syncline (Okpoma and the adjoining region), represented by a blue color. These areas are depocenters bordering intrusions (represented by red-pink color) associated with the Santonian AA [74] and Tertiary-Recent intrusions of the IMR [7]. These synclinal structures, that are dominated by argillite, coincide with the sites of the major brine fields in the investigation area [1,4,16,17,66,99]. Intrusions delineated by Figures 8 and 9 occur in the neighborhood of the brine fields. This finding validates the results of Figures 7 and 8. Igneous intrusion systems in rifted basins are usually distinguished by networks of interrelated, laterally, and vertically wide-ranging complexes of dykes and sills that transgress basin stratigraphy [42]. These intrusions are associated with normal fault blocks, faults, uplifts, and folds. The faults and other openings serve as a pathway for the hydrothermal fluid's migration upward. The widespread occurrence of igneous intrusions in the investigated area signifies a critical geological risk in hydrocarbon surveys [101].
Furthermore, intrusions are commonly connected to hydrothermal fluid [21,40,100] that is as salty or even saltier than seawater, and may have some traces of dissolved minerals such as lead, zinc, copper, and gold. In the LBT, there are massive occurrences of lead-zinc-barite coexistence with salt ponds [3,28,31]. The presence of salt in the water halts the metallic minerals from precipitating out of the brine, as the chlorides in the salt preferentially bond with the metals [22,100]. Nevertheless, since the brine is hot, the minerals dissolve more easily [40]. As magma cools, it frees its super-heated, mineralenriched water (metalliferous brines) into adjoining rock [21,40]. As they travel long distances laterally, they experience modifications in pressure and/or composition [100]. The hydrothermal fluid becomes diluted once they come into contact with meteoric water (groundwater). Fluid flow in the fractured upper crust is usually driven by hydraulic gradients, which may perhaps result from a number of different possible causes and imbalances, including thermal and chemical disequilibrium, topography, overburden loads [100], and attendant convective cells in the hydrothermal system. They drive the brines up through hydraulic boundary faults/fractures via porous and permeable strata until oozing takes place at the surface ( Figure 10). This conceptual model was created based on the geologic, stratigraphic ( Figure 3) and tectonic history of the study area. Additionally, geodynamic information on the robust thermally driven convection process [105], related heat, and movement of hydrothermal fluid [22], served as a control in the design of the model. The metals are precipitated out when the brines rise and cool [22]. The cool brines are then trapped by argillite close to the Earth's surface and occur as salt ponds such as those present at Uburu, Okposi, Okpoma, etc. in the studied area. The absence of hot springs in the studied area may be due to a lack of deep-reaching vertical circulation systems [107,108]. Moreover, ascent channels for hydrothermal fluids are very conducting structures allowing high flow rates so that hot brines can reach the surface environment at high temperatures [108]. The conceptual model (Figure 10) of the hydrothermal system of the LBT agrees with the Darcy flow law [109], describing fluid flow through porous media. This defines the ability of a fluid to flow through a porous media such as rock. It relies on the fact that the amount of flow between two points is directly related to the difference in pressure between the points, the distance between the points, and the interconnectivity of flow pathways in the rock between the points. The measurement of interconnectivity is called permeability.
The Darcy law is expressed as: where,  Moreover, ascent channels for hydrothermal fluids are very conducting structures allowing high flow rates so that hot brines can reach the surface environment at high temperatures [108]. The conceptual model (Figure 10) of the hydrothermal system of the LBT agrees with the Darcy flow law [109], describing fluid flow through porous media. This defines the ability of a fluid to flow through a porous media such as rock. It relies on the fact that the amount of flow between two points is directly related to the difference in pressure between the points, the distance between the points, and the interconnectivity of flow pathways in the rock between the points. The measurement of interconnectivity is called permeability.
The Darcy law is expressed as: where, → q is the specific discharge vector per cross sectional area (m 3 s −1 m −2 ) with the components q x, q z , q z, (K) (m s −1 ) the tensor of hydraulic conductivity, K (kg m −3 ) the density of the fluid, g (m s −2 ) the acceleration due to gravity, and ∇P (kg m −2 s −2 or Pa m −1 ) the vector of the pressure gradient.

Conclusions
Investigation connecting igneous intrusions and associated hydrothermal fluids as a brine source in a rifted environment such as BT was carried out in southeastern Nigeria. To map these intrusions and determine their spatial distributions within the study area, HRPF data were used. The ASig results showed the spatial distribution of the short-and long-wavelength geologic structures. The main igneous bodies and bordering synclines, which coincide with the sites of Uburu, Obubra, and Okpoma salt ponds, were delineated by the low pass, UPWC, and 2D GM-SYS results. In general, the low-frequency maps and 2D models showed brine field sites in the neighborhood of magnetic intrusions, which are commonly associated with metalliferous brines. To fit these interpretations into the overall stratigraphic and geologic settings of the area, a conceptual model of the brine source was generated. This model is more akin to a hydrothermal system that is driven by associated convective cells of the hydrothermal fluid and overburden loads. Furthermore, studies involving geochemical analyses of the brines and adjoining igneous rocks should be carried out to compare their elemental composition, which will be the subject of future research.