Journal of Asian Earth Sciences 127 (2016) 32–46

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Journal of Asian Earth Sciences

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Full Length Article

Origin and tectonic implications of the �200 Ma, collision-related Jeraipluton of the Western Granite Belt, Peninsular Malaysia

http://dx.doi.org/10.1016/j.jseaes.2016.06.0041367-9120/� 2016 Elsevier Ltd. All rights reserved.

⇑ Corresponding author.E-mail address: azmangeo@um.edu.my (A.A. Ghani).

Azmiah Jamil a, Azman A. Ghani a,⇑, Khin Zawb, Syamir Osman c, Long Xiang Quek a

aDepartment of Geology, University of Malaya, Kuala Lumpur 50603, MalaysiabCODES ARC Centre of Excellence in Ore Deposits, University of Tasmania, Private Bag 126, Hobart, Tasmania 7001, AustraliacPREX, Level 16, Tower 1, KLCC, Petronas Twin Tower, Kuala Lumpur, Malaysia

a r t i c l e i n f o

Article history:Received 23 June 2015Received in revised form 31 May 2016Accepted 8 June 2016Available online 9 June 2016

Keywords:Western Belt granitePeninsular MalaysiaPegmatiteU–Pb datingS-type granite

a b s t r a c t

Triassic granitoids (�200–225 Ma) are widespread in the Western Belt of Peninsular Malaysia. The MainRange granite is the biggest batholith in the Western Belt composed of peraluminous to metaluminousgranite and granodiorite and displays typical ilmenite-series characteristics. Jerai granitic pluton occursat the northwestern part of the Main Range granite batholith. The Jerai granite can be divided into threefacies: (i) biotite-muscovite granite; (ii) tourmaline granite; and (iii) pegmatite and aplopegmatite.Biotite-muscovite granite accounts for 90% of the Jerai pluton, and the rest is tourmaline granite.Geochemical data reveal that pegmatite and tourmaline granite are more differentiated than biotite-muscovite granite. Both pegmatite and tourmaline granite have a higher SiO2 content (70.95–83.94% ver-sus 69.45–73.35%) and a more pronounced peraluminous character. The U–Pb zircon geochronology ofthe Jerai granite gave an age ranging from 204 ± 4.3 Ma, 205 ± 4 Ma and 205 ± 2 Ma for pegmatitebiotite-muscovite granite and tourmaline granite, respectively. The biotite-muscovite Jerai granites aresimilar to S-type Main Range granite, but the tourmaline granite has a signature of late-stage hydrother-mal fluid interaction such as tourmaline quartz pods, the accumulation of large pegmatitic K-feldspar,pronounced peraluminous character, higher SiO2 content. Age evidence of these two granitic facies sug-gest that they are from the same magma.

� 2016 Elsevier Ltd. All rights reserved.

1. Introduction

The I– and S–type granite classification was initially developedin southeastern Australia by Chappell and White (1974) wherethey emphasised the importance of source rock composition andrefractory residue during production of felsic magmas. In the Lach-lan Fold Belt of SE Australia, a clear spatial distribution existsbetween ‘I’ and S–type granites. The scheme considers I–type gran-ites as the melt products of meta-igneous source rocks, whereas ‘S’type granites result from melting of meta-sedimentary sourcematerial. In both cases, the source is considered to have residedwithin continental crust. Crustal-derived S-type granites, typifiedby the Himalayan leucogranites tend to be peraluminous (contain-ing garnet, muscovite, biotite, alumino-silcate minerals and tour-maline), have meta-sedimentary xenoliths, associated withregional high-grade metamorphic-migmatite belts, and in manycases are associated with Sn-W mineralization. In manyMesozoic-Cenozoic continental margins such as the Andes, S–type

batholiths (e.g. Cordillera Blanca batholith) occur on the continen-tal side, or inboard to, I–type granite belts (e.g. Coastal batholith;Pitcher, 1983). The ‘I-S’ duality is believed to reflect the progressiveremobilization of continental crust in granitoid genesis with timeas the locus of magmatism migrates landwards and away fromthe subduction system.

The association of granite pegmatite and mineralized granites isnot an uncommon feature (e.g., London, 1992, 2005). Pegmatiteusually occurs as a late-residual fraction of silicic melt that issqueezed out of a crystal mush to form a late-stage dyke andmagma pods that intrude into already crystallized granitic plutons(Jahns, 1955, 1982; London, 2005). These evolved late residual sili-cic melt deviate in texture, mineral composition and geochemicalcharacteristics from the more primitive granitic host.

The present study focuses on the geochemical and field rela-tionships of the different granitic facies of the Jerai granite(Ghani et al., 2013) in the northwest of Peninsular Malaysia. Wepresent a new U–Pb zircon geochronology of the Jerai graniteand discuss the tectonic scenario of the granite. The granite wasemplaced into the Jerai formation, which is considered equivalentto the Machinchang formation (Cambrian Age) on Langkawi Island

A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46 33

(Bradford, 1972). The Jerai granite occurs as a pluton of less than100 km2 and represents one of numerous granite plutons that ‘off-shoot’ to the west of the Main Range granite. The pluton forms partof the Jerai Mountain, which is the highest peak in the northwest ofPeninsular Malaysia. The Jerai pluton ranges in composition frombiotite-muscovite syenogranite to muscovite tourmaline-richleucogranite to highly evolved pegmatites. Late-stage magmaticstructures, such as tourmaline quartz pods, the accumulation oflarge pegmatitic K-feldspar, and the association with the aplopeg-matite phase, are common features in the pluton. In the Jerai gran-ite, cassiterites that occur together with columbite-tantalites arefound associated with pegmatite and other late-phase varieties ofgranites, which normally contain coarse muscovite, tourmaline,garnet and other ore minerals (Wan Hassan, 1983; Bradford, 1972).

2. Geological setting

Peninsular Malaysia forms an integral part of the SoutheastAsian continental core of Sundaland and comprises two tectonicterranes–Sibumasu in the west and the Sukhothai Arc (East Malayablock) in the east – that were assembled in the Late Triassic(Hutchison, 1973, 1975; Cobbing et al., 1986; Metcalfe, 1988,2000, 2011a, 2011b, 2013; Sone and Metcalfe, 2008; Morley,2012). These two crustal blocks are separated by the Bentong–Raub Suture, which preserves the remnants of the Devonian–Permian Paleo-Tethys ocean basin (Metcalfe, 2000, 2013).Paleobiogeographic and tectonostratigraphic analyses have shownthat both Sibumasu and East Malaya were once part of theGondwana supercontinent, but separated at different times inthe Phanerozoic (Metcalfe, 1988, 2000, 2013; Burrett et al., 1990).The two blocks collided in the late Triassic, giving rise to the Easternand Western Belt granites and triggering Permo-Triassic volcanismin Peninsular Malaysia. The granitoids of Peninsula Malaysia belongto the Eastern province and the Main Range province of the

Fig. 1. (a) Subdivision of granitoids from the Southeast Asia Tin Belt (modified from Cobblocated at the northwest of the Peninsular.

Southeast Asian Tin Belt (Bignell and Snelling, 1977; Hutchisonand Taylor, 1978; Cobbing et al., 1986; Krahenbuhl, 1991;Schwartz et al., 1995; Metcalfe, 2000; Hutchison and Tan, 2009)(Fig. 1a). It is widely accepted that these granitic rocks (Easternand Western Belt granites) record the closure of the Paleo-Tethysocean as they show distinct age, petrological and geochemicalcharacteristics (Hutchison, 1975; Metcalfe, 1988, 2000; Cobbinget al., 1986; Hutchison and Tan, 2009; Ghani et al., 2013).

The Main Range granite is the largest granite batholith in thewestern belt of Peninsular Malaysia, extending from Malacca inthe south to the Thai border in the north (Fig. 1b). It has a restrictedcompositional range, from granite to granodiorite and peralumi-nous to metaluminous biotite granite, and displays typicalilmenite-series characteristics (Ghani, 2009; Ghani et al., 2013).New U–Pb SIMS zircon ages indicate that the tin-bearing granitewas emplaced in the Triassic approximately 198–227 Ma (Searleet al., 2012; Cottam et al., 2013; Ng et al., 2015b). Several smallerplutons and granitic complexes occur to the west of the MainRange granite (e.g., Penang, Langkawi and Jerai granitic com-plexes). The Main Range granite is also exposed off the west coastof Peninsular Malaysia in the form of islands, including Pangkor,Sembilan and Jarak. The granite of Jarak Island, which is locatedapproximately 34 km off the west coast of Peninsular Malaysia,shares the same texture as the Main Range granite (Ghani, 2008).

3. The Jerai pluton

The Jerai pluton, which is part of the Main Range Graniteexposed in NW Peninsular Malaysia, is surrounded by metasedi-ments of the Jerai Formation (Fig. 2). The Jerai granite displays analmost circular intrusive geometry and features a weaklyelliptical steep-sided pluton. Bradford (1972) reported a fewoccurrences of hornblende in the Jerai granite, which commonlycontains the accessorymineral cassiterite. However, no hornblende

ing et al., 1992), (b) granites from Peninsular Malaysia. The study area – Jerai pluton

Fig. 2. Simplified geological map of the Jerai pluton and main granite location describe in the text. The granite is mainly surrounded by Jerai sedimentary formation.

34 A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46

granite was found in this study. The difference between the Jeraigranite and the other Main Range granite is the presence of peg-matites (associated with aplites), which cut the granite and sur-rounding metasediments (Jerai and Sungai Petani formations;Bradford, 1972). The pegmatite composition varies from almostpure quartz and feldspar to books of mica, to types rich in tourma-line and almandine garnet. Xenolith, metasedimentary raft and roofpendants of surrounding sedimentary rocks are also present in thegranite, notably in Tanjong Jaga and near Sungai Bujang (Bradford,1972). In Tanjong Jaga, the largest metasedimentary raft (quartziteand garnet mica schist) – 50 m long and up to 20 m wide – wasrecorded in fine-grained leucogranite (Bradford, 1972) (Fig. 3). Sur-micaceous enclaves are also common in the main granite body.

The Jerai pluton is dominated by coarse-grained primary-textured biotite muscovite granite. Fine-grained tourmaline andgarnet granites form pods or occur as marginal facies in the maingranite. In this study, the Jerai granite is divided into three faciesbased on mineralogy and texture: (i) biotite-muscovite granite,(ii) tourmaline granite and (iii) late aplopegmatite complex, whichintruded both (i) and (ii).

3.1. Biotite-muscovite granite

This granite is coarse- to medium-grained and primary-textured and can be slightly porphyritic. The average mafic mineralcontent is approximately 15%. Locally, biotite displays preferredorientation parallel to the gross course of intrusive contacts,resembling a flow structure. Xenoliths and biotite-rich enclavesare common (Fig. 4a and b). The xenoliths are rectangular to sub-rounded, and preserve sedimentary bedding and well-developedmetamorphic fabrics. In contrast, mafic microgranular enclavesare rounded, show igneous textures and have mineral assemblagestypical of granites (Fig. 4a).

3.2. Tourmaline granite

The tourmaline granite is a fine to medium-grained granite withan abundance of tourmaline and garnet. The granite occurs as dark

layers of fine-grained granite within the main biotite-muscovitegranite (Fig. 4c). This fine-grained granite forms a coastal outcrop250 m long and approximately 50 m wide at the western marginof the Jerai pluton and sometimes occurs as pods (up to 1 m across)in the main granite. The area, also known as Tanjong Jaga, is essen-tially composed of fine-grained tourmaline granite, with manyblocks and rafts of country rocks, and is intruded by pegmatite(Fig. 3). Xenoliths present in the rock are mainly composed ofquartz arenite, micaceous quartzite, biotite muscovite schist andgarnet tourmaline schist. These blocks probably represent thestoped blocks of the Jerai Formation rocks that fell into the Jeraimagma chamber during emplacement.

Essential minerals include quartz, K-feldspar, plagioclase, tour-maline and reddish garnet. Tourmaline occurs as euhedral, stubbycolumnar to acicular crystals. Garnet stands out as euhedral dodec-ahedral brown crystals sometimes forming a layer structure in thegranite (Fig. 4d). Quartz occurs as aggregates and individual grains.K-feldspars are mainly subhedral, and white to cream in colour.

3.3. Pegmatite

The Jerai pegmatite intrusion transitions from a homogeneousinclusion-poor body to sub-parallel and sub-vertical dykes, whichrange from several centimetres to several metres in thickness.The pegmatites can be divided in two types based on the fieldoccurrence: (i) layered or tabular pegmatite aplite facies, and(ii) lenticular to pod-shaped pegmatite (Fig. 5). The layered totabular pegmatite (Fig. 5a) consists of a coarse-grained quartz,plagioclase, muscovite and randomly oriented megacrysts ofmicrocline-perthite intergrown with the graphic granite. BlockyK-feldspar and quartz associated with the tourmaline and garnetoccur sporadically in the pegmatite. The maximum size of the peg-matite crystal is 5 m. The main trend of the tabular pegmatite isNE–SW (Fig. 6a), in contrast to the lenticular to pod-shaped peg-matite, which mainly has a NNW–SSE trend (Fig. 6b). The lenticularto pod-shaped pegmatites is smaller in size compared to thetabular pegmatite, ranging 0.2–0.2 m in width and 0.01–0.7 m inlength (Fig. 5b). The pods sometimes form a continuous chain of

Fig. 3. Field occurrence of the Jerai granite. (a) Biotite rich enclave in the biotite muscovite granite, (b) metasediments xenolith of the host rocks (Jerai formation ?) in thebiotite muscovite granite, (c) contact relationship in the biotite muscovite granite (coarse grained and fine grained types) and (d) garnet crystal (1–2 mm) in the Tourmalinegranite (diagram taken from Bradford, 1972).

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two to four other pods, which are connected by fine-grainedtourmaline-rich veins. The pods consist of a cluster of black,millimetre-scale, schorl-type tourmaline crystals, surrounded bya white halo or bleached zone. Mineral zoning towards the centreof a tourmaline pod indicates a decrease in plagioclase and mus-covite and an increase in tourmaline and quartz. Tourmaline podsare scattered through the granite rock, especially near the peg-matite, aplite veins and dykes.

Aplopegmatite consists of aplite or layered aplite and is mostlypaired or alternated with pegmatite layers. The aplopegmatitesometimes show sharp contact with biotite muscovite granite(Fig. 5c). Albite and quartz are the predominant constituents(Fig. 5d) of aplite, with less abundant K-feldspar and tourmalinegrains or needles. Muscovite and garnet form only minor, sparselydistributed phases. The detailed structure of the aplopegmatitecomplex is shown in Fig. 7.

4. Petrography

One of the special features of the tin-bearing granite ofSoutheast Asia is the presence of the two phase variant granite

or secondary textured granite (Cobbing et al., 1986, 1992). Thegranite is characterized by the presence of heterogeneous por-phyritic microgranite or porphyritic granite, in many cases, associ-ated with Sn mineralization. The textures are the result ofdisrupted crystallization of the granitic magma during the laterstage of crystallization (Cobbing et al., 1986, 1992). The particulartextures occur in the late phase granitic bodies and are moreevolved than the earlier primary textured host. This resulted fromthe infiltration of volatile-rich residual granite melt into a whollyor partially consolidated granitic host. In the study area, thebiotite-muscovite granite is composed of primary textured granite,whereas the tourmaline granite is mainly of secondary texture. TheJerai granite consists both of primary biotite-muscovite granite andsecondary textured granite (tourmaline granite).

4.1. Biotite-muscovite granite

Biotite-muscovite granite is predominantly of a medium- tocoarse-grained biotite-muscovite-bearing type, typically compris-ing K-feldspar, plagioclase, quartz, biotite, muscovite and zircon.K-feldspars are anhedral to subhedral and are mainly composed

Fig. 4. Detail sketch map of the Tanjung Jaga area (western part of the Jerai pluton). This area dominated by fine grained tourmaline granite with variety of metasedimentaryblocks and xenoliths. The diagram is taken from Bradford (1972).

Fig. 5. Pegmatite dyke in the Jerai granite. (a) Tabular type pegmatite in Batu Pahat river, (b) lenticular to Pod shaped pegmatite in Batu Pahat river, (c) contact betweenbiotite muscovite granite and pegmatite (scale as in Fig. 5b), and (d) Sawn slab of pegmatite sample showing graphic texture.

36 A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46

of microperthitic orthoclase and microcline (Fig. 8a). The granite isprimary textured granite characterized by a homogeneous textureand an order of crystallization that suggests its precipitation frommelt. Plagioclase is subhedral with typical albite and Carlsbad-albite twinning. Quartz mostly occurs as anhedral interstitialgrains. The biotite commonly occurs as euhedral to subhedral

flakes, with strong pleochroism, and a light brown to reddishbrown colour. Some of the biotite has been partly replaced by chlo-rite and commonly includes zircon. Two types of muscovite occurin the granites. The first type is small or tiny crystals present inheavily sericitized parts of plagioclase. Sometimes the tiny flakesare well oriented at the centre of plagioclase suggesting that the

Fig. 6. Rose diagram showing the general trend between (a) tabular and (b) lenticular to pod shape pegmatite in the study area.

Fig. 7. Section through a subhorizontal layered aplite-pegmatite dike, Kemelongquarry (see Fig. 2 for location). Massive aplitic (MA), skeletal microcline-quartzintergrowths (GMc), Layered aplite (LA), Graphic albite-quartz intergrowths (GAb)and graphic microcline (GMc).

A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46 37

mineral developed along cracks. These textural relationshipssuggest that this muscovite is not primary but altered fromplagioclase. The second type occurs as large subhedral to anhedralcrystals adjoining all other rock forming minerals (Fig. 8a). Thistype accounts for less than 5% of the biotite-muscovite granite.Sharp contacts with other minerals and non-replacive boundariessuggest the muscovite is primary in origin (Miller et al., 1981).

4.2. Tourmaline granite

Tourmaline granite is very felsic and contains relatively abun-dant tourmaline and garnet. It is composed of quartz, K-feldspar,plagioclase, tourmaline and garnet. Muscovite and iron oxide arecommon accessory minerals. The rocks are generally composedof secondary textured granite and in many cases contain heteroge-neous porphyritic microgranite to highly evolved aplite. K-feldsparis anhedral orthoclase or, in rare cases, microcline. Plagioclaseoccurs mainly as subhedral crystals with lamella twinning. Perva-sive fine-grained muscovite alteration in the central portions ofplagioclase is common. Tourmaline is strongly pleochroic, lightbrown to brown in colour, and sometimes occurs as skeletalcrystals (Fig. 8b). Garnet is pale brownish yellow, subhedral to

Fig. 8. Microscopic texture of the Jerai granite. (a) General texture of the biotite muscovite granite, (b) skeletal tourmaline in the fine grained tourmaline granite,(c) tourmaline and garnet in highly evolved pegmatite, and (d) pegmatite, tourmaline and biotite in the pegmatite. Scale for all figure: — 0.2 mm.

38 A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46

euhedral, and occurs in the form of slightly rounded grains con-taining irregular cracks. It also occurs interstitially or as inclusionsin quartz and occasionally in feldspar. Tiny minerals filling thecracks in garnet are mica and apatite needles. The cracks also con-tain plagioclase, K-feldspar, quartz and secondary muscovite, i.e.,identical in composition to the matrix minerals in the granite. Gar-net crystals show no evidence of inclusions, with every mineralcontained within the garnet being connected to the matrix bycracks in the crystals. Secondary muscovite occurs as an alterationproduct of plagioclase and K-feldspar. Iron oxide is observed inbetween some mineral grains.

4.3. Pegmatite

The simple pegmatites are usually composed of the minerals ofgranitoid rocks, namely, quartz and feldspars, with or withoutmuscovite, biotite and a few other accessory minerals (Fig. 8c).Complex pegmatite may contain tourmaline and garnet (Fig. 8d).K-feldspar is more abundant than plagioclase in the pegmatiticgranitic facies. The perthitic intergrowths in K-feldspar are not welldeveloped in the pegmatite. Quartz usually occurs as polycrys-talline aggregates bounded by feldspar and/or micas. Plagioclaseis rare, occurring either as individual crystals or as patches insidethe K-feldspar crystals. Tourmaline usually occurs as an individualcrystal. Concentric zoning is observed in prismatic tourmalinegrains. Sometimes it shows optical zoning with small bluish coresand wide brownish green rims with alternating darker and lightercoloured zones. Brownish, subhedral to euhedral garnet crystals,with diameters of approximately 1–1.5 mm are common in peg-matite. Muscovite commonly occurs as ‘books’ inside the differentzones of the pegmatite. Muscovite also occurs in some small greis-enized bodies as white flakes, usually less than 1 mm in length.

5. Geochemistry

5.1. Methods

Twenty-five rock samples from Gunung Jerai (10 samples frombiotite-muscovite granite, 10 samples from tourmaline granite and5 samples from pegmatite) were analysed for major and trace ele-ments. The list of data samples is given in Table 1. Each sample wascrushed in the Geology Department of the University of Malaya, inpreparation for whole-rock chemical analyses at the GeoAnalyticalLaboratory of Washington State University (USA). Major oxide ele-ments and trace elements were analysed at the GeoAnalytical Lab-oratory by X-ray fluorescence (XRF), using standard procedures.The accuracy of the major and trace element analyses was checkedby routine analysis of the following USGS standard samples (PCC-1,BCR-1, BIR-1, DNC-1, W-2, AGV-1, GSP-1, G-2 and STM-1), usingvalues recommended by Govindaraju (1994). Precision was typi-cally ±2–5% for both major and trace elements. From the numericaldata, the Geochemical Data Toolkit (GCDKit) program (Janouseket al., 2006) was used to perform the calculations and constructthe normative geochemical graphs. Harker plot diagrams andseveral other classification and geotectonic discriminationdiagrams are further described in the following sections.

5.2. Results

The major and trace element content of all the analysed sam-ples is presented in Table 1. The range of SiO2 for each of thebiotite-muscovite granite, tourmaline granite and pegmatite sam-ples are 69.96–73.96%, 71.16–80.80% and 74.35–83.94%, respec-tively. Selected Harker variation diagrams for selected major andtrace elements are given in Fig. 9. Specifically within the Jerai

Table 1Major and trace elements of composition of the Jerai granite.

Sample Biotite-muscovite granite

JRIQ-B1 JRIQ-B2 JRIQ-B3 JRIQ-B4 JRIQ-B5 JRIQ-B6 PAHT-B7 PAHT-B8 TUPH-B9 TUPH-B10

Major elementSiO2 (wt.%) 72.93 72.81 72.90 71.31 73.02 73.96 69.96 72.48 71.57 71.80TiO2 0.24 0.23 0.24 0.28 0.20 0.22 0.42 0.22 0.02 0.24Al2O3 14.02 14.53 13.99 15.00 14.10 14.55 14.52 15.56 14.79 14.80FeO⁄ 1.59 1.56 1.66 1.79 1.55 1.71 2.92 1.59 0.32 1.84MnO 0.03 0.03 0.04 0.03 0.04 0.03 0.05 0.04 0.01 0.02MgO 0.42 0.43 0.46 0.54 0.41 0.05 0.81 0.05 0.04 0.04CaO 0.92 0.75 0.88 0.75 0.79 0.80 1.13 0.94 0.12 0.97Na2O 2.76 2.85 3.05 2.72 2.85 3.14 2.94 2.83 2.23 4.25K2O 5.38 5.62 5.13 5.86 5.50 4.85 4.93 5.16 9.02 5.11P2O5 0.24 0.19 0.21 0.21 0.22 0.16 0.28 0.16 0.20 0.17LOI 0.80 0.52 0.68 0.81 0.91 0.25 1.27 0.54 0.98 0.35Total 99.32 99.52 99.24 99.37 99.59 99.72 99.22 99.57 99.30 99.56

Trace elementNi (ppm) 5 8 8 9 7 8 13 14 3 4Cr 149 126 99 139 107 180 122 185 83 175Sc 3 2 3 4 4 2 5 6 1 1V 16 15 18 19 13 3 34 33 3 3Ba 292 298 304 361 281 35 252 252 46 43Rb 417 452 450 466 391 1049 462 908 667 937Sr 43 45 44 48 40 94 38 125 13 108Zr 127 124 123 137 113 188 149 169 8 214Y 23 23 22 26 22 3 26 27 4 6Nb 21 18 21 19 17 5 28 27 1 1Ga 20 20 19 24 20 17 26 25 14 14Cu 6 14 5 7 4 60 197 80 2 74Zn 52 66 58 63 55 113 93 121 13 118Pb 42 48 44 55 47 45 35 71 49 46La 34 40 34 43 28 3 36 36 0 4Ce 79 76 68 82 65 2 84 82 2 1Th 31 31 30 35 27 2 30 31 1 1Nd 34 33 34 29 28 2 35 37 2 2U 8 24 11 9 11 3 11 14 13 12

Sample Tourmaline granite

JAGA-T1 JAGA-T2 JAGA-T3 JAGA-T4 JAGA-T5 JAGA-T6 JAGA-T7 JAGA-T8 JAGA-T9 JAGA-T10

Major elementsSiO2 (wt.%) 71.94 73.41 71.16 72.04 80.80 72.69 73.93 72.31 72.47 73.46TiO2 0.01 0.04 0.02 0.04 0.05 0.04 0.02 0.02 0.01 0.01Al2O3 15.67 15.50 15.22 15.55 10.74 16.12 14.47 15.41 15.72 15.85FeO⁄ 1.31 0.75 0.74 0.67 1.15 0.92 1.89 1.13 0.95 1.65MnO 0.57 0.04 0.13 0.01 0.10 0.08 0.56 0.21 0.19 0.42MgO 0.02 0.28 0.08 0.48 0.16 0.15 0.06 0.06 0.33 0.32CaO 0.16 0.42 0.30 0.29 0.26 0.32 0.37 0.22 0.24 0.23Na2O 6,06 5.16 2.07 4.12 4.26 5.37 5.77 4.60 6.78 4.08K2O 0,73 1.17 9.01 3.14 1.06 1.50 1.82 0.36 0.84 3.35P2O5 0.43 0.41 0.39 0.44 0.32 0.39 0.43 1.37 0.49 0.32LOI 2.13 2.14 0.46 3.15 0.96 1.89 0.19 3.96 1.63 0.28Total 99.02 99.33 99.59 99.93 99.85 99.48 99.52 99.65 93.6 99.97

Trace elementsNi (ppm) 3 7 6 8 6 9 4 4 4 3Cr 89 155 87 139 158 178 102 246 92 227Sc 4 3 1 4 2 5 5 3 3 2V 2 3 2 3 5 3 3 3 2 2Ba 11 2 207 4 13 1 8 14 15 13Rb 100 88 674 281 117 126 210 560 105 847Sr 471 40 32 144 48 4 6 264 663 325Zr 32 25 27 23 35 22 24 95 18 96Y 4 7 7 3 2 6 3 4 4 4Nb 95 11 5 15 45 5 114 112 21 19Ga 24 23 20 22 17 23 21 21 22 22Cu 2 3 3 2 3 2 2 70 2 58Zn 7 23 51 23 63 25 62 103 28 116Pb 7 10 45 14 6 13 5 38 8 21La 0 0 7 2 2 �1 2 2 0 3Ce 2 6 5 7 4 2 0 0 0 0Th 0 4 2 3 2 5 0 1 0 1Nd 1 2 4 2 1 1 0 0 0 1U 7 5 4 6 5 3 9 7 11 10

A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46 39

Fig. 9. Selected major and trace elements Harker diagrams of different units of the Jerai granite.

Sample Pegmatite

JRIQ-P1 JRIQ-P2 JRIQ-P3 JRIQ-P4 JRIQ-P5

Major elementsSiO2 (wt.%) 83.94 75.23 74.35 74.73 75.20TiO2 0.03 0.05 0.07 0.09 0.06Al2O3 9.44 14.42 15.20 15.27 13.46FeO⁄ 0.52 0.77 0.62 0.36 1.02MnO 0.01 0.02 0.02 0.01 0.02MgO 0.12 0.18 0.11 0.06 0.23CaO 0.79 0.96 1.18 1.34 0.67Na2O 3.45 4.41 4.98 6.22 3.62K2O 0.39 1.86 2.12 0.84 2.37P2O5 0.072 0.10 0.10 0.13 0.10LOI 1.12 1.52 0.35 0.48 3.12Total 99.88 99.51 99.10 99.46 99.88

Trace elementsNi (ppm) 6 5 5 6 0Cr 126 139 154 144 125Sc 1 3 5 2 4V 2 1 3 3 3Ba 4 16 18 5 24Rb 37 163 205 90 196Sr 19 14 21 25 11Zr 7 2 4 0 6Y 2 7 7 4 8Nb 2,3 12,6 19,9 8,3 10,0Ga 13 24 26 21 22Cu 2 1 3 2 3Zn 28 36 21 8 55Pb 11 21 23 19 20La 1 3 2 1 4Ce 5 1 3 3 9Th 2 7 10 4 3Nd 2 2 3 2 2U 8 5 23 4 9

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pluton, the tourmaline granite and the biotite-muscovite granitehave a higher TiO2, FeO, MgO, CaO and K2O content and a lowerAl2O3, MnO, Na2O and P2O5 content. In contrast to both of the

granites, the pegmatite has a higher CaO content and lower TiO2,FeO, MnO, MgO, K2O and P2O5 content. Both granites andpegmatite, however, overlap in terms of the MgO, Na2O and

Fig. 11. Na2O + K2O vs. SiO2 diagrams of the Jerai granite. Symbols as in Fig. 9.

A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46 41

Al2O3 content. For the trace elements, the granites and pegmatiteoverlap in terms of Ni, Cr, Sc, Nb, Ga, Cu and U; the tourmalinegranite and pegmatite overlap in terms of Ba, Y, La, Ce, Zn, Pb,Th, and Nd; and the pegmatite has a lower Rb, Sr and Zn content.The biotite-muscovite granite exclusively has a higher Ba, Zr, Y,La, Ce, Zn, Pb, Th and Nd content, and Sr is exclusively higher inthe tourmaline granite.

All of the analysed samples are peraluminous and plot in theS-type field of Chappell and White (1991). This is evident fromthe A/CNK versus A/NK and ACNK versus SiO2 plots (Shand,1943) (Fig. 10). The ACNK value of the samples ranges between1.08 and 1.42. The total alkali content (Na2O + K2O) for the tourma-line granite and pegmatite is low, ranging from 4.96% to 7.62% and3.84% to 7.10%, respectively. The biotite-muscovite granite has ahigher alkali content, ranging from 7.87% to 11.26% (Fig. 11). Thebiotite-muscovite granite samples plot in the high-K calc-alkalinefield. In the K2O versus Na2O diagram (Fig. 12), 9 out of 10biotite-muscovite granite samples plot in the S-type field.

Granites are subdivided according to their intrusive settingsinto four main groups: ocean ridge granites (ORG), volcanic arcgranites (VAG), within-plate granites (WPG) and syn-collisiongranites (COLG) (Pearce et al., 1984). On the Rb versus Nb + Ydiagram, the biotite-muscovite granite samples plot in thesyn-collision granite consistent with other Main Range batholithgranites of Peninsular Malaysia (Ghani, 2009; Cobbing et al.,1992; Ng et al., 2015a, 2015b) (Fig. 13a). On the Nb + Y diagram,all samples plot in the syn-collision field (Fig. 13b). The ambigui-ties of the tourmaline granite and pegmatite samples may resultfrom the late-stage fluid interaction.

Fig. 12. K2O vs Na2O- I-S discrimination diagram of the Jerai rocks. Note thatpegmatite and tourmaline granite samples plot in the S-type field. Symbols as in

6. Geochronology

6.1. Methods

The zircon was analysed at CODES, University of Tasmania,Hobart, Tasmania. Three samples were selected: biotite-

Fig. 10. (a) A/NK vs A/CNK and (b) A/CNK vs. SiO2 diagrams of the Jerai granite.Symbols as in Fig. 9.

Fig. 9.

muscovite granite (Sample BG4Q), tourmaline granite (SampleTG3J) and pegmatite (Sample PG2Q). Crushed rocks were sievedin a Cr-steel ring mill to a grain size of <400 lm. Magnetic andnon-magnetic heavy minerals were then separated using a goldpan and a Fe–B–Nd hand magnet. The zircon samples were hand-picked from the heavy mineral concentrate under a microscopein cross-polarized transmitted light and were placed on double-sided sticky tape, mounted in epoxy glue and polished. After exam-ining their internal textures using cathodoluminescence imaging,the zircon samples were U–Pb analysed on an Agilent 7500 csquadrupole ICPMS, with a 193 nm Excimer, using the ResoneticsM50 ablation cell, at CODES at the University of Tasmania(Meffre et al., 2007, 2008). The down-hole fractionation, instru-ment drift and mass bias correction factors for the Pb/U ratios ofzircons were determined based on the primary 91500 standard(Wiedenbeck et al., 1995) and validated using the Temora (Blacket al., 2003), GJ1 (Jackson et al., 2004) and Mud Tank (Black andGulson, 1978) zircon standards. The zircon was sampled for 32 or13 lm spots using the laser at 5 Hz and a density of approximately2 J/cm2. The flow rate of the He carrier gas was 0.6 L/min, carryingparticles ablated by the laser out of the chamber to be mixed withAr gas and then to the plasma torch. The isotopes measured in thezircon were 56Fe, 90Zr, 181Hf, 202Hg, 204Pb, 206Pb, 207Pb, 208Pb, 232Thand 238U, with each element measured every 0.16 s, with a longercounting time used for the Pb isotopes compared to the other ele-ments. The propagation of uncertainties was based on the method

Fig. 13. (a) Nb + Y vs. Rb (b) Y vs. Nb diagrams of the Jerai granite (Pearce et al.,1984). Symbols as in Fig. 9.

42 A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46

proposed by Meffre et al. (2008) and Paton et al. (2010). The resultsare plotted on Tera Wasserburg concordia diagrams, and the dataare given in Table 2.

Table 2Zircon U Pb results for the rock samples from the Jerai granite.

Sample-spot Concentrations Isotope

U ppm Th ppm Th/U 206Pb ppm 207Pb/20

BG4Q, Biotite-muscovite granite103 12,875 56 0.0043 338.3 0.0515108 12,260 61 0.0049 342.9 0.051499 6582 108 0.0164 195.2 0.0628109 7585 65 0.0085 219.1 0.0529106 8712 36 0.0041 246.8 0.0546101 5352 29 0.0054 148.1 0.0539100 7299 57 0.0078 211.9 0.0591104 4544 74 0.0164 140.5 0.0554102 7893 77 0.0098 242.6 0.0526110 7385 24 0.0032 227.3 0.0523105 8562 84 0.0098 270.2 0.0535

TG3J, Tourmaline granite81 8085 25 0.0031 220.7 0.050484 4694 6 0.0012 132.0 0.049991 8995 7 0.0008 254.9 0.050585 9842 15 0.0015 282.6 0.051392 6109 13 0.0021 174.9 0.051283 7162 9 0.0012 197.0 0.049990 5774 8 0.0013 158.6 0.049986 7081 5 0.0008 195.5 0.050887 6624 8 0.0012 184.3 0.050388 7077 7 0.0010 213.0 0.055489 8209 11 0.0013 235.2 0.0500

PG2Q, Pegmatite124 4368 15 0.0035 116.0 0.0500122 4895 15 0.0032 136.5 0.0510121 4208 14 0.0034 120.7 0.0539120 4717 20 0.0043 136.4 0.0533119 7118 52 0.0074 208.6 0.0510123 4997 20 0.0039 148.9 0.0518117 4021 44 0.0109 120.2 0.0542

6.2. Results

The U–Pb age results for all three samples are shown in Fig. 14,in which, all the mean 206Pb/238U ages are given at the 95% confi-dence level for all samples. All of the analyses are concordant,and the 206Pb/238U ages for BG4Q (biotite-muscovite granite)(Fig. 14a) scatter between 184 and 216 Ma, giving a weightedmean age of 205.5 ± 4.1 Ma (MSWD = 1.8). For the TG3J (tourma-line granite) (Fig. 14b) and PG2Q (pegmatite) (Fig. 14c), the206Pb/238U ages plot between 188 and 208 Ma and 163 and211 Ma, respectively. This gives the mean age for TG3 J and PG2Qof 205.5 ± 2 Ma (MSDW = 0.19) and 204.6 ± 4.3 Ma (MSWD = 2.5),respectively. The U–Pb zircon geochronology data for the biotite-muscovite granite, tourmaline granite and pegmatite show over-lapping ages within the analytical error.

7. Discussion

7.1. Age and tectonic setting

The Jerai pluton occurs as an isolated granitic complex that hasintruded into the lower Paleozoic metasediments. It is locatedapproximately 50 km to the west of the Main Range Granitebatholith. The U–Pb zircon geochronology shows that the Jeraiintrusion constituted a specific event that occurred at 204.6–205.5 Ma, within the U–Pb zircon age of the Main Range granite(198–225 Ma) (Liew, 1983; Searle et al., 2012; Ng et al., 2015b).The U–Pb zircon emplacement ages for the Main Range granitesrange from Late Triassic (225 ± 1.3 Ma) to earliest Jurassic(200 ± 1.8 Ma), with a peak at approximately 210 Ma (Liew andPage, 1985; Ng et al., 2015b). Ng et al. (2015b) also showed a gen-

ratios Age (Ma)

6Pb ±1 r (%) 206Pb/238U ±1 r (%) 206Pb/238U ±1 r%

1.6 0.0312 1.9 198 40.6 0.0312 1.7 198 30.8 0.0318 0.9 199 20.8 0.0322 0.9 203 21.2 0.0323 1.2 204 21.8 0.0323 1.4 204 31.4 0.0332 1.8 209 41.8 0.0335 1.3 211 32.7 0.0341 2.2 216 50.9 0.0348 1.2 220 30.6 0.0349 2.0 220 4

0.7 0.0306 0.7 194 12.0 0.0312 1.3 198 30.6 0.0317 0.8 201 21.5 0.0319 1.2 202 20.8 0.0320 0.8 203 21.2 0.0321 1.3 204 31.8 0.0322 1.5 205 31.4 0.0323 1.3 205 31.3 0.0325 1.3 206 31.3 0.0327 0.8 206 20.9 0.0325 1.5 206 3

2.2 0.0310 1.3 197 20.9 0.0311 0.8 197 21.2 0.0320 1.0 202 21.0 0.0320 0.8 202 21.2 0.0320 1.9 203 41.4 0.0327 1.0 207 21.9 0.0335 1.5 211 3

Fig. 14. U-Pb LA-ICP-MS zircon geochronology data for the biotite-muscovite granite, Tourmaline granite and pegmatite of the Jerai pluton. Symbols as in Fig. 9.

A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46 43

eral westerly decreasing granitic age trend across PeninsularMalaysia.

It is generally accepted that the subduction of the Paleo-Tethysoceanic floor beneath Indochina terrane started in the Early Per-mian (Metcalfe, 2000; Sone and Metcalfe, 2008). The modelinvolves eastward subduction of the Paleo-Tethyan lithospherebeneath the Paleo-Tethyan Bentong Raub ocean, resulting insubduction-related, Andean I-type granite intrusions and volcan-ism along the Indochina block in the Eastern province (Metcalfe,2000, 2011a, 2011b; Sone and Metcalfe, 2008; Searle et al.,2012). The subduction triggered early magmatism along the east-ern margin of the Indochina terrane, which resulted in the develop-ment of the Sukhothai island arc system (Sone and Metcalfe, 2008;Metcalfe, 2013). Simultaneously (earliest Permian), convection inthe asthenosphere driven by the downward drag of the oceanicslab resulted in spreading and produced a back arc basin behindthe magmatic arc (Sukhothai Arc) (Sone and Metcalfe, 2008;Ghani et al., 2014). Further movement to the east initiated the col-lision between the Sibumasu and Indochina, thrusting Sibumasueastwards under the Central Belt and, thus, potentially doublingthe continental crustal thickness. However, based on the Bouguergravity anomaly data (Ryall, 1982), Oliver et al. (2014) suggestedthat the Sibumasu was thrust over the Indochina province alongthe Bentong Raub suture zone. This resulted in partial melting ofthickened crust in Sibumasu, and the generation of felsic meltemplaced along the Western part of Peninsular Malaysia (Searleet al., 2012; Metcalfe, 2000, 2013). Ng et al. (2015b), based onthe U–Pb zircon SIMS data, suggested that the first contactbetween the Indochina – East Malaya Block and the SibumasuBlock occurred ca. 227 Ma. The felsic melt was generated by crustalmelting in a syn- to post-collisional setting, later emplaced as aMain Range granite batholith. U-Pb zircon ages suggested a fairlyrestricted period of intrusion of the Main Range granites, spanning227–198 Ma (Liew and McCulloch, 1985; Ng et al., 2015b). Basedon the U–Pb zircon geochronology, the Jerai granite was emplacedat the end of the post-collisional event as an isolated pluton at thewesternmost part of the Main Range granite (Fig. 15). The tectonic

relationship between pre-collision I- type granites and syn-collision granites in along India Asia collision (Himalaya and SouthTibet) is comparable to the Peninsular Malaysia granites. Thus theEastern province granitoids are comparable to arc related I typeGandese Ladakh granites (Chiu et al., 2009) and the collisionrelated Main Range granites are comparable to the Greater Hima-laya tourmaline two mica granites.

The U–Pb age obtained from this study also suggests that thevariable ages for the Jerai intrusion obtained by previous research-ers (Bignell and Snelling, 1977) are not the true magmatic age. TheJerai granite was dated using the K/Ar method, which gave an ageof no more than 135 ± 6 Ma (Bignell and Snelling, 1977). They alsogave Lower Tertiary K/Ar mineral ages of 47 ± 3 Ma and 59 ± 3 Ma,respectively, for biotite and muscovite, which were separated frombiotite-muscovite granite. The age given for the Jerai granite is sig-nificantly younger than the general age of the Main Range granite(U–Pb age 198–220 Ma). Another interesting consideration is thatthe biotite-muscovite and the tourmaline granite are almost coe-val. The field relation shows that the pegmatite intrusions areclearly separated in time from those of the tourmaline andbiotite-muscovite granites. The age link between both graniteand pegmatite is an expected result of this study and confirmstheir age.

7.2. Comments on magmatic evolution

The Jerai granite is a highly felsic (SiO2 > 70%), peraluminous(ACNK > 1.3) and perphosphoric (P2O5 up to 0.5%) fractionatedgranite. The pluton consists of two granitic types, which are themain coarse-grained biotite muscovite primary-textured graniteand the fine-grained secondary textured tourmaline granite (seeSection 4 for the introduction of primary and secondary texturedgranite) (Cobbing et al., 1992). The primary-textured biotite gran-ite may represent a primary magma and is geochemically similarto the rest of the Main Range granite. The petrographic features,whole-rock composition and geochemistry of the Jerai graniteallow the distinction between primary-textured biotite-

Fig. 15. Cartoon sketch of the end stage of Sibumasu and Indochina continental collision. Blue circle represent the Jerai granite intruded at the end of the collision (Modifiedfrom Metcalfe (2000)). (For interpretation of the references to colour in this figure legend, the reader is referred to the web version of this article.)

44 A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46

muscovite granite and fine-grained secondary textured tourmalinegranite (Cobbing et al., 1992). Both granites were intruded by a ser-ies of pegmatite dykes. The tourmaline granite and pegmatite aremore differentiated than the biotite-muscovite granite, as demon-strated by the more pronounced peraluminous character, higherSiO2 content (70.95–83.94% and 69.45–73.35%, respectively) andlower biotite content. Based on the U Pb zircon age, both thebiotite-muscovite granite and tourmaline granite magmas mayrepresent the same magmatic event. The pegmatites andtourmaline-bearing granites represent fluids expelled from a par-ental anatectic granite. It is very likely that the biotite muscovitegranite of Jerai represents a fluid-depleted mush, and thus it maybe a cumulate granite (Castro, 2013). The biotite-muscovite granitemagma may have originated from dehydration melting from crus-tal rocks of metasedimentary origin (e.g., Greywackes). The peralu-minous geochemistry, S-type character and presence ofmetasedimentary enclaves strongly support a crustal metasedi-mentary source for these granites.

The relationship between the tourmaline and biotite muscovitegranites are unlikely to be attributable to fractional crystallizationalone, as most of the Harker plots show no continuous trend fromthe less-evolved biotite muscovite granite to the more-evolved

Fig. 16. Comparison between Jerai and other Main Range granite. Selected major a

tourmaline granite. In most of the geochemical plots, tourmalinegranite shows a similarity to pegmatite, which has an affinity withthe geochemical family of granitic pegmatites (Cerny, 1991). Thepresence of tourmaline granite as pods in the biotite muscovitegranite provides strong evidence for the presence and exsolutionof a vapour phase from the Jerai granite magma, probably duringthe final stages of solidification (Jahns, 1982; Jahns and Burnham,1969).

7.3. Relationship to the Main Range granite

The Main Range granites of the Western Belt of PeninsularMalaysia form the largest mountain range of the Peninsula,extending northwards into Thailand and southwards into theIndonesian Tin Islands (Fig. 1). The granite comprises a series oflarge batholiths and plutons of tin-bearing, predominantlybiotite-muscovite granites emplaced in the Lower to MiddlePalaeozoic low-grade metamorphic (greenschist facies) rocks(Cobbing et al., 1992). The granites are regarded as an internationalstandard for S-type granites, as they show high initial 87Sr/86Srratios ranging from 0.7159 to 0.7512, indicating a typical sedimen-tary source (Liew and McCulloch, 1985; Cobbing et al., 1992). The

nd trace elements Harker diagram of both Jerai and other Main Range granite.

Fig. 17. Selected binary plot (a) SiO2 vs. Na2O + K2O, (b) SiO2 vs K2O, (c) SiO2 vs. ACNK and (d) Nb + Y vs. Rb for Jerai and other Main Range Granite. Symbols as in Fig. 16.

A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46 45

geochemical relationship between the Jerai and other Main Rangegranites is shown in Figs. 16 and 17. Comparison plots of the MainRange granite (data taken from Cobbing et al., 1992) are alsoshown for all trace and major elements. In most of the diagramsin Figs. 15 and 16, both the Main Range granite and Jerai biotite-muscovite granite plot in the same field. This can be observed inthe TiO2, Na2O, K2O, P2O5 Ba and Rb vs. SiO2 diagrams. Bothgranites have high TiO2, K2O and Ba and low Na2O, P2O5 andSr compared to both fine-grained tourmaline granite andpegmatite. The geochemical evidence suggests that the biotitemuscovite granite represents a primary melt and has the samegeochemical characteristics as most of the biotite granite fromthe Main Range. In terms of the geotectonic plot (Fig. 13a and b),all biotite muscovite granites from the Jerai pluton plot in thesyn-collision field, which suggests that the granite formed duringthe collision of the Sibumasu and Indochina plates.

7.4. Comments on tin mineralization in the Main Range granite

In Peninsular Malaysia, tin mineralization occurs in both theSibumasu and Indochina blocks. It is not restricted to the peralumi-nous crustal melt granites of the Main Range province, althoughthis is where the majority of tin deposits are hosted. Primary tinmineralization is commonly associated with highly differentiatedlate phase felsic intrusion. Classification of primary tin depositsbased on their occurrences has been summarized by Schwartzet al. (1995). They include (1) hydrothermal veins and lodes, (2)veins, stringers and stockwork, (3) and skarn (pyrometasomatic)mineralization. The skarn type has been divided into three sub-types, namely, Pelepah Kanan, Stanniferous skarns, Stanniferouspegmatites and aplites. The Jerai pegmatite has been classifiedunder Stanniferous peg matites and aplites (Hutchison and Tan,2009); in many cases, the pegmatite and aplite are small andunzoned and characterized by associations with columbite-tantalite. Field relations of the present study suggest that Sn depos-its are hosted by pegmatitic bodies, where the presence of fluidsignificantly altered the granitoids. It was then concentrated by

fluid activities, primarily induced by the devolatization of thegranitic magma. The relative reduced oxidation state of the graniticmagma may also favour the deposition of Sn–W. The occurrence offine-grained, secondary-textured tourmaline granite suggests thatthe Jerai magma was saturated with late-stage fluids that wereresponsible for the post-mineralization fluid movement. Thismight explain the association of Sn with the secondary granite tex-ture (see Cobbing et al., 1992).

8. Conclusions

1. Jerai granite units can be divided into three facies: (i) biotite-muscovite granite; (ii) tourmaline granite; and (iii) pegmatiteand aplopegmatite.

2. The U–Pb zircon geochronology of the Jerai granite gives an ageranging from 204 ± 4.3 Ma for pegmatite, 205 ± 4 Ma and205 ± 2 Ma for the biotite-muscovite granite and tourmalinegranite, respectively.

3. Pegmatite and tourmaline granite are more differentiated thanthe biotite-muscovite granite, as demonstrated by the lowerbiotite content, higher SiO2 content (70.95–83.94 wt.% versus69.45–73.35 wt.%) and the more pronounced peraluminouscharacter.

4. The biotite-muscovite Jerai granites are similar to S-type MainRange granite, but the tourmaline granite has a signature oflate-stage hydrothermal fluid interaction. Age evidence of thesetwo granitic facies suggests that they are derived from the samemagma.

5. The Jerai granite represents the latest magmatic event of thecontinental collision of Sibumasu and Indochina (Liew, 1983;Searle et al., 2012; Ng et al., 2015b).

Acknowledgements

The work was partly sponsored by the University Malaya(UMRG Grant No. RG263/13AFR and the UM/MOHE High Impact

46 A. Jamil et al. / Journal of Asian Earth Sciences 127 (2016) 32–46

Research Grant UM.C/625/HIR/MOHE/SC/23). Thanks are extendedto Dr. Meor Hakif for reviewing earlier versions of this manuscript.

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