Petrogenesis of Malaysian granitoids in the Southeast Asian tin belt: Part 2. U-Pb zircon...

Ng et al.

1238 Geological Society of America Bulletin, v. 127, no. 9/10

Petrogenesis of Malaysian granitoids in the Southeast Asian tin belt: Part 2. U-Pb zircon geochronology and tectonic model

Samuel Wai-Pan Ng1,†, Martin J. Whitehouse2, Michael P. Searle1, Laurence J. Robb1, Azman A. Ghani3, Sun-Lin Chung4,5, Grahame J.H. Oliver6, Masatoshi Sone3, Nicholas J. Gardiner1, and Muhammad H. Roselee3

1Department of Earth Sciences, University of Oxford, South Parks Road, Oxford OX1 3AN, UK2Swedish Museum of Natural History, and Nordic Center for Earth Evolution, Box 50007, SE-104 05 Stockholm, Sweden3Department of Geology, University of Malaya, 50603 Kuala Lumpur, Malaysia4Institute of Earth Sciences, Academia Sinica, Taipei 10529, Taiwan5Department of Geosciences, National Taiwan University, Taipei 10617, Taiwan6Department of Geography, National University of Singapore, Singapore 117570

ABSTRACT

In our complementary geochemical study (Part 1), the Malaysian granitoids of the Southeast Asian tin belt were divided into a Middle Permian to Late Triassic I-type–domi-nated Eastern province (Indochina terrane) and a Triassic to Early Jurassic transitional I/S-type Main Range province (Sibumasu terrane), separated by the Bentong-Raub suture zone which closed in the Late Triassic. Previous geochronology has relied on only a few U-Pb zircon ages together with K-Ar and whole rock Rb-Sr ages that may not accu-rately record true magmatic ages. We pre sent 39 new high-precision U-Pb zircon ion micro-probe ages from granitoids and vol canics across the Malay Peninsula. Our results show that ages from the Eastern province granit-oids span 289–220 Ma, with those from the Main Range province granitoids being en-tirely Late Triassic, spanning 227–201 Ma. A general westerly younging magmatic trend across the Malay Peninsula is considered to reflect steepening and roll-back of the Ben-tong-Raub subduction zone during progres-sive closure of Paleo-Tethys. The youngest ages of subduction-related granites in the Eastern province roughly coincide with the youngest ages of marine sedimentary rocks along the Paleo-Tethyan suture zone. Our petrogenetic and U-Pb zircon age data sup-port models that relate the Eastern prov-ince granites to pre-collisional Andean-type magmatism and the western Main Range province granites to syn- and post-collisional

crustal melting of Sibumasu crust during the Late Triassic. Tin mineralization was mainly associated with the latter phase of magma-tism. Two alternative tectonic models are dis-cussed to explain the Triassic evolution of the Malay Peninsula. The first involves a second Late Triassic to Jurassic or Early Cretaceous east-dipping subduction zone west of Sibu-masu where subduction-related hornblende and biotite–bearing granites along Sibumasu are paired with Main Range crustal-melt tin-bearing granites, analogous to the Bolivia Cordilleran tin-bearing granite belt. The sec-ond model involves westward underthrusting of Indochina beneath the West Malaya Main Range province, resulting in crustal thicken-ing and formation of tin-bearing granites of the Main Ranges. Cretaceous granitoids are also present locally in Singapore (Ubin dio-rite), on Tioman Island, in the Noring pluton, of the Stong complex (Eastern Province), and along the Sibumasu terrane in southwest Thailand and Burma (Myanmar), reflecting localized crustal melting.

INTRODUCTION

The Permo-Triassic tectonics of the Malay Peninsula have been interpreted in terms of east-ward-dipping subduction of Permian–Early Tri-assic oceanic lithosphere beneath the Andean-type margin of Indochina–East Malaya followed by the closure of Paleo-Tethys along the Ben-tong-Raub suture zone during the Middle–Late Triassic (Hutchison, 1973; Mitchell, 1977; Sone and Metcalfe, 2008; Searle et al., 2012; Oliver et al., 2014). In Thailand a Permian–Early Trias-sic island arc terrane, the Sukhothai island arc, is sandwiched between Indochina to the east and Sibumasu to the west (Sone and Metcalfe, 2008;

Metcalfe, 2011). Cobbing et al. (1986) proposed that the Malay Eastern province granitoids were Cordilleran I-type granites formed above the east-dipping subduction zone along the Ben-tong-Raub suture zone, while the Malay Main Range province granitoids were S-type granites emplaced into the Sibumasu terrane to the west of the suture (Fig. 1). The I- and S-type generic system of granitoids was initially proposed by Chappell and White (1974) and was used to categorize Malaysian granitoids by Beckinsale (1979) and Cobbing et al. (1986). The lack of U-Pb zircon ages was a major hindrance to understanding the tectonic evolution of Malay-sia, which had previously relied on K-Ar mica cooling ages and Rb-Sr isochron ages (Bignell and Snelling, 1977; Darbyshire, 1988; Krähen-buhl, 1991).

The direct application of Chappell and White’s (1974) I- and S-type generic system was ques-tioned by Ghani (2000), Ghani et al. (2013b), Searle et al. (2012), and in Part 1 of the present study (Ng et al., 2015). It was shown that despite being divided into two tectonic provinces based on slight differences in lithology, geochemistry, and isotopes, Malaysian granitoids originated from similar parental igneous protoliths mixed with different proportions of sedimentary proto-liths (Ng et al., 2015). The trace element geo-chemistry of these granitoids shows that they are more fractionated and more enriched than typical Cordilleran I- and S-type granitoids as documented by Chappell and White (1974). The petrogenetic model for the Malaysian granitoids proposed in Part 1 (Ng et al., 2015) now requires temporal constraints, reported here. It has been shown that the dating methods employed by previous workers (Bignell and Snelling, 1977; Darbyshire, 1988; Krähenbuhl, 1991) are not able to accurately interpret the crystallization

GSA Bulletin; September/October 2015; v. 127; no. 9/10; p. 1238–1258; doi: 10.1130/B31214.1; 11 figures; 3 tables; Data Repository item 2015121; published online 3 April 2015.

†Current address: Department of Earth Sciences, The University of Hong Kong, Pok Fu Lam Road, Pok Fu Lam, Hong Kong; waipanng@ hku .hk.

For permission to copy, contact [email protected] © 2015 Geological Society of America

Petrogenesis of Malaysian granitoids in the Southeast Asian tin belt: Part 2

Geological Society of America Bulletin, v. 127, no. 9/10 1239

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Ng et al.


age for granite because the closure tempera-tures are lower than the granite crystallization temperatures (Searle et al., 2012). Although some initial high-precision U-Pb zircon dat-ing has been published by Liew (1983), Liew and McCulloch (1985), Liew and Page (1985), and more recently by Searle et al. (2012) and Oliver et al. (2014), there are no more than 20 ages available throughout the Malay Peninsula. In this paper, 39 additional high-precision U-Pb ages are presented, ages that allow better tem-poral constraints to be placed on the tectonic evolution of the Malay Peninsula. Together with our new understanding on the petrogenesis of the Malaysian granitoids (Ng et al., 2015), we discuss two possible tectonic models for the evolution of the Malay granite provinces.

GEOLOGICAL BACKGROUND

Southeast Asia comprises accreted Precam-brian continental terranes that have succes-sively rifted off from Gondwana since the Early Devonian, when the Paleo-Tethys Ocean started opening (Metcalfe, 2011). These terranes were reassembled again along sutures on the Eur-asian plate, forming a biogeographical terrane referred to as Sundaland in some literature (Fig. 1) (Asama, 1984; Bird et al., 2005; Met-calfe, 2011). The tectonic evolution of Sunda-land can be constrained temporally and spatially by both the fossil record and paleomagnetic data from various terranes. A Cathaysia-related Late Permian Gigantopteris flora is found in Indo-china–East Malaya and Northern Thailand east of the Nan-Uttaradit line (Fontaine and Work-man, 1978; Asama, 1984; Hutchison, 2007). A Gondwana-related Permian Glossopteris flora is found to the west of the Nan-Uttaradit line in the Sibumasu terrane, which was not sepa-rated from Gondwana until the Early Permian (Hutchison, 2007; Metcalfe, 2011). The divi-sion between these two floral provinces lies on both the Nan-Uttaradit line and the Ben-tong-Raub line (Fig. 1) (Hutchison, 2007). It was traditionally believed that these divisions marked the location of the Paleo-Tethys Ocean, although the nature of the Nan-Uttaradit line as a major suture has been recently challenged by Sone and Metcalfe (2008). These authors recognized the existence of the Sukhothai arc terrane in between the Indochina and the Sibu-masu terranes, while the Nan-Uttaradit line was described as a parallel suture responsible for the closure of the suprasubduction back-arc basin created between the Sukhothai arc terrane and the Indochina terrane (Sone and Metcalfe, 2008). Metcalfe (2013) later suggested that this island arc could be extended to the Malay Pen-insula and be responsible for the I-type magma-

tism in the Eastern province. However, there is no field evidence for Mesozoic back-arc rifting on the Malay Peninsula to support this specula-tion. The hypothesis is also not supported by the geochemistry of the Eastern province granitoids (Ng et al., 2015). The granitoids are generally peraluminous, unlike the metaluminous island arc granites. The parental magma of the Eastern province granitoids would require sedimentary source input, which could not be sufficiently provided by an island arc terrane. The Bentong-Raub line running along the Malay Peninsula remains as the most widely accepted main suture of the Paleo-Tethys Ocean (Hutchison, 1977; Mitchell, 1977).

It is generally accepted that the Malaysian granitoids were formed in this convergent tec-tonic regime. The “I-type” Eastern province granitoids were associated with Andean-type magmatism and emplaced into the Indochina–East Malaya terrane, while the “S-type” Main Range province granitoids were formed in the subsequent continental crustal thickening set-ting. The “I-S” designation was given, as this model appears to be supported by field and petrographic observations, in which granitoids to the east of the Bentong-Raub line contain hornblende and biotite, while those to the west contain biotite but locally also have S-type min-erals such as tourmaline, muscovite, andalusite, garnet, and low-Al biotite (Cobbing et al., 1986; Ghani, 2000). The Main Range province gran-itoids are more potassic and less sodic than the Eastern province granitoids. However, Part 1 of this study (Ng et al., 2015) questioned this designation, as it noted that these observations are not regionally applicable, and earlier stud-ies appear to have overlooked the similarities shared by these granitic provinces. For exam-ple, the Bintang batholith in the Main Range province has some characteristics similar to those of some granites in the Eastern prov-ince. Moreover, muscovite grains present in the Main Range province are commonly secondary (Schwartz et al., 1995), although locally pri-mary muscovite was also reported in the Main Range province granitoids (Liew, 1983; Cob-bing et al., 1992). The secondary muscovites are related to post-magmatic hydrothermal altera-tion and to greisenization. Most of the Main Range province granitoids are biotite granites devoid of hornblende, such as those also present in the Eastern province (Schwartz et al., 1995). Hence, the mineralogical differences between the two provinces are less distinctive than pre-vious workers indicated. Moreover, the trace element geochemistry of the Malaysian granit-oids shows that both Eastern province and Main Range province granitoids follow the same trace element enrichment and depletion pattern while

their liquid lines of descent in crystal fraction-ation are parallel and largely overlapped with each other (Ng et al., 2015). The Sr-Nd isotopic data also showed that they were both formed from similar hybridized parental melt of igne-ous and sedimentary protoliths but in different proportions.

In Part 1 (Ng et al., 2015), the Sr-Nd isotopic data demonstrated that the hybridized parental melt was probably a mixture of differing pro-portions of melts derived from crustal rocks iso-topically similar to the enriched ortho amphibo-lites and paragneisses of the Indochina Kontum massif . The orthoamphibolite is a metamor-phosed product of Ordovician intraplate tholei-itic basalt while the paragneiss represents Meso-proterozoic basement of the Indochina terrane (Lan et al., 2003). It is believed that the crustal rocks similar to the Ordovician Kontum amphib-olite could give the enriched high field strength element (HFSE) signature to the Malaysian granitoids (Ng et al., 2015). With this model, around 20% of sedimentary-sourced melt was incorporated into the parental melt that formed the Eastern province granitoids, while up to 40% was involved in the formation of the Main Range province granitoids. The higher involve-ment of sedimentary-sourced melt in the Main Range province was due to the compositional difference between the two continental terranes, whereby the Sibumasu terrane might be more dominated by sedimentary protoliths compared with the Indochina–East Malaya terrane. Both Indochina and Sibumasu crust comprise Lower Paleozoic sedimentary and carbonate rocks, but the succession hosted by the Sibumasu terrane is more complete, causing the Sibumasu crust to be 13 km thicker (Ghani et al., 2013a). The incorporation of sedimentary material into the parental magma can be inferred by the pres-ence of ilmenite-series granitoids in the Eastern and Main Range provinces, and this also sug-gests that the Eastern province granitoids are more reduced than typical Cordilleran I-type granitoids. The hybridization of igneous- and sedimentary-sourced melts in a reduced envi-ronment may favor the metallogenesis of Sn-W deposits (Ng et al., 2015).

U-Pb ZIRCON GEOCHRONOLOGY

Geochronological work on these granitoids started in the late 1970s. Bignell and Snelling (1977) and Darbyshire (1988) were the first group to date the Malaysian granitoids using K-Ar mica ages and Rb-Sr whole rock isochron ages (Table 1). These studies suggested that the Eastern province granitoids were formed mainly in the Permo-Triassic periods with few plutons formed in the Cretaceous. However,



both dating methods are unreliable as the parent and daughter isotopes in the Rb-Sr system are extremely mobile in magmatic-hydrothermal systems and readily reset, while the K-Ar ages represent only the cooling age of the rock through the closure temperatures of muscovite and biotite (350–300 °C) (Searle et al., 2012). It is now widely accepted that these methods can-not produce reliable crystallization ages for rocks such as the highly mineralized granitoids of the Malay Peninsula. The robustness of the U-Pb system in zircon makes it the preferred method for granitoid dating, and, since the development of high-spatial-resolution U-Pb isotopic analysis using microbeam methods in zircon (e.g., sec-ondary ionization mass spectrometry [SIMS]), this has become routine, allowing for the rapid and precise determination of both crystallization ages and possible inherited ages in zircon cores.

Before this work, only twenty reliable U-Pb zircon ages for the Malaysian granitoids were available (Table 1). They were obtained mainly from granitoids collected along the eastern and western coasts of the Malay Peninsula and in Singapore (ages in boxes in Fig. 2) (Liew, 1983; Liew and McCulloch, 1985; Liew and Page, 1985; Searle et al., 2012; Oliver et al., 2014). More extensive high-precision U-Pb geochro-nology on the Malaysian granitoids is clearly necessary for the reconstruction of the Malay-sian tectonic framework. Thirty-nine new U-Pb zircon ages have been obtained in our study, and will be presented in the following sections. We analyzed 24 samples from the Eastern province and 15 samples from the Main Range province. Most of the rock samples were collected from road cuts and quarries. Samples of the Stong region were collected mainly from riverside out-

crops along the Kenerong and Renyok Rivers. Samples collected from outlying islands like Perhentian, Tioman, Penang, Langkawi, and Ubin were from fresh shoreline outcrops.

High-spatial-resolution, high-precision SIMS was used to analyze the U-Pb isotopic composi-tion of the extracted zircon grains. The grains were extracted from rock samples by standard disaggregation, heavy liquid (bromoform) separation, and magnetic separation proce-dures. Handpicked zircon grains were then mounted in epoxy, polished, and imaged using a Robinson cathodoluminescence (CL) detector mounted to a Hitachi S4300 scanning electron microscope. U-Pb isotope ratios were collected using a Cameca IMS1280 ion microprobe at the NordSIM facility, Swedish Museum of Natu-ral History, Stockholm, following the proto-cols described by Whitehouse et al. (1999) and

TABLE 1. SUMMARY OF RADIOMETRIC DATING OF MALAYSIAN GRANITOIDS PRIOR TO THIS STUDY; DATA COMPILATION AFTER GHANI (2009)

)aM(eganocrizbP-U)aM(egaacimrA-K)aM(eganorhcosirS-bRnoitacoLecnivorPEastern province–Eastern belt Bekok1 218

Belumut1 231–234Bidang1,2 922–0414±312Bukit Batu1 224Dura2 240 ± 10Kerai2 205 ± 25Lata Tungil3 215 ± 10Lunchoo2 812–5026±712Nal2 230 ± 4Panchor2 00203±791Saok1,4 752262–432Chukai5 240–243Kemaman1,5 253–275, 327, 271Kuantan1,4,5,6,7 252, 207–247 263Paka1,4 722022Sungai Lembing1,5 156

Eastern province–Central belt Batang Melaka1,8 69–72, 81.9 ± 1.1Stong–Kenerong1,2 563±97Stong–Noring2 90 ± 3Benom1,2,3 207 ± 7, 219 ± 10 123–199, 169

)etitamgep(iareJecnivorpegnaRniaM 1 47, 59–137Langkawi1,8 79.1 ± 0.8, 82Bukit Mor1 135–164Kledang Range1,8 198–213, 193–216, 203Ipoh East8 176–204, 193–209Cameron Highlands8 105–205Bukit Tinggi1 237Ampang1 202Berenang1,2,4,9 215 ± 2 124–214, 156–218 211–215Bubu (Bintang)1,4 198Bujang Melaka1,2,5 207 ± 14, 194 192–208, 203–210Dingdings1,2 681–3717±312Genting Sempah1,4 912891Jelutong2 211 ± 9Jor Dam1 100–199Kajang9 134–188, 170–217Kulim–Bongsu1,2 102–6915±422Penang–Batak1,4,10 180–199, 185–194 215Penang–Bunga1,4,10 402–8613±022Penang–Feringgi1,2,4,10 212 ± 7Selama2 230 ± 9Seremban1,9 82–173, 160–201Sik1 135–190, 178Sungai Baru1 156Tampin1,2 971–1821±522Tranum1,4 802561–061Ulu Kali1,4,9,11 602–891771,841–39602Wing Sang Cheong11 198–202

Note: Ages are provided by: 1Bignell and Snelling (1977); 2Darbyshire (1988); 3Cobbing et al. (1992); 4Liew (1983); 5Schwartz and Askury (1990); 6Liew and McCulloch (1985); 7Yap (1986); 8Krähenbuhl (1991); 9Kwan (1990); 10Kwan and Yap (1986); 11Yap and Kwan (1984).

Ng et al.


104°°301°201°101°00199°E

104°

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6°

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Main Range Province granitoids

Alkali granitoids

Eastern Province granitoids

50 km0

THAILAND

Main Range batholith Benom

Kapal batholith

Kuantan

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Perhentian

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Tioman

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(d) - Granitic dyke(da) - Dacite(di) - Diorite(l) - Leucogranite(r) - Rhyolite(s) - Syenite

1 - Liew, 1983; Liew and Page, 19852 - Liew, 1983; Liew and McCulloch, 19853 - Searle et al., 20124 - Oliver et al., 20145 - This work

*220 ± 4 Ma (d)5

84 ± 1 Ma (l)5

258 ± 2 Ma5

284 ± 2 Ma (s)5

*289 ± 2 Ma5

248 ± 2 Ma5

232 ± 1 Ma5

248 ± 2 Ma5

227 ± 2 Ma2

250 ± 2 Ma (da)5

267 ± 2 Ma2

270 ± 1 Ma5222 ± 2 Ma (d)6

80 ± 1 Ma3

80 ± 1 Ma5

80 ± 1 Ma5

80 ± 1 Ma (d)5

82 ± 1 Ma (di)5

81 ± 1 Ma (mg)5

237 ± 1 Ma4

244 ± 2 Ma4

238 ± 2 Ma (r)4

230 ± 6 Ma4

*231 ± 3 Ma5

222 ± 2 Ma5

227 ± 2 Ma5

*226 ± 3 Ma5

238 ± 2 Ma4

239 ± 2 Ma (r)5

*244.5 ±3.1 Ma5

226 ± 1 Ma5

76 ± 1 Ma5

285 ± 5 Ma4

276 ± 5 Ma4

257 ± 4 Ma2

215 ± 3 Ma5

216 ± 2 Ma5

209 ± 1 Ma1

215 ± 6 Ma1

214 ± 3 Ma5

216 ± 2 Ma5

212 ± 2 Ma5

216 ± 2 Ma5

220 ± 1 Ma5220 ± 3 Ma5

219 ± 2 Ma5

225 ± 1 Ma5

218 ± 2 Ma5

209 ± 2 Ma1

206 ± 2 Ma1

198 ± 2 Ma1

219 ± 9 Ma1

215 ± 2 Ma1

215 ± 7 Ma3

210 ± 7 Ma3

222 ± 2 Ma5

201 ± 2 Ma5

226 ± 1 Ma (d)5

217 ± 1 Ma5

Figure 2. U-Pb zircon ages of the Malaysian granitoids presented in this research and those provided by previous workers (Liew, 1983; Liew and McCulloch, 1985; Liew and Page, 1985; Oliver et al., 2014; Searle et al., 2012).



Whitehouse and Kamber (2004). Instrument configuration details as well as the full analyti-cal data are provided in the GSA Data Reposi-tory1. Discussion of the data is presented in groups according to the geographical locality of samples. Data are summarized in Tables 2 and 3, and the ages obtained are mapped on Figure 2. Selected CL images of dated zircon grains and Tera-Wasserburg concordia diagram inter-pretations of all the samples are presented in Figures 3 and 4 respectively. The Tera-Wasser-burg concordia diagrams are preferred here because the 238U/206Pb axis stretches out toward young (<500 Ma) data, which is easier to visual-ize in this type of diagram. In addition, Pb loss is horizontal if it is recent. Given the ubiquitous presence of post-crystallization, possibly recent, Pb loss, causing a skewed age dispersion toward apparently younger ages, as well as the presence in some zircon grains of clear inherited cores, we used a consistent filtering approach to extract the probable crystallization age. This involved first excluding any obvious older cores, then reject-ing the youngest analyses (238U/206Pb age) inter-preted on the basis of CL images to belong to the main magmatic crystallization group, which most likely reflect Pb loss, until the remaining group of ages yielded a concordia age sensu Ludwig (1998), with a statistically significant low mean square weighted deviation (MSWD). In general, we consider concordia ages obtained from five or more pooled analyses to be robust indicators of the magmatic crystallization age, while those incorporating fewer analyses are given as reference ages that are accorded some-what lower significance in our interpretation. All ages are presented at 2s (or, where appropriate, 95% confidence level), including decay con-stant errors, with the MSWD value representing that of both concordance and equivalence, fol-lowing the recommendation of Ludwig (1998). Decay constants follow the recommendations of Steiger and Jäger (1977).

In this section, the U-Pb zircon data and ages of the Eastern province and Main Range granit-oids are presented separately. The Eastern prov-ince granitoids are further divided into Eastern belt granitoids, Central belt granitoids, based on the stratigraphy of the host rocks and Cre-taceous granitoids for the convenience of data presentation. It should be noted that there is no significant compositional or geochemical differ-ence between the granitoids in the Eastern belt and the Central belt (Ng et al., 2015).

1GSA Data Repository item 2015121, Methodol-ogy on U-Pb zircon geochronology,Tera-Wasserburg diagrams for all dated samples and ion microprobe U-Th-Pb data of the zircons extracted from the sam-ples, is available at http:// www .geosociety .org /pubs /ft2015 .htm or by request to editing@ geosociety .org.

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zoni

ng66

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000.

27–0

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30,1

00

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suonegomo

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ory

zoni

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0–38

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.76

1300 0086

36.0–92.00023–024

gninozyrotallicso

raelC

krad-LC

smsirp

detecaf-lleW

051–05natnau

K55

AM

006,2169.0–90.0

0022–083gninoz

yrotallicsotniaF

krad-LC

detnemgar

F081–05

ukeB

kayniM

66A

M MA

68B

atu

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at–H

anso

n qu

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ell-f

acet

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rism

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nd C

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ca

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lear

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zoni

ng49

0–32

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M59

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22,0

00 005266.0–75.0

066–012gninoz

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thgirb-LC

smsirp

detecaf-lleW

081–08dnalsI

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000.

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29,0

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098–096gninoz

yrotallicsotniaF

krad-LC

smsirp

detecaf-lleW

002–08gnaul

K–gnaulameJ

401A

Myrotallicso

raelc,mir-ero

Cthgirb-L

Cs

msirpdetecaf-lle

W022–08

nahame

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zoni

ng44

0–92

00.

15–0

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1800

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e: C

ore-

rim—

core

-rim

rel

atio

nshi

p (t

wo-

stag

e gr

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) is

obs

erve

d.

Ng et al.


TAB

LE 2

B. Z

IRC

ON

PR

OP

ER

TIE

S O

F T

HE

EA

ST

ER

N P

RO

VIN

CE

CR

ETA

CE

OU

S G

RA

NIT

OID

S

Sam

ple

no.

Loca

tion

Zirc

on s

ize

(dia

met

er)

(nm

)Z

ircon

sha

peC

ore

(CL—

cath

odol

umin

esce

nce)

Text

ure

U c

onte

nt in

age

-yi

eldi

ng g

roup

(pp

m)

Th/

U r

atio

in a

ge-

yiel

ding

gro

upH

ighe

st-U

gra

in in

sa

mpl

e (p

pm)

MA

43K

ener

ong–

Ren

yok

Riv

er0066

50.4–55.10021–054

gninozyrotallicso

raelC

thgirb-LC

smsirp

detecaf-lleW

001–05

000307.1–05.0

0032–026gninoz

yrotallicsorael

Cthgirb-L

Cs

msirpdetecaf-lle

W022–021

gniroN

54A

M,denoznu

suonegomo

Hthgirb-L

Cs

msirpdetecaf-lle

W051–08

dnalsIna

moiT87

AM

clou

dy60

–160

00.

45–1

.25

5900

thgirb-LC

dnakrad-L

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Bs

msirpdetecaf-lle

W001–05

09A

Mca

n be

foun

dH

omog

enou

s un

zone

d,

clou

dy, c

ore-

rim50

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1.40

–1.7

985

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thgirb-LC

dnakrad-L

Chto

Bs

msirpdetecaf-lle

W001–05

19A

Mca

n be

foun

dH

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00.

36–0

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376,

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msirpdetecaf-lle

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79A

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cilla

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zon

ing

120–

750

0.55

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611

00

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thgirb-LC

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m-LC

smsirp

detecaf-lleW

022–08001

AM

clou

dy, c

ore-

rim90

–300

0.59

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717

00

Not

e: C

ore-

rim—

core

-rim

rel

atio

nshi

p (t

wo-

stag

e gr

owth

) is

obs

erve

d.

TAB

LE 2

C. Z

IRC

ON

PR

OP

ER

TIE

S O

F T

HE

MA

IN R

AN

GE

PR

OV

INC

E G

RA

NIT

OID

S

Sam

ple

no.

Loca

tion

Zirc

on s

ize

(dia

met

er)

(nm

)Z

ircon

sha

peC

ore

(CL—

cath

odol

umin

esce

nce)

Text

ure

U c

onte

nt in

age

-yi

eldi

ng g

roup

(pp

m)

Th/

U r

atio

in a

ge-

yiel

ding

gro

upH

ighe

st-U

gra

in in

sa

mpl

e (p

pm)

MA

06C

amer

on H

ighl

ands

50–1

50W

ell-f

acet

ed p

rism

sB

oth

CL-

dark

and

CL-

brig

ht

can

be fo

und

Cle

ar o

scill

ator

y zo

ning

320–

1200

0.08

–0.7

347

,400

,denoznusuonego

moH

krad-LC

smsirp

detecaf-lleW

051–0570

AM

clou

dy15

00–8

500

0.35

–1.1

719

,300

yrotallicsoraelc,

mir-eroC

thgirb-LC

smsirp

detecaf-lleW

052–00131

AM

zoni

ng10

0–32

00.

27–0

.76

4040

smsirp

detecaf-lleW

002–0841

AM

and

frag

men

tsyrotallicsotniaf,

mir-eroC

thgirb-LC

zoni

ng46

0–15

000.

04–0

.69

1510

thgirb-LC

dnakrad-L

Chto

Bs

msirpdetecaf-lle

W022–04

hopI51

AM

can

be fo

und

Cor

e-rim

, fai

nt o

scill

ator

y zo

ning

280–

3000

0.13

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353

20

MA

16Ta

ipin

g40

–200

Wel

l-fac

eted

pris

ms

and

frag

men

tsB

oth

CL-

dark

and

CL-

brig

ht

can

be fo

und

Cle

ar o

scill

ator

y zo

ning

480–

1820

0.11

–1.1

784

40

MA

19P

enan

g Is

land

80–3

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ell-f

acet

ed p

rism

s an

d fr

agm

ents

yrotallicsotniaf,mir-ero

Cthgirb-L

Czo

ning

240–

1450

0.23

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155

40

smsirp

detecaf-lleW

003–0802

AM

and

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tsyrotallicsotniaf,

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krad-LC

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ng77

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600.

40–0

.54

6520

smsirp

detecaf-lleW

003–0432

AM

and

frag

men

tsyrotallicsotniaf,

mir-eroC

thgirb-LC

zoni

ng70

–520

0.33

–0.7

395

0


Cthgirb-L

Cs

msirpdetecaf-lle

W003–051

dnalsIiwakgnaL

62A

Mzo

ning

160–

720

0.13

–1.3

544

50


Cthgirb-L

Cs

msirpdetecaf-lle

W003–051

03A

Mzo

ning

160–

660

0.25

–0.6

823

40


Cthgirb-L

Cdetne

mgarF

082–021dnalsI

abuT92

AM

zoni

ng45

0–15

500.

12–0

.41

3965

yrotallicsoraelc,

mir-eroC

thgirb-LC

smsirp

detecaf-lleW

051–05rup

muLalau

K13

AM

zoni

ng54

0–11

600.

10–0

.94

6180 0403

09.0–64.00201–063

gninozyrotallicso

raelC

krad-LC

smsirp

detecaf-lleW

021–05ro

MtikuB

26A

Myrotallicso

raelc,mir-ero

Ckrad-L

Cdetne

mgarF

022–08hap

meS

gnitneG

011A

Mzo

ning

650–

1480

0.19

–0.6

847

10

Not

e: C

ore-

rim—

core

-rim

rel

atio

nshi

p (t

wo-

stag

e gr

owth

) is

obs

erve

d.



TABLE 3A. U-Pb ZIRCON AGES OF THE EASTERN PROVINCE GRANITOIDS IN THE EASTERN BELT

Sample edutignoLedutitaLnoitacoLygolohtiL.on

Age (Ma)

MSWD of conc. and equiv.

n, total

n, age cluster

dnalsInaitnehrePetinargtB74AM 05°55′16.5″N 102°43′23.9″E 257.6 ± 1.6 0.62 12 9MA48 Syenite 284.2 ± 1.6 1.17 33 10MA50 Kfs-phyric (Hbl)-Bt granite

w/ Qtz-Tour miarolitic cavitiesMaras-Jong 05°20′47.6″N 103°02′12.5″E 289.3 ± 2.4* 1.15 20 4

egnaRlapaKetinargtB-lbH15AM 05°09′04.2″N 102°46′59.2″E 247.8 ± 1.7 0.53 25 7egnaRyradnuoBetinargtB-lbH25AM 04°59′21.6″N 102°28′53.3″E 248.4 ± 1.8 1.60 12 7

MA54 Kfs-Pl–phyric dacite Kerteh 04°37′12.1″N 103°24′20.8″E 250.5 ± 1.7 0.60 38 7natnauKetinargtB-lbH55AM 03°50′19.7″N 103°21′07.1″E 270.0 ± 1.4 1.40 25 12

MA73 Migmatitic granite Ubin Island 01°24′29.0″N 103°59′21.8″E 231.0 ± 2.6* 2.10 15 3MA76 Kfs-phyric rhyolite Musoh River mouth 01°22′13.0″N 104°16′50.9″E 238.5 ± 1.7 1.02 15 6MA104 Kfs-phyric Hbl-Bt granite Jemaluang–Kluang 02°18′10.4″N 103°39′25.2″E 244.5 ± 3.1* 1.70 15 3

Note: Ages with asterisks (*) represent reference ages yielded by a group of less than fi ve but at least three pooled analyses in the Tera-Wasserburg diagram. Mineral abbreviations: Bt—biotite; Hbl—hornblende; Kfs—K-feldspar; Pl—plagioclase; Qtz—quartz; Tour—tourmaline. MSWD of conc. and equiv.—Mean square of weighted deviation of combined concordance and equivalence.

TABLE 3B. U-Pb ZIRCON AGES OF THE EASTERN PROVINCE GRANITOIDS IN THE CENTRAL BELT


Age (Ma)


n, total

n, age cluster

enimdlogmojnePekidetisleF33AM 04°08′40.0″N 101°59′29.3″E 222.4 ± 1.8 1.20 32 5MA36 Kfs-phyric Hbl-Bt tonalite Berengkat–Kampong Jerek 05°08′22.2″N 101°58′49.5″E 231.8 ± 1.7 0.95 20 5MA42 Migmatitic tonalite Berengkat–Renyok River 05°34′47.1″N 101°52′25.5″E 220.4 ± 3.9* 2.40 12 4MA66 Cpx-Hbl-Bt granite Minyak Beku 01°49′08.8″N 102°54′37.3″E 222.2 ± 1.8 0.96 15 5MA68 Kfs-phyric Bt microgranite Batu Pahat–Hanson quarry 01°49′01.0″N 102°54′50.9″E 227.2 ± 1.9 0.67 15 5MA69 Kfs-phyric Bt granite 225.5 ± 2.5* 0.24 15 3MA109 Kfs-phyric Bt granite Kemahan 05°49′11.1″N 101°56′07.2″E 226.7 ± 2.2 2.00 15 5

Note: Ages with asterisks (*) represent reference ages yielded by a group of less than fi ve but at least three pooled analyses in the Tera-Wasserburg diagram. Mineral abbreviations: Bt—biotite; Cpx—clinopyroxene; Hbl—hornblende; Kfs—K-feldspar. MSWD of conc. and equiv.—Mean square of weighted deviation of combined concordance and equivalence.

TABLE 3C. U-Pb ZIRCON AGES OF THE CRETACEOUS GRANITOIDS IN THE EASTERN PROVINCE


Age (Ma)


n, total

n, age cluster

MA43 Leucogranitic dike Kenerong–Renyok River 05°34′47.1″N 101°52′25.5″E 83.9 ± 0.8 0.70 12 7MA45 Kfs-phyric Hbl-Bt granite Noring 05°39′42.5″N 101°41′26.7″E 75.7 ± 0.6 1.17 20 5MA78 Cpx-Hbl-Bt granite Tioman Island 02°48′26.1″N 104°09′20.0″E 80.1 ± 0.6 1.20 15 7MA90 Microgranitic dike 02°43′06.9″N 104°10′27.0″E 80.2 ± 0.7 1.50 15 5MA91 Diorite 81.5 ± 0.7 1.40 14 5MA97 Ms-Tour granite 02°49′48.8″N 104°11′44.2″E 79.7 ± 0.7 1.01 15 5MA100 Migmatitic granite 02°46′39.4″N 104°12′59.9″E 80.7 ± 0.5 1.30 14 8

Note: Mineral abbreviations: Bt—biotite; Cpx—clinopyroxene; Hbl—hornblende; Kfs—K-feldspar; Ms—muscovite; Tour—tourmaline. MSWD of conc. and equiv.—Mean square of weighted deviation of combined concordance and equivalence.

TABLE 3D. U-Pb ZIRCON AGES OF THE MAIN RANGE PROVINCE GRANITOIDS


Age (Ma)


n, total

n, age cluster

MA06 Kfs-phyric Crd-Bt granite Cameron Highlands 04°33′50.4″N 101°11′55.4″E 220.1 ± 2.8* 1.60 34 4MA07 Fe-stained Bt granite 219.4 ± 1.5 0.57 20 6MA13 Kfs-phyric Ms-Bt granite 04°35′00.3″N 101°24′24.5″E 225.4 ± 1.3 1.09 38 10MA14 Kfs-phyric Ms-Bt microgranite 04°34′49.5″N 101°20′22.8″E 218.3 ± 2.4 1.18 11 9MA15 Kfs-phyric Ms-Bt granite Ipoh 04°32′56.1″N 101°01′46.8″E 220.1 ± 1.0 0.79 20 13MA16 Kfs-phyric Hbl-Bt granite Taiping 04°46′54.9″N 100°44′11.0″E 215.7 ± 1.6 1.09 20 7MA19 Kfs-phyric Bt granite Penang Island 05°27′48.0″N 100°13′58.9″E 213.9 ± 2.9* 0.38 11 4MA20 Kfs-phyric microgranite 05°28′13.5″N 100°11′31.1″E 215.5 ± 1.5* 1.50 10 4MA23 Kfs-phyric Bt granite 05°16′11.3″N 100°16′57.3″E 212.1 ± 2.4 1.60 20 6MA26 Kfs-phyric Bt granite Langkawi Island 06°24′11.4″N 99°48′12.3″E 215.3 ± 2.6 1.90 12 6MA30 Kfs-phyric Ms-Bt microgranite 06°17′56.9″N 99°51′10.1″E 215.9 ± 1.7 0.58 12 6MA29 Ms-Bt microgranite Tuba Island 06°15′45.6″N 99°51′02.1″E 200.8 ± 2.0* 1.90 34 4MA31 Kfs-phyric Bt granite Kuala Lumpur 03°19′39.6″N 101°44′52.0″E 222.4 ± 1.8 0.91 35 5MA62 Kfs-phyric Bt granite Bukit Mor 01°58′32.8″N 102°40′24.5″E 217.4 ± 1.2 1.20 15 6MA110 Qtz-phyric Opx dacite Genting Sempah 03°21′10.9″N 101°48′39.9″E 226.2 ± 1.2 1.30 15 6

Note: Ages with asterisks (*) represent reference ages yielded by a group of less than fi ve but at least three pooled analyses in the Tera-Wasserburg diagram. Mineral abbreviations: Bt—biotite; Crd—Cordierite; Hbl—hornblende; Kfs—K-feldspar; Ms—muscovite; Opx—orthopyroxene; Qtz—quartz. MSWD of conc. and equiv.—Mean square of weighted deviation of combined concordance and equivalence.

Ng et al.


A1

A2

Figure 3 (on this and following page). (A1–A2) Representative cathodoluminescence (CL) images of extracted zircon grains from the Eastern province granitoids.



Eastern Province Permo-Triassic Granitoids in the Eastern Belt

Zircon grains extracted from granitic samples collected in the Eastern belt are mostly well-faceted prisms, exhibiting oscillatory zoning with CL-dark cores, although those extracted from the Kerteh dacite (sample MA54) are frag-mented and homogeneous (Fig. 3A). The CL-dark domains in such images typically reflect high U contents, as confirmed by the SIMS analyses (Table 2A). The age-yielding clusters generally have U contents ranging from 300 to 4000 ppm and Th/U ratios ranging from 0.11 to 1.14. Sample MA50 from Maras-Jong has much

higher U contents in the age-yielding zircon grains than other samples, ranging from 3700 to 7000 ppm, while the zircon grains extracted from the dacite sample (MA54) from Kerteh has much lower U contents, ranging from 180 to 380 ppm. Although both U contents and Th/U ratios vary over a large range between samples, they are quite consistent within each sample, add-ing a confidence to our interpretation of mag-matic ages from each pooled group of analyses. Exceptions are the Maras-Jong granite (MA50), the Jemaluang–Kluang granite (MA104), and the Ubin migmatitic granite (MA73). All of these samples have zircon grains that exhibit Pb loss, and their Th/U ratios vary even within sam-

ple. This reduced the pooled analyses available for age calculation, and hence, only reference magmatic ages could be calculated for these samples. Inherited zircon grains are identified with core ages recorded at 444.3, 467.7, and 1044.7 Ma (Figs. 4A and 5A).

The granitoids of the Eastern province are largely Permo-Triassic in age. The oldest gran-itoids were found in the Eastern belt. These samples have U-Pb ages ranging from 289.3 ± 2.4 to 231.0 ± 2.6 Ma (Fig. 2). The age data are summarized Table 3A. The oldest sample is the Maras-Jong K-feldspar–phyric (hornblende)-biotite granite (sample MA50). However, zir-con grains extracted from this sample exhibit a

B

Figure 3 (continued). (B) Representative CL images of extracted zircon grains from the Main Range province granitoids.

Ng et al.


serious post-magmatic Pb-loss problem. Omit-ting the analyses interpreted as showing Pb loss, a group of four analyses yield a reference con-cordia age of 289.3 ± 2.4 Ma. The oldest robust age is obtained from the Perhentian Island syenite (MA48). A group of thirteen analyses yields a magmatic age of 284.2 ± 1.6 Ma. The biotite granite (MA47) intruding the syenite has

an age of 257.6 ± 1.6 Ma. Other robust east-ern coast ages obtained from Terengganu and Pahang include 250.5 ± 1.7 Ma for the Kerteh K-feldspar–phyric dacite (MA54) and 270.0 ± 1.4 Ma for the Kuantan hornblende-biotite gran-ite (MA55). The hornblende-biotite granites in Kapal batholith (MA51) and Boundary Range (MA52) inland yielded robust concordia ages of

247.8 ± 1.7 Ma and 248.4 ± 1.8 Ma respectively, which are younger than the ages of the coastal samples. Only one robust age was obtained in the southern part of the Malay Peninsula, 238.5 ± 1.7 Ma from the K-feldspar phyric rhyolite collected at the Musoh River Mouth (MA76). The other two ages obtained are refer-ence ages of 244.5 ± 3.1 Ma for the Jemaluang–

A

C D

B

Figure 4. Tera-Wasserburg concordia diagrams for representative Malaysian granitoids. Tera-Wasserburg diagrams for all dated granitoids can be found in the Data Repository (see footnote 1). MSWD—mean square weighted deviation.



Kluang K-feldspar–phyric hornblende-biotite granite (MA104) and 231.0 ± 2.6 Ma for the Ubin Island migmatitic granite in Singapore (MA73). Zircon grains extracted from these two samples have suffered from serious Pb loss, which hindered the age interpretation. Most of the U-Pb zircon ages presented here agree with those obtained by Liew (1983) and Liew and McCulloch (1985).

Eastern Province Permo-Triassic Granitoids in the Central Belt

Similar to the zircon grains extracted from Eastern belt samples, the zircon grains extracted from the Central belt samples are mostly well-faceted oscillatory-zoned prisms, with either a CL-bright or a CL-dark core (Fig. 3A). Zircon grains extracted from Minyak Beku (sample MA66) and Batu Pahat (MA68 and MA69) samples generally have CL-dark cores, which indicate high U contents as shown in Table 2A. Zircon grains extracted from the Renyok sample (MA42, migmatitic tonalite) have metamor-phic overgrowths, which display growth zon-ing. The age-yielding clusters have U contents ranging from 270 to 4000 ppm and Th/U ratios ranging from 0.09 to 1.52. Generally, both U contents and Th/U ratios are consistent within samples. Exceptions are the Berengkat migma-titic tonalite collected from the Renyok River (MA42) and the Batu Pahat K-feldspar–phyric biotite granite (MA69). Both have zircon grains exhibiting Pb loss. In addition, zircon grains extracted from sample MA69 suffered from

matrix-induced U-Pb calibration caused by the presence of extremely high-U metamict zircon grains, which affects the accuracy of the ages. Metamorphic rims were found in the zircon grains extracted from the Berengkat migma-titic tonalite (MA42). No good rim ages have been calculated because of Pb loss, which is also a problem in inherited zircon grains found in samples MA36 and MA109. Most of the core data obtained from these grains are dis-cordant. Although these data are not useful in individual sample age analysis, they help define inheritance chords along with other discordant data obtained from other samples, which gives upper intercept ages at Cambro-Ordovician or Protero zoic times in the Tera-Wasserburg dia-gram (Fig. 5A).

The granitoids occurring in the Central belt of the Malay Peninsula have ages ranging from 231.8 ± 1.7 to 222.2 ± 1.8 Ma (Fig. 2). The age data are summarized in Table 3B. Robust U-Pb zircon ages were obtained from the K-feld-spar–phyric hornblende-biotite granite of the Jeli Blunero quarry (sample MA109, 226.7 ± 2.2 Ma), felsite of the Penjom gold mine (MA33, 222.4 ± 1.8 Ma), K-feldspar–phyric hornblende-biotite tonalite from Berengkat in the Stong region (MA36, 231.8 ± 1.7 Ma), clinopyroxene-hornblende-biotite granite from Minyak Beku (MA66, 222.2 ± 1.8 Ma), and K-feldspar–phyric biotite microgranite from Batu Pahat (MA68, 227.2 ± 1.9 Ma). The U-Pb zircon ages of the Eastern province Permo-Triassic granitoids get younger to the west. Reference ages only were obtained from samples MA42 and MA69 due to

the presence of zircon grains with Pb loss. For sample MA42, clusters of four analytical spots yield reference age at 220.4 ± 3.9 Ma. This refer-ence age is broadly consistent with the age of the other Berengkat sample collected at Kampong Jerek (MA36) and other robust ages obtained in the Central belt. It also confirms the tempo-ral relationship between the hosting tonalite and the Cretaceous Kenerong–Renyok leucogranitic dike (MA43). For the Batu Pahat K-feldspar–phyric biotite granite (MA69), a cluster of four pooled analyses yield a reference age at 225.5 ± 2.5 Ma. This age is consistent with that of sam-ple MA68 collected at the same locality, which has a robust age at 227.2 ± 1.9 Ma. Although field relationships suggested that the Batu Pahat biotite microgranite (MA68) cuts the coarser-grained granite (MA69), the age difference obtained is within the error bars of both ages, and so the two granitic bodies likely formed almost contemporaneously.

Eastern Province Cretaceous Granitoids

Granitoids cropping out in the Stong region (Kenerong and Noring) and Tioman Island are of Late Cretaceous age. Zircon grains extracted from a Kenerong leucogranitic dike (sample MA43) at Renyok are mainly multi-faceted prismatic metamorphic zircon crystals. They are homogeneous and unzoned. In contrast, grains from the Noring K-feldspar–phyric hornblende-biotite granite (MA45) are well-faceted oscilla-tory-zoned magmatic zircon grains. U contents of zircon grains from both Stong samples are

A B

Figure 5. Inherited zircon ages and likely inheritance chords yielded from (A) the Eastern Province and (B) the Main Range Province granitoids.

Ng et al.


high, ranging from 450 to 6600 ppm. The Tio-man zircon grains are well-faceted prisms (Fig. 3A). They are mainly homogeneous, unzoned to faintly oscillatory-zoned magmatic zircon grains. The zircon grains generally have lower U contents than those extracted from the peninsula samples. They generally have U contents <1000 ppm (Table 2B). However, the Th/U ratios of all of the Cretaceous zircon grains are variable, in the range of 0.36–4.05. They are generally higher than those of the Permo-Triassic gran-itoids. Older inherited zircon grains were also extracted from the Cretaceous samples. Most of them gave discordant data similar to those of the inherited zircon grains extracted from the Eastern belt. Although two of these grains give Carboniferous to Triassic concordant ages, no relevant petrologic or tectonic interpretation can be made.

Robust U-Pb zircon ages were obtained from the Kenerong leucogranitic dike (sample MA43) at 83.9 ± 0.8 Ma and the Noring K-feld-spar–phyric hornblende-biotite granite (MA45) at 75.7 ± 0.6 Ma. The granitic samples col-lected from different parts of the Tioman Island (MA78, MA90, MA91, MA97, and MA100) yield robust ages all near 80.0 ± 1.0 Ma, the same age as that reported by Searle et al. (2012) from Tioman Island (Table 3C).

Main Range Province Granitoids

Zircon grains extracted from the Main Range province granitoids are mostly well-faceted prismatic grains and are slightly bigger than those extracted from the Eastern province gran-itoids (Fig. 3B). Both CL-dark and CL-bright cores can be found in the grains with oscillatory zoning. Fragmented zircon grains are found in the volcanic sample collected from Genting Sempah (sample MA110). Zircon in the age-yielding groups generally have U contents rang-ing from 100 to 3000 ppm (Table 2C). Sample MA07 from Cameron Highlands has higher U contents in its age-yielding group, ranging between 1500 and 8500 ppm. The Th/U ratios in the age-yielding groups range from 0.04 to 1.35 and are similar to those in the Eastern province. In contrast to the Eastern province samples, the Main Range province samples have a relatively limited range of Th and U concentrations. Core-rim relationships were found in some of the extracted zircon grains in most of the samples. The core ages, if concordant, generally suggest Cambro-Ordovician or Neoproterozoic upper intercept ages in the Tera-Wasserburg diagrams (Fig. 5B).

Fifteen samples were dated in the Main Range province. The U-Pb zircon ages range from 226.2 ± 1.2 to 200.8 ± 2.0 Ma (Fig. 2).

The oldest samples with robust ages were found inland, i.e., from the Cameron Highlands (sam-ple MA07, 219.4 ± 1.5 Ma; MA13, 225.4 ± 1.3 Ma; MA14, 218.3 ± 2.4 Ma), Ipoh (MA15, 220.1 ± 1.0 Ma), Kuala Lumpur (MA31, 222.4 ± 1.8 Ma), and Bukit Mor (MA62, 217.4 ± 1.2 Ma). All of these ages were obtained from K-feldspar–phyric (muscovite)-biotite granites. Younger samples were found on the western coast and outlying islands like Penang (MA23, 212.1 ± 2.4 Ma) and Langkawi (MA26, 215.3 ± 2.6 Ma; MA30, 215.9 ± 1.7 Ma). The only horn-blende-bearing granite in the Main Range prov-ince, the Taiping granite (MA16) of the Bintang batholith, also gives a robust age of 215.7 ± 1.6 Ma. Hence, it formed at the same time as the hornblende-free Main Range granitoids. Reference ages are provided when the zircon grains suffered from serious Pb loss. These ages are given to the Cameron Highlands K-feld-spar–phyric cordierite-biotite granite (MA06, 220.1 ± 2.8 Ma), the Penang K-feldspar–phyric biotite granites (MA19, 213.9 ± 2.9 Ma; MA20, 215.5 ± 1.5 Ma), and the Tuba muscovite-biotite microgranite (MA29, 200.8 ± 2.0 Ma). The reference ages provided are comparable to the robust ages obtained in nearby samples. All of these ages are reported in Table 3D.

Westward-Younging Ages of the Malaysian Granitoids

The westward-younging trend observed in age data from the Eastern province also follows in the Main Range province (Figs. 2 and 6). The Eastern province granitoids have U-Pb ages ranging from 289 Ma to 220 Ma (Eastern belt, 289–231 Ma; Central belt, 226–220 Ma). The Main Range province granitoids have U-Pb ages ranging from 226 Ma to 201 Ma. However, it is also observed that the conceptual 220 Ma and 210 Ma isolines in the Main Range prov-ince are close to each other, and they are not as well defined as isolines in the Eastern province (Fig. 6). The Genting Sempah volcanics have been correlated with the Main Range magma-tism due to their similar geochemistry (Ghani and Singh, 2002, 2005; Ng et al., 2015). The orthopyroxene-bearing dacite (sample MA110) was dated at 226.2 ± 1.2 Ma (2s, MSWD of con-cordance and equivalence = 1.30), which pro-vides temporal evidence for such a conclusion.

U and Th Contents and Th/U Ratios of Zircon in Malaysian Granitoids

Compared to the common U and Th contents of zircon in granitic rocks (median values 350 ppm of U and 140 ppm of Th, n = 1684) (Wang et al., 2011), the zircon grains in the Malaysian

granitoids are generally more enriched in U and Th than typical granitoids. The U contents can be ten times those values in normal zircon grains extracted from granitoids. Zircon grains with U contents of thousands of parts per million are common in the Malaysian granitoids (Table 2). Radiation damage to the crystal lattice enhances Pb mobility rates, which can explain the ubqui-tious Pb-loss problem in these samples. The U and Th geochemistry does however suggest a subtle difference in the source region and/or petro genesis of the different sample groups. Com-pared to the Permo-Triassic Malaysian granitoids (Th/U ratios ranges from 0.2 to 1.2, with average Th/U = 0.5), the Cretaceous plutons generally have higher Th/U ratios, ranging from 0.5 to 2.5, and average Th/U = 1.3 (Fig. 7). Because the U and Th contents of the zircon grains are primarily controlled by the U and Th contents of the melt, the difference observed here may be attributed to the compositional difference of the sources. The additional heat required to explain to explain the Main Range granitoids may have been derived from internal heat production as evidenced by the high-U zircon grains.

DISCUSSION

U-Pb Ages of the Eastern Malay Province and Temporal Constraints on the Closure of the Paleo-Tethys Ocean

Our new U-Pb age data support the earlier contention that the Eastern province granitoids were formed in an Andean-type setting along the western margin of Indochina above an east-dipping subduction zone during the Early Permian to Mid to Late Triassic (Mitchell, 1977; Cobbing et al., 1986, 1992). Our new U-Pb zir-con ages generally agree with zircon ages from previous workers in the Malay Eastern province (Liew, 1983; Liew and McCulloch, 1985; Liew and Page, 1985; Searle et al., 2012). Our data also agree with the U-Pb zircon ages of gabbros from Singapore Island of 260 ± 2 Ma to 249 ± 2 Ma, and of granites of 249 ± 2 Ma to 230 ± 6 Ma also on Singapore Island, published by Oliver et al. (2014).

Our U-Pb zircon ages from the dominantly hornblende- and biotite-bearing monzogranites of the Eastern province span the period 289–220 Ma, which we interpret to reflect the timing of active subduction and Andean-type magma-tism. The “Central belt” of Chu et al. (1988) and Hutchison and Tan (2009) contains plutons that have a similar chemistry to those of the East-ern belt (Ghani, 2009), so we envisage both as being part of the same Indochina terrane. The intervening Lebir fault is a later structure that truncates the granites but has limited offsets.



104°°301°201°101°00199°E

104°

1°

6°

5°

4°

3°

2°

7°N

1°

6°

5°

4°

3°

2°

7°N

°301°201°101°00199°E

Bentong-Raub suture zone


Alkali granitoids


50 km0

THAILAND

Main Range batholith Benom

Kapal batholith

Kuantan

Kota Baharu

Perhentian

Redang

Boundary Range batholith

Bentong-Raubsuture

Tioman

LangkawiIs. Pulau

Tuba

KohTarutao

Singapore

Kuala Lumpur

Malacca

Johor Bharu

Kinta Valley

PenangNoringStong

Ipoh

BukitTinggi

KledangBubu

Kulim

Selama

JerongMaras-Jong

Gul f ofThai land

Strai ts o f M

elacca

Sibu

N

250 Ma

260 Ma

230 Ma

220 Ma

210 Ma

(d) - Granitic dyke(da) - Dacite(di) - Diorite(l) - Leucogranite(r) - Rhyolite(s) - Syenite

1 - Liew, 1983; Liew and Page, 19852 - Liew, 1983; Liew and McCulloch, 19853 - Searle et al., 20124 - Oliver et al., 20145 - This work

*220 ± 4 Ma (d)5

84 ± 1 Ma (l)5

258 ± 2 Ma5

284 ± 2 Ma (s)5

*289 ± 2 Ma5

248 ± 2 Ma5

232 ± 1 Ma5

248 ± 2 Ma5

227 ± 2 Ma2

250 ± 2 Ma (da)5

267 ± 2 Ma2

270 ± 1 Ma5222 ± 2 Ma (d)6

80 ± 1 Ma3

80 ± 1 Ma5

80 ± 1 Ma5

80 ± 1 Ma (d)5

82 ± 1 Ma (di)5

81 ± 1 Ma (mg)5

237 ± 1 Ma4

244 ± 2 Ma4

238 ± 2 Ma (r)4

230 ± 6 Ma4

*231 ± 3 Ma5

222 ± 2 Ma5

227 ± 2 Ma5

*226 ± 3 Ma5

238 ± 2 Ma4

239 ± 2 Ma (r)5

*244.5 ±3.1 Ma5

226 ± 1 Ma5

76 ± 1 Ma5

285 ± 5 Ma4

276 ± 5 Ma4

257 ± 4 Ma2

215 ± 3 Ma5

216 ± 2 Ma5

209 ± 1 Ma1

215 ± 6 Ma1

214 ± 3 Ma5

216 ± 2 Ma5

212 ± 2 Ma5

216 ± 2 Ma5

220 ± 1 Ma5220 ± 3 Ma5

219 ± 2 Ma5

225 ± 1 Ma5

218 ± 2 Ma5

209 ± 2 Ma1

206 ± 2 Ma1

198 ± 2 Ma1

219 ± 9 Ma1

215 ± 2 Ma1

215 ± 7 Ma3

210 ± 7 Ma3

222 ± 2 Ma5

201 ± 2 Ma5

226 ± 1 Ma (d)5

217 ± 1 Ma5

Figure 6. Chronological isolines drawn according to the U-Pb zircon ages presented in this paper.

Ng et al.


Although the Bentong-Raub suture zone contains only serpentinites, deep-sea radio-larian cherts, and sedimentary rocks spanning Middle Devonian (ca. 390 Ma) to Late Permian age (ca. 250 Ma) (Metcalfe, 2000; Sevastjanova et al., 2011), the Paleo-Tethyan main suture in Thailand (Changning-Menglian suture zone, Inthanon suture zone, and the Klaeng tectonic line) contains marine sediments as young as mid-Triassic (ca. 230 Ma) (Sone and Metcalfe, 2008; Sone et al., 2012). The youngest marine sedimentary rocks in the suture zone correspond roughly to the youngest I-type subduction-related granite ages from the Eastern province, and thus we interpret these data to imply closure of Paleo-Tethys along the Bentong-Raub suture zone between 230 and 220 Ma. Continental red-bed clastic sediments overlie older marine sedi-ments both along the suture zone and across the Indochina terrane (Sone et al., 2012). In Singa-pore, Oliver and Prave (2013) demonstrated the change to continental sedimentation during the Late Triassic.

Earlier Paleo-Tethyan closure times have been suggested by Metcalfe (2000, 2003, 2009) and Barber and Crow (2009). These authors proposed that the Sibumasu–Indochina (East Malaya) collision could have occurred as early as Late Permian. Their arguments are based on the fact that no Triassic radiolarian cherts were found along the Bentong-Raub suture zone in the Malay Peninsula, but only in the Semanggol Formation on the western coast. They inter-preted the Triassic radiolarian cherts there as successor-basin deposits, rather than Paleo-Tethyan deposits (Metcalfe, 2000, 2009; Bar-ber and Crow, 2009; Sevastjanova et al., 2011), because there is a major unconformity separat-

ing the uppermost Permian and the lower most Triassic in the Malay Peninsula and Sumatra, which could represent the collision (Metcalfe, 2000, 2009; Barber and Crow, 2009). The idea of “early collision” does not agree with the interpretation made by previous authors (Sashida et al., 1995, 2000a, 2000b; Sashida and Igo, 1999; Kamata et al., 2002; Hirsch et al., 2006; Ishida et al., 2006; Ueno et al., 2006), who suggested that the Semanggol sediments were related to Paleo-Tethys. A recent paper by Kamata et al. (2014) further suggested that the Permo-Triassic deep-water succession in southern Thailand, which is partly equivalent to the Semanggol Formation in the Malay Penin-sula, was formed on the Sibumasu continental slope, while no unconformity is found between Permian and Triassic. In addition, no regional unconformity in the Eastern province could be linked to supposed Indosinian orogeny near the Permo-Triassic boundary (Lee, 2009). Hence, in this paper, we infer that the Sibumasu–Indo-china (East Malaya) collision and closure of the Bentong-Raub suture occurred in the Late Trias-sic at ca. 230 Ma.

These data can now be used to determine a suitable tectonic model for the evolution of the Malay granite provinces. Two main tectonic models have been proposed which are discussed individually below.

Tectonic Model A—Two East-Dipping Subduction Zones

The model generally accepted for the evo-lution of the Malay granite provinces (Met-calfe, 2000, 2011; Barber and Crow, 2003; Sone and Metcalfe, 2008; Barber et al., 2011; Searle et al., 2012) involves eastward subduc-tion of Paleo-Tethyan lithosphere along the Paleo-Tethyan Bentong-Raub ocean, resulting in subduction-related, Andean I-type granite intrusions along the upper plate (Indochina) in the Eastern province (Fig. 8). Our U-Pb age data show this age range to be Early Permian to Middle to Late Triassic (ca. 289–220 Ma). Following closure of the Paleo-Tethys Ben-tong-Raub Ocean and continental collision of Sibumasu and Indochina, oceanic subduc-tion ceased, I-type magmatism ended soon after, and magmatism started in the Main Range province (Sibumasu) where volumi-nous crustal-melt granites were intruded, forming the Main Range batholith during the Late Triassic. Our U-Pb zircon ages suggest a fairly restricted period of intrusion of these granites, spanning 227–201 Ma (Fig. 8). This model is consistent with the well-known tec-tonic evolution of the Himalaya-Tibet collision where earlier, pre-collision (ca. 180–50 Ma)

I-type granites (Gangdese-Ladakh granites) and calc-alkaline volcanics (Linzizong Group) occur on the Asian plate above a northward-dipping oceanic subduction zone, and later (ca. 26–19 Ma), post-collision S-type leucogranites occur along the Indian plate south of the suture zone (Fig. 9). The major difference with the Himalaya is that the Main Range granites of western Malaysia are of much larger extent, are of batholithic proportions, are not directly con-nected to a regional sillimanite-grade migma-tite terrane, and are tin-bearing.

Searle et al. (2012) suggested that a second east-dipping subduction zone was required west of the Sibumasu Main Range province in order to explain another belt of subduction-related I-type granites extending from western Phuket Island along western Thailand and southeast-ern Burma (Fig. 8). Cobbing et al. (1986, 1992) referred to this zone as the Western province composed of large batholiths of S-type tin-bearing granites and smaller I-type plutons. However, most of the granitoids along the west coast of Phuket Island are hornblende- and bio-tite-bearing diorites, monzogranites, and gran-ites that continue north along the Mergui coast of south Burma. In Burma they are dominantly either tin-bearing Main Range transitional I/S types or fractionated I-type granites, but appear to be much younger with Cretaceous ages (Bar-ley and Zaw, 2009; Gardiner et al., 2014).

A lack of zircon age data in this region pre-cludes any detailed tectonic correlations, but in the Mogok belt of Burma, subduction-related I-type diorites and granodiorites have U-Pb ages spanning the Jurassic to mid-Cretaceous (Barley et al., 2003; Mitchell et al., 2012). However, Searle et al. (2012) provided new U-Pb zircon core ages of 212 ± 2 and 214 ± 2 Ma for the Phuket granite, while Late Triassic zircon xenocrysts (209 ± 4 Ma) were reported previously in the Kyanigan gneiss further north in Mandalay of Burma by Barley et al. (2003). More detailed U-Pb zircon age constraints are needed along this belt in order to constrain the tectonic evolution of Neo-Tethyan closure along this part of the India-Burma-Sibumasu collision zone. Although the evidence lies mostly north of Malaysia in Thailand and Burma, the pres-ence of Late Triassic Andean I-type granites, dacites, and calc-alkaline volcanics along the Thai-Burmese border would seem to require a second east-dipping subduction zone to the west of Sibumasu. It is possible that once the Paleo-Tethyan subduction zone ceased along the Bentong-Raub suture zone during the Late Triassic, the Neo-Tethyan subduction zone ini-tiated to the west of Sibumasu, but until more age data become available, this model remains speculative.

Figure 7. Average Th concentration of the age-yielding group of each sample plotted against the average U concentration. It is shown that the Cretaceous granitoids gener-ally have higher Th/U ratios.



Tectonic Model B—Westward Underthrusting of Sibumasu by Indochina

An alternative tectonic model was proposed by Oliver et al. (2014) who demonstrated a progressive decrease in age of subduction-

related gabbros, granitoids, and rhyolites from east to west, from Sibu Island (with 285 Ma early magmatic zircon) off the southeastern coast of Malaysia to Singapore (Ketam gran-ite, 230 ± 6 Ma). Based on limited sampling, they suggested that the subduction zone steep-

ened and progressively rolled back, resulting in stretching of the lithosphere and a westward-migrating magmatic front (Fig. 10). Our new U-Pb zircon age data support this model with 15 new zircon ages across the Eastern province also showing a pronounced westward decrease

PALAEO-TETHYSBentong-Raub[Devonian - Mid-Triassic]


W E

Shallow dipping subduction zone

A. Early Permian to Middle Triassic 290–245 Ma

Perhentian syenite

245–290 Ma

SIBUMASUShallow marine strata since Cambrian

INDOCHINA - EAST MALAYAShallow marine strata,

volcanics since Devonian

Basalticunderplating

NEO-TETHYSMain Range Province granitoids

Bentong-Raub


Steeper dipping subduction zoneSlab roll-back

B. Middle to Late Triassic 245–220 Ma

Benom syenite Perhentian syenite245–290 Ma220–245 Ma


220–226 Ma





Stong Berengkat Granite

Slab pull

Block compression and thickening

C. Late Triassic to Early Jurassic 220–200 Ma

NEO-TETHYS Bentong-Raub sutureEastern Province granitoids

Benom syenite Perhentian syenite

220–245 Ma 245–290 Ma





200–220 Ma

Block compression and thickening


Figure 8. Tectonic model explaining the formation and the emplacement of the Malaysian tin-bearing granites, modified after Searle et al. (2012).

Ng et al.


in ages (Fig. 10). Oliver et al. (2014) further suggested that following collision, the Main Range province (Sibumasu) was thrust over the Indochina province along the Bentong-Raub suture zone, resulting in partial melting of thickened crust in Sibumasu and intrusion of S-type tin granites along the Main Ranges of western Malaysia.

This model is also not without its problems. First, the Sukhothai arc terrane does not extend to the Malay Peninsula, as discussed previ-ously. Second, there is no geological evidence for westward underthrusting of the Main Range province over the Eastern province. In fact, structural and geophysical evidence showed the other way round in Thailand (Morley et al., 2011; Milsom, 2011); third, the source for the Main Range transitional I/S-type granitoids is unlikely to be the underthrust Eastern prov-ince hornblende-bearing I-type granitoids; and third, the main transitional I/S-type tin-bearing granites are in the western Sibumasu in west-ern Malaysia (Kinta valley and west coast), and are not restricted to the eastern part of the Main Range province as shown on Oliver et al.’s model (2014) (Fig. 10). Ghani et al. (2013b) and Ng et al. (2015) showed that the Main Range granites were fractionated transitional I/S types with many characteristics typical of S types (ele-vated 87Sr/86Sr ratios > 0.710, presence of ilmen-ite and occasional cordierite and andalusite, and

v vv v

S N

IND

US

-TS

AN

GP

O S

UTU

RE

ZO

NE

INDIAN PLATE ASIAN PLATE

ASIANPLATE

INDIANPLATEIndian Shield lower crust

Miocene partial melt middle crust

sillimanitegneiss

STDMCTMBT

Greater Himalaya SeriesPost-collision S-typeleucogranites + + + (25–14 Ma)in regional migmatites

Lhasa BlockPre-collision I-typeGangdese-Ladakh granites x x x (ca. 180–47 Ma)+ calc-alkaline volcanics v v v

50 k

m

50 km

STD - South Tibetan DetachmentMCT - Main Central ThrustMBT - Main Boundary Thrust

Figure 9. Schematic cross-section showing the Indo-Asian collision in the Miocene, edited after Searle et al. (2009, 2011). Ages are provided by Chiu et al. (2009) and Chu et al. (2006).

B Early to Middle Triassic 250–230 Ma

Moho

Singaporegabbro + granites

Pengerang Volcano 238 Ma (1)

Passive margin

260–230 Ma(1)

melts

Accretionaryprism

C Late Triassic 230–200 Ma Moho

Tin-bearing lower

S-type tin-granites

Indosinian Orogeny

Neo-Tethys Jurong Fm

CentralEastern Belt

(285)(2)(250)(2)(235)(2) (245)(1)(215)(2)(205)(2)

219–198 Ma (3)

Modal detrital zircon ages Belt

in brackets

W. Belt

crustal melts

I-type

tin-granites

A Permian 290–250 Ma

Vertical scale = 25 km

Horiz scale = 100 km Mantle

Palaeo Tethys

3,500 km wide Magmatic arc

Sibu285–276 Ma(1)

Andean-typemargin

264 Ma(3)Sibumasu

Figure 10. Tectonic model proposed by Oliver et al. (2014), suggesting underthrusting of the Central belt (western part of the Indochina terrane) beneath the Sibumasu terrane to account for the Main Range magmatism. Ages of the granitoids are denoted in parentheses. Ages are provided by (1) Oliver et al. (2014), (2) Sevastjanova et al. (2011), and (3) Liew and McCulloch (1985).



presence of metasedimentary enclaves), but also some characteristics of I types (presence of sphene and amphibole, meta-igneous enclaves). These granitoids are more likely to have been sourced by a metasedimentary lower crust than

a hornblende-biotite granodiorite-granite as required in the Oliver et al. (2014) model.

A study of U-Pb detrital zircon ages in mod-ern rivers across Malaysia by Sevastjanova et al. (2011) concluded that it was not possible to

distinguish between Eastern province and Main Range province basement rocks, both of which have a common Proterozoic (or possibly Neo-archean) age. Although detrital zircon ages and particularly zircon Hf isotopes can potentially

100.5

~145.0

163.5 ±1.0

174.1±1.0

201.3 ±0.2

~237

247.2252.17 ±0.06

259.8 ±0.4

272.3 ±0.5

298.9 ±0.15

100

110

300

120

130

140

150

160

170

180

190

200

210

220

230

240

250

260

270

280

290

90

80

Lower

Upper

Middle

Lower

Upper

Middle

Lower

Lopingian

Guadalupian

Cisuralian

UpperP

erm

ian

Tria

ssic

Jura

ssic

Cre

tace

ous

Period Epoch (Ma) Main Range ProvinceSibumasu Block

B-RSuture

Eastern ProvinceEast Malaya Block

Rad

iola

rian

cher

ts -

Pal

aeo-

Teth

yan

sutu

re(S

one

and

Met

calfe

, 200

8)

Basaltic dykes of the Eastern Province(Ghani et al., 2013a)

Mar

as-J

ong

Kua

ntan

Per

hent

ian

Isla

nd

Kap

al R

ange

Bou

ndar

y R

ange

Ker

teh

(dac

ite)

Jem

alua

ne -

Klu

ang

Mus

oh R

iver

Mou

th (r

hyol

ite)

Sin

gapo

re -

Ubi

n Is

land

Ber

engk

at -

Kam

pong

Jer

ek

Bat

u P

ahat

Jeli

- Blu

nero

Qua

rry

Ber

engk

at -

Ken

eron

g

Pen

jom

Gol

d M

ine

(fels

ite)

Min

yak

Bek

u

Sin

gapo

re -

Ket

am (O

liver

et a

l., 2

014)

Perhentian Island(syenite)

Cam

eron

Hig

hlan

dsC

amer

on H

ighl

ands

Buk

it M

orG

entin

g S

empa

h (d

acite

)K

uala

Lum

pur1

Cam

eron

Hig

hlan

dsC

amer

on H

ighl

ands

IpohTa

ipin

gP

enan

g Is

land

Pen

ang

Isla

ndP

enan

g Is

land

Lang

kaw

i Isl

and

Lang

kaw

i Isl

and

Tuba

Isla

nd

1 The U-Pb zircon ages of 215 ±7 Maand 210 ±7 Ma were given by Searleet al., (2012)

Tiom

an Is

land

(5 s

ampl

es +

1 s

ampl

e fro

m S

earle

et a

l., 2

012)

Nor

ing

Ken

eron

g - R

enyo

k R

iver

Sin

gapo

re -

Ubi

n Is

land

(dio

rite)

(Oliv

er e

t al.,

201

1)

The chart follows the International Chronostratigraphic Chart v 2014/02

Figure 11. Summary of ages obtained from the Malaysian granitoids. B-R—Bentong-Raub.

Ng et al.


provide good indicators of provenance, the Hf results from the Main Range province are essen-tially inconclusive.

CONCLUSION

We present new high-precision U-Pb zircon ion microprobe ages for 39 granitoids across the Malay tin-bearing granite province in Malaysia. Hornblende- and biotite-bearing, mostly I-type granitoids from the Eastern Malay province span 289–220 Ma and are interpreted as sub-duction-related Andean-type magmas formed during eastward subduction of Paleo-Tethys beneath the Indochina active plate margin dur-ing the Permian to Middle-Late Triassic. Source rocks included Mesoproterozoic and Cambro-Ordovician crust. A general westerly younging trend across the Malay Peninsula could reflect steepening and roll-back of the Bentong-Raub subduction zone during progressive closure of Paleo-Tethys (Fig. 11). Closure of Paleo-Tethys and collision of Sibumasu with Indochina closed the Bentong-Raub suture zone and shut off subduction-related Andean-type magmatism at 230–220 Ma. Following collision, crustal thickening in the Sibumasu plate resulted in extensive tin-bearing crustal melt granitoids intruded along the Main Range batholith over a fairly restricted Late Triassic time range, span-ning 227–201 Ma (Fig. 11).

Our preferred tectonic model to explain the progressive closure of Paleo-Tethys and the change in magmatism from Early Permian to Middle-Late Triassic subduction-related granit-oids to later Late Triassic continental-collision magmatism along the Main Range is discussed below. From the Early Permian to the Middle Triassic (290–245 Ma), the eastward Paleo-Tethyan subduction along the Bentong-Raub suture zone led to the partial melting of the overriding Indochina–East Malaya basement. This basement is postulated to be composed of Cambro-Ordovician metabasalt, which is iso-topically similar to the Kontum orthoamphibo-lites, and a subordinate amount of Mesoprotero-zoic metapelite, which is isotopically similar to the Kontum paragneisses in Vietnam, one of the nearest exposures of granulite-amphibolite facies lower crust. This is supported by the iso-topic data of the Malaysian granitoids as shown in Part 1 of this study (Ng et al., 2015) and inherited zircon grains ages of the Eastern prov-ince granitoids presented in this paper. Melting of this enriched metabasalt with heat and water supplied by the Bentong-Raub subduction could have produced large amounts of metalu-minous to weakly peraluminous melt with an enriched HFSE signature, which in turn could have formed the Eastern province granitoids.

Isotopic data presented in Part 1 suggest that, as the melts rose to form the plutons, up to 20% of crustal components were incorporated due to partial melting of metasedimentary basement and crustal assimilation (Ng et al., 2015). Less-fractionated melts produced the alkali granitoids exposed on Perhentian Island and in Benom. As the subduction zone steepened and the subduct-ing plate started to roll back, the lithosphere became stretched and magmatism propagated westward with time.

From the Middle Triassic to the Late Triassic (245–220 Ma), the Eastern province magmatism gradually moved to the central part of the pres-ent Malay Peninsula. During the Late Triassic, collision of Sibumasu with Indochina closed the Paleo-Tethyan Ocean along the Bentong-Raub suture zone. Crustal thickening ensued along the Sibumasu terrane where Late Triassic granites were intruded along the Main Range batholith. These granites are the main host of the exten-sive tin mineralization in Malaysia, although some tin mineralization is also present in the Eastern province. The Main Range granitoids are extremely voluminous, and their geochem-istry and isotopic composition suggest that they formed in a supra-subduction zone setting rather than a Himalayan-type setting. No regional meta morphic-migmatite terrane is associated with the Main Range granitoids.

Closing of Paleo-Tethys may have resulted in initiation of a new east-dipping Neo-Tethyan subduction zone at ca. 230 Ma to the west of the Malay Peninsula and Thailand, extend-ing north to the Mogok area of Burma (Searle et al., 2012). Fluids driven off this subduction zone could have triggered partial melting of thickened Sibumasu crust, and also driven tin mineralization. The basement of the Sibumasu terrane appears to be compositionally and tem-porally similar to that of the East Malaya prov-ince, with Cambrian-Ordovician metabasalt and Meso protero zoic metapelite, both are isotopi-cally similar to the Kontum massif correspond-ing units. However, metasedimentary compo-nents dominated the source region for the Upper Triassic Main Ranges granitoids in contrast to the Eastern province. This produced the Main Range province granitoids with an enriched HFSE signature, but that are more fractionated than those of the Eastern province (Ng et al., 2015). The Sibumasu terrane has much thicker crust (up to 13 km thicker) than the East Malaya terrane (Ghani et al., 2013a); up to 40% crustal sources were incorporated into melts due to par-tial melting of metasedimentary basement and crustal assimilation (Ng et al., 2015).

During Late Cretaceous time (95–80 Ma), localized thermal events of unknown origin caused the restricted Cretaceous magmatism

on the Indochina–East Malaya terrane. These Cretaceous granitoids exposed in the Stong area (Noring pluton) and on Tioman Island (Searle et al., 2012; this paper) and Ubin Island (Oliver et al., 2011) appear to be only localized thermal events of unknown origin. However, trace ele-ment geochemistry suggested that these Creta-ceous granitoids have lower Y/Nb ratios com-pared to the Permian-Triassic granitoids, which put them into the A1-type geochemical field in Eby’s (1992) diagram (Ng et al., 2015). The extracted zircon grains from these Cretaceous granitoids also show higher Th/U ratios than the Permo-Triassic Malaysian granitoids. More detailed U-Pb zircon dating of granitoids along the Southeast Asian tin-bearing granite province is needed in order to test these tectonic models in greater detail.

ACKNOWLEDGMENTS

This paper is dedicated to the memory of Charles Hutchison, who sadly passed away in October 2011. Azman Ghani and Masatoshi Sone acknowl-edge University of Malaya High Impact Research Grants (UM.C/HIR/MOHE/SC/27 and UM.C/625/1/HIR/140 respectively) for supports during fieldwork. WYNG Foundation (Hong Kong) and Raphael Mar-tin of Dark Capital Group are also gratefully acknowl-edged for funding support. The Penjom gold mine (J. Resources) is also acknowledged for permission to collect samples in the mine. The NordSIM facility at the Swedish Museum of Natural History is oper-ated under an agreement between the research funding agencies of Denmark, Iceland, Norway, and Sweden, the Geological Survey of Finland, and the Swedish Museum of Natural History. K. Lindén and L. Ilyinsky are also acknowledged here for their technical sup-port. The Batu Pahat Hanson quarry, Bukit Batupejal quarry, and the Jeli Blunero quarry are thanked for ap-proving and guiding our visit and sampling. We would also like to thank C.K. Morley and A.J. Barber for re-viewing this article.

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