Structural Analysis of Aeromagnetic Data and Digital ...

ISSN (Print): 2476-8316

ISSN (Online): 2635-3490 Dutse Journal of Pure and Applied Sciences (DUJOPAS), Vol. 7 No. 1 March 2021

*Author for Correspondence Bala B., DUJOPAS 7 (1): 180-190, 2021 180

Structural Analysis of Aeromagnetic Data

and Digital Elevation Model for Geothermal Mineralization Potentials of Peninsular Malaysia

Bala Balarabe

Department of Physics, Faculty of Physical Sciences,

Ahmadu Bello University, Zaria

Email: [email protected]

Abstract The present study was conducted to reveal the predominant geological structural and tectonic controls, their relationships from surface to the subsurface, and depths to basement structures, which could harbor mineralization and geothermal potentials of the Peninsular Malaysia. The Earth Anomaly and DEM data used, indicated that the dominant magnetic anomalies lie on the NW-SE, NWW-SEE, N-S, and E-W directions. The regions having high data conformity and lineaments density, could likely be attributed to mineral and geothermal occurrences. The featuring of magnetic lineaments aligning with hot springs are possible indications of conduits for geothermal and mineral fluids migration. The depth to the basement structures varies from 1.0 to 20.0 km with an average of 5.0 km, suggesting a decrease of the sedimentary cover. Therefore, the study revealed prominent structural discontinuities representing subsurface responses, possibly linked to high deformation events in the Peninsular. Hence, uncovering the vast geothermal and mineral potentials for exploration and tourism development. Keywords: DEM, EMAG2, Enhancement techniques, Geothermal potentials, Peninsular Malaysia, Introduction Magnetic anomalies often provide vital subsurface geological information and bodily features of the Earth’s crust. The information is mostly on depth to magnetic basement, magnetic susceptibilities, and shape and properties of magnetic sources, aiming at peculiar studying objectives and/or magnetic outlines/ trends. There exist a linkage among evident magnetic anomalies, and the Earth’s crust thermal and mineral resources. Magnetic susceptibility of a rock unit generally varies with the type of lithology, geological stratigraphic/ structural, hydrological and thermal units (Li et al., 2010). For instance, pluton or igneous intrusion is noticeable in a magnetic study owing to the disparity in magnetic susceptibility per the adjacent rock. In a situation of high magnetic susceptibility rocks, the local magnetic field will be strong against the low magnetic susceptibility rock, resulting in the weaker fields. Minerals that have

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Structural Analysis of Aeromagnetic Data and Digital Elevation Model for Geothermal Mineralization Potentials of Peninsular Malaysia

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been altered possibly will remain in regions of movement of hydrothermal waters. This modification is the conversion from magnetic minerals (magnetite) to hydrous oxide or earthen minerals with little magnetic susceptibility within the Earh’s crust (Blakely, 1995). Also, the change in mineralogy depresses the magnetic susceptibility in the locality of hydrothermal activity and designates the existence of the geothermal reservoir and pipe structures such as faults or dikes.

Malaysia’s economic growth and development depend on tin, gold, oil, and gas (Hutchison, 1996 and Metcalfe, 2013). Geothermal and other mineral resources have been recorded through the endowed complex geological structures of the Peninsular. As such the region offers an admirable prospect that demands periodic regional study as a key at preparatory stage to hydrocarbon, mineral and geothermal explorations as well as geotechnical investigations. Regional geophysical and geochemical investigations are the necessary reconnaissance surveys that point at fresh mineralized provinces and zones succeeding geological studies. Several studies have been conducted on the Peninsular, which are mostly on determination of temperature and thermodynamic properties (Javino, 2015), physio-chemical properties potential of springs, quality and quantity of the thermal springs as well as assessment of their capacity bases as drinkable water (Enjop 1990; Abdul Rashid 1991; Samsuddin et al., 1997; Zaini et al., 2013). Furthermore, Baioumy et al. (2015) reported the non-volcanic origin and geothermal energy generating potentials of the hot spring. This, therefore, cannot be unconnected with the main fault/fracture zones succeeding the intrusion of granitic rocks through magmatic events and also along the Main Range of the granite batholiths located in the Western belt. The Bentong-Raub Suture Zone (BRSZ)forms the boundary between the Western and Central Belts of thePeninsular, that had undergone strike-slip motion. Gold and other natural resources have been revealed to be associated with the main features along the BRSZ (Hutchison, 1996; Metcalfe, 2013; Fakhuddin et al., 2019). The Eastern boundary of the Central Belt delineated by major N-S trending faults, the Lebir Fault being the largest (Hutchison, 1996; Fakhuddinet al., 2019). However, the geological features which sheltered the natural resources, still not fully being characterized and harnessed, sinceboth geological and geochemical mapingsare only meaningful for characterization if the target has surface expressions. However, cannot probe deep into the crustal structures, especially when for example, a non-exposed fault, concealed by thick accretions of sedimentary rocks, repressed surface relief and of few outcrops, thus lead to poor characterizations of the Peninsular Malaysia for geothermal and mineral explorations. In order to offer some important information to minimize the problem of poor characterization of the Peninsular Malaysia for geothermal and mineral exploration systems associated with the Bentong-Raub suture zone, Lebir fault zone and other significant hidden features in the Peninsular Malaysia, this study work was conducted to reveal the predominant structural and tectonic controls, their relationship from surface to the subsurface, and depths to basement structures. The updated high-resolution Earth Magnetic Anomaly Grid 2 Version 3 (Meyer et al., 2017) was used for interpretation/analyses of the structures within the basement and DEM data for external morphology of the structures.Hence, significant structural details of tectonically formed stratigraphic features are often revealed by potential field data (Grauch, 2001), and DEM data (Kervyn et al., 2006).


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Geological Structures of the Malay Peninsula The Malaysian Peninsular (Fig.1) has received wide documentation and categorization as a three-components north–south longitudinal belts. It extends over an area of about 183, 000 km2 spanning the Isthmus of Kra and Singapore. These belts incorporate the Western, Central and Eastern parts of the Peninsular based on discrete changes in stratigraphy, structure, magmatism, geological evolution and volcanism (Metcalfe, 2013). Furthermore, inside the Western belt (Fig.1), there exists a N-W domain. A major suture zone recognized, called the Bentong-Raub Suture, which extends as a narrow N-S zone through the Malaysian Peninsular. It forms the boundary between the Western and Central Belts of the Malaysian Peninsular. The Bentong-Raub Suture Zone (BRSZ) has recorded remarkable strike-slip motion. Several gold mines and prospects in the Peninsular Malaysia are linked to the main features along the BRSZ

The Eastern boundary of the Central Belt delineated by major N–S faults, the Lebir Fault being the largest. The Western Belt forms part of the Sibumasu Terrane derived from NW Australian Gondwana in the late Early Permian (Metcalfe, 2006). The Central and Eastern Belts were recently regarded as a single tectonic block, the East Malaya Block, formed part of the Indochina-East Malaya Terrane that separated from Gondwana in the Devonian (Metcalfe, 2006). The granitoids are the West Malaya Main Range S-Type group of granitoids that yield Late Triassic to earliest Jurassic U–Pb zircon ages, and an Eastern Malaya group of dominantly I-Type granitoids with a range of ages from early- Middle Permian to early- Late Triassic (Searle et al., 2012).A noteworthy Late Cretaceous thermo-tectonic occurrence influenced the Malaysian Peninsular with key faulting, granitoid intrusion and repositioning of paleomagnetic signatures.

Fig. 1 Geological map of the Malaysian Peninsular showing the Bentong-Raub suture zone, three belts and the spread of hot springs (circle-black). After Tate et al. (2009). Materials and Methods Magnetic Data of the Peninsular Malaysia The magnetic data employed in this study comprised of three different data sets harmonized as the global Earth Magnetic Anomaly Grid 2 Version3 (EMAG2-V3). It includes aeromagnetic and ship borne magnetic measurements and satellite data. The height of the flight for the magnetic grid acquisition was 4 km above the geoid with 3.7 km resolution (Meyer et al., 2017). The


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magnetic data used in this study was extracted from the global databaseusing a script and the data span from longitude 990 - 1050 E and latitude 00 - 70 N latitude, covering the Peninsular Malaysia and its vicinity.

Reduction to Magnetic Equator In order to subdue this bipolarity occurrence, the RTEfield was generated from total magnetic intensity field. The values of magnetization field ranges from –35 to 32 nT. The inclination of -10.67° and a declination of -0.04° are used for the correction. RTE of total magnetic field intensity is a field due to the combination of both deep seated and shallow sources due to regional and local structures. As such high pass and low pass filters were then applied on the RTE field, to separate deep seated structures and shallowstructures in which the shallow structures are depictedinhigh pass filtered RTE (HRTE) field.It is imperative to adopt and register various pivotal and rudimentary processings to the HRTE data, to improve and boost the magnetically anomalous imaging and proper refining interpretations of geologic structures. Such techniques include, Total Horizontal Derivative (THD), Analytic Signal (AS), 3D -Euler Deconvolution (3ED) and Source Parameter Imaging (SPI), via Geosoft Oasis Montaj software (Mohamed & Zaher, 2019; Pamuk, 2019).

Total Horizontal and Vertical Derivatives

The THD of the magnetic field (M) in the x and y directions is given by Eq. (1)

√( ⁄ ) ( ⁄ ) (Millgan and Gunn, 1997) (1) THD is independent of inclination, like Analytic Signal. The distinction between these derivatives is that the former is sharper and generates better-defined maxima centered over the body edges. The edge of having no dependency makes more important in terms of responding to different types of magnetization of a body. Analytic Signal technique Analytic signal method can aid in the determination of depths to magnetic sources. The depths to magnetic sources are estimated from the ratio of the AS of the magnetic data to the vertical derivative of analytic signal (VAS) of the magnetic data.

VAS √( ⁄ ) ( ⁄ ) ( ⁄ ) (2)

The maximum amplitude, D=

(3)

where Mv = first vertical derivative of the magnetic field, and D = depth to the magnetic body, N = structural index, related to the geometry of the magnetic source. For instance, N = 1 for contact, N =2 for dyke, N = 3 for pipe thin dike and N = 4 for sphere (Reid et al.,1990). Euler Deconvolution (ED) technique ED uses potential field profile and gridded data to automatically and rapidly determine the locations of linear geologic structures. It requires no prior information of magnetization source azimuth and resistive to the existence of remanence. At a given value of structural index, positions and depth values ( , , ) of any source are normally determined using Eq. (4):

( )

( )

( ) ( ) (4)

where M = observed magnetic field measurement position (x, y, z) and B = base level value of the magnetic field and, I = structural index value (Reid et al.,1990). It permits a movable


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window over the data, and adopts least-squares inversion to find the range of depth values and plane position of sources of varying structural indices.In this work a window size of 8, 10 grid cells and a depth tolerance of 14% and structural index 0, proved to be the best solutions. It was applied on the HRTE map in order to determine depth values at various locations and trends in the study area. Source Parameter Imaging (SPI) A depth value is estimated at the source boundary from the reciprocal of the local wave number for a given magnetic field using SPI technique and is expressed in Eq. (5)

( )

(5)

where Kmax= peak value of the local wavenumber K over the step source. Digital Elevation Model (DEM) Data Different data grids were made into one composite STRM-DEM mapsand surface lineaments were extracted using ArcGIS software. Superficial mapping of fault zones seems to be hard due to the poor exposures and sparse distribution of rocks by different geologic processes cutting the faults. Consequently, DEM data was used to delineate fault zones and other features, by sudden variations in color or tonal outlines/shapes, gentle topographic slopes and cliffs. Results The RTE map (Fig. 2a) shows magnetic anomalies of low resolution and which do not reflect the geological settings of the study while the HRTE(Fig. 2b) map offers improved clarity, visibility, precision and contrast of shallow magnetic rock units.


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Results The RTE map (Fig. 2a) shows magnetic anomalies of low resolution and which do not reflect the geological settings of the study while the high pass filtered Reduced To the Equator (HRTE)(Fig. 2b) map offers improved clarity, visibility, precision and contrast of shallow magnetic rock units. Fig. 2(a). Reduced to the magnetic equator (RTE) of the total magnetic intensity map. Black boxes represent hot springs. There are three belts separated by Bentong-Raub suture zone (yellow dotted line) and Lebir fault zone (cyan colour line). (b) RTE (High pass) map showing all the three belts, hot springs distribution, the Bentong-Raub Suture zone and Lebir fault (cyan colour). Figure 3a, reveals the hidden anomalies and enhancing all the anomalies with their visible major dominant NW-SE and E-W trends and geologic contacts of different lineaments in the three belts. Also, the Lebir fault zone and minor NE-SW trends have been effectively and thoroughly mapped with new faults (Fig. 3a). While Figure3b, shows depth values within the Peninsula range from approximately 2 to 20 km. But the values are averagely 3 km in the middle of the study area, shallower than the extremes in the northern, eastern, western and southern parts, which may be related to plutonic or granitic intrusions of sedimentary characteristics during uplift of the Peninsular. . Fig. 3(a). THD map revealing the predominant magnetic lineaments in NW-SE and E-W of the Peninsular Malaysia. (b) Depths map obtained from the ratio of Analytic Signal map of magnetic data to that of the first vertical derivative of the Analytic signal using structural index of 1. The results of 3ED (Fig. 4a) show depth values at the middle parts of the study area ranging from 1 to 20 km indicating shallow strucutres. The SPI map (Fig. 4b) shows depth values ranging from approximately 3 to 26 km at the middle parts of the Peninsular Malaysia in relative agreement to the depth values obtained in Figs. 3b&4a.

a b


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Fig. 4(a)Euler Deconvolution Map underlaid by tilt derivative for magnetic depth values to coincide with edge of the magnetic sources. (b) Source Parameter Imaging Map of the study area showing depth variation and hot springs distribution in black box. In Fig. 5, the magnetic anomalies are inferred to be the new mineralized and fault zones revealed from the magnetic data. Faults and contacts delineated may be of economic importance for exploration of geothermal and mineral resources.

Fig. 5. Magnetic derived lineaments map of the study area showing the conspicuous positive magnetic anomalies extracted from the THD map. Physical inspection and description of SRTM DEM displayed on maps reveal structural trends, patterns and spatial distribution of faults zones and geologic structures. The conspicuous granitic intrusions along the Main Range figure out with other pockets of intrusions spread across the entire study area ( Figs. 6a & b) and trend in NW-SE, NNW-SEE, N-S, E-W, & NE-SW directions.

a b


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Fig. 6. Surface lineaments superimposed on the DEM data (a), and surface lineaments derived from DEM data of the study area (b). Discussion Main qualitative observation of the HRTE map (Fig. 2b) allows the discovery and recognition of quite a lot of different types of anomalies of varying properties (for instance shape and magnetic field values). The magnetic field values range from -27 to 27 nT reflecting a variety of geological materials within the study area. The Western Belt corresponds to NW-SE structure that houses the Main Range Granite Batholith of the Peninsula trending from Malacca in the southern part to Thailand in the northern part. This distinguished structure corresponds to the regions of high surface lineaments density with associated orientation. The regions of the lineaments showing the high lineaments density could be considered as regions with favourable mineral occurances. Moreover, the lineaments distributed around the hot springs’ distribution and orientation in the study area can be areas of possible geothermal occurances. The dominant orientations of the DEM-derived structures/lineaments(Figs. 6a &b) are found to be in the NW-SE, N-S and E-W directions. These are in conformity with the dominant directions of magnetic-derived lineaments which can be attributed to different stages of structural deformation through evolution, magnetism and volcanism undergone by the Peninsular Malaysia (Metcalfe, 2013).The obtained low magnetization range in the Western Belt could be attributed to the dual sources of the granitic rocks (Azman, 2001). Also, the low magnetization could be linked to the intrusion of the country rocks such as isoclinal, folded phyllitic lower Paleozoic by the granites of S-type and Upper Paleozoic Formations ( Hutchison, 1996). The map (Fig. 2b) offers improved clarity, visibility, precision and contrast of shallow magnetic rock units. At this juncture, individual anomalies and magnetic field intensity values together with patterns and directions are believed to be the reflections of the rock types ranging from batholiths and plutons of tin-bearing, largely biotite granites of S-type ilmenite series, emplaced into Lower to Middle Palaeozoic low-grade metamorphic in the western belt (greenschist facies) rocks (Cobbing et al., 1992). Also, the low magnetization (Fig. 2b) agreed with the existence of volcano-plutonic arc concealed by thick Triassic volcaniclastic mudstones and turbidites, volcanic rocks related to limestone in the central belt (Metcalfe et al., 1982). The eastern belt houses granitoids of calc-alkaline series of metaluminous I-type and S-type. The thick sedimentary cover overshadowed the high magnetic disposition of the granitic, volcanic and ilmenite rocks, visible at the middle of the study area.


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Figure 3a, reveals all the magnetic anomalies of the dominant orientations and trends to be NW-SE, E-W, N-S and WWN-EES. Furthermore, almost all the hot springs feature in the areas of positive anomalies along the NW-SE direction of the western belt, correspond to the main range granite batholith of the Peninsula. The magnetic anomalies portrayed in the Main Range within the western belt could be the responses of bulk of granitoids that intruded from 251-254 Ma and proposed to be of a magmatic arc setting of a continental crust (Kwan et al.,1992). Magnetic field responses along the Bentong-Raub Suture Zone poorly depict its geological trend with cross-cutting smaller and short anomalies (Fig. 3a). This weak magnetization could be attributed to the Bentong-Raub Suture Zone being overlie by a dense system of conglomerates, mudstones and sandstones place. However, the suture is reported to have surface expression about 20 km widespread neighboring the eastern boundary of the Main Range granitoids but not clearly shown by magnetic data due to series of faulting, folding and weathering proceses. The Lebir fault zone and minor NE-SW trends have been mapped (Fig. 3a). The results (Fig. 3b) show depth values within the Peninsular ranged from ~ 2 to 20 km, while those overlaid on the tilt derivative map (Fig. 4a) span from 1 to 20 km. These (Fig. 3b & 4a) show a good depths correlation as compared to SPI map (Fig. 4b) with depth values ranging from 3 to 26 km. AS and ED are good potential field depth estimation methods. But in the middle portion of the study area (Figs. 3b, 4a & 4b), the values are shallower, averagely 5km, which may be related to plutonic or granitic intrusions of sedimentary characteristics during uplift of the Peninsular. Furthermore, the existence of many hot springs at the locations of varying magnetic depth values (Figs. 3b, 4a & 4b) along the Western belt testify to the fact that the granites are of mostly S- type, consequence of melting from sedimentary or metasedimentary (pellitic) rocks (Hutchison, 1996) and of non-volcanic source (Baioumy et al., 2015). In the Fig. 5, magnetic anomalies with sharp edges, trends and patterns have been revealed as being the faults, fractures and contacts inferred to be harbouring both fluid and mineral migration along the Bentong-Raub suture and Lebir fault zones. Therefore, the melting origin, intrusion of the granitic rocks as well as the varying depth values associated with regions hosting most of the hot springs, implied the significance of geologic structural controls in revealing geothermal energy potentials of the hot springs.Besides, the mineral veins that occurred during the metamorphism stages of the Peninsular were also revealed. It could add to geothermal energy resource and tourism opportunities in the country. Conclusion Main qualitative and quantitative characterizations of the High pass filtered Residual Magnetic Field (HRMF) map allows the discovery and recognition of quite a lot of different types of anomalies of varying properties. The magnetic anomalies processing from the generated maps reveal lineaments maps showing that the dormant orientations, patterns and trends are the NW-SE corresponding to the Main Range granite of Western Belt of Peninsular Malaysia, the NWW-SEE and N-S (relatively parallel to Bentong-Raub Suture and Lebir Fault Zones) and E-W directions. Therefore, strong correlation was obtained with the regional structural trends of the Peninsular especially along


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the NW-SE striking faults in the Western Belt.The obtained depths to magnetic sources of the whole Peninsular spans from 1.0 to 20 km with 5.0 km average at middle of the area. The sedimentary rock cover shrinked towards the central regions of all the three belts. AS and ED methods have strong depth values correlation pinpointing high and lowdepth regions of the study not previously found.The structural map shows the Bentong-Raubsutue and Lebir fault Zones are poorly exposed magnetically due to overlay of mudstones and sandstones. The predominant featuring of magnetic faults in the NW-SE direction in alignment with hot springs and crossed by minor normal faults inferred to be harbouring and serving as conduits for geothermal and mineral fluids transportation and migration in the western belt, conform well with bulk of granites intrusions of S-type characteristics from 251-254 Ma geochronological age. Also, could be viewed as the granitoids that have narrow thermalaureoles and that are normally not deformed, except cataclasis related to fault. Also some minor faults can suggest concealed geothermal and mineral zones. Geophysical anomalies analyses correlate well with the geological framework of the area which give insight on the vast geothermal and mineral potential zones, and also for tourism industrial development.

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