Gondwana Research 19 (2011) 1024–1039

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Granitic magmatism, basement ages, and provenance indicators in the Malay Peninsula: Insights from detrital zircon U–Pb and Hf-isotope data

Inga Sevastjanova a,⁎, Benjamin Clements a,b, Robert Hall a, Elena A. Belousova c, William L. Griffin c, Norman Pearson c a Southeast Asia Research Group, Department of Earth Sciences, Royal Holloway University of London, Egham Hill, TW20 0EX, UK b Statoil ASA, Forusbeen 50, N-4033 Stavanger, Norway c GEMOC ARC National Key Centre, Department of Earth and Planetary Sciences, Macquarie University, Sydney, NSW 2109, Australia article info abstract

Article history: The Malay Peninsula lies on two continental blocks, Sibumasu and East Malaya, which are intruded by Received 20 May 2010 granitoids in two provinces: the Main Range and Eastern. Previous models propose that Permian–Triassic Received in revised form 30 September 2010 granitoids are subduction-related and syn-to post-collisional. We present 752 U–Pb analyses that were Accepted 1 October 2010 carried out on zircons from river sands in the Malay Peninsula; of these, 243 grains were selected for Hf- Available online 11 November 2010 176 177 isotope analyses. Our data suggest a more complex Sibumasu–East Malaya collision history. Hf/ Hfi ratios – Editor: M. Santosh reveal that Permian Triassic zircons were sourced from three magmatic suites: (a) Permian crustally-derived granitoids, (b) Early-Middle Triassic granitoids with mixed mantle–crust sources, and (c) Late Triassic Keywords: crustally-derived granitoids. This suggests three Permian–Triassic episodes of magmatism in the Malay Sundaland Peninsula, two of which occurred in the Eastern Province. Although the exact timing of the Sibumasu–East Malay Peninsula Malaya collision remains unresolved, current data suggest that it occurred before the Late Triassic, probably in Basement Late Permian–Early Triassic. Our data also indicate that Sibumasu and East Malaya basements are Detrital zircon chronologically heterogeneous, but predominantly of Proterozoic age. Some basement may be Neoarchaean – U Pb ages but there is no evidence for basement older than 2.8 Ga. Finally, we show that Hf-isotope signatures of Triassic Hf-isotope dating zircons can be used as provenance indicators. © 2010 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction Griffin et al., 2004, 2006a; Murgulov et al., 2007) as well as for other parts of the world (e.g. Bahlburg et al., 2010; Bodet and Schärer, SE Asia is a composite region of continental crustal fragments and 2000; Kuznetsov et al., 2010; Matteini et al., 2010), and have also volcanic arcs, separated by sutures that represent remnant ocean aided provenance interpretations (e.g. Belousova et al., 2009; basins (e.g. Metcalfe, 2006, 2010). These continental fragments are Howard et al., 2009; Veevers et al., 2006). However, there are no allochthonous to the Eurasian margin and separated from Gondwana Hf-isotope studies for the Sundaland region and few studies have in the Palaeozoic and Mesozoic (Audley-Charles, 1988; Metcalfe, addressed the age and nature of the basement fragments in the 1988, 1996a,b). Palaeogeographic reconstructions show that these region. This is the first study to apply zircon U-Pb dating and Hf- fragments arrived from NW Australia and NE Greater India (Hall, isotope analyses to Sundaland. 2008; Hall et al., 2009; Metcalfe, 1988, 1996b, 2009). In this paper we discuss U–Pb and Hf-isotope data in detrital In the SE Asian region, U–Pb detrital zircon geochronology has zircons from modern rivers draining the Malay Peninsula. Current been successfully used for tracing sediment pathways (Clements and data suggest a complex multi-phase evolution of the volcanic arcs that Hall, 2008; van Hattum, 2005; van Hattum et al., 2006), dating large developed in the Permian and Triassic on the western margin of SE Cenozoic eruptions (Smyth et al., 2008), and identifying fragments of Asia as a result of predominantly east-directed Palaeo-Tethys unexposed basement (Smyth et al., 2007). Studies of Hf-isotope subduction. Crustal model ages reveal that the basement beneath compositions in detrital zircons have resulted in detailed crustal the East Malaya and Sibumasu Blocks (Fig. 1) is Palaeoproterozoic, evolution models for parts of Australia (Belousova et al., 2006; although of different age, and with probable Neoarchaean crust also present. The Sundaland basement is intruded by abundant Permian– Triassic, Jurassic, and Cretaceous granitoids. A significant overlap in U–Pb zircon ages from different Sundaland source areas makes provenance interpretations difficult. However, the different Hf- ⁎ Corresponding author. Tel.: +44 1784 443592; fax: +44 1784 434716. isotope compositions enable distinctions to be made between granitic E-mail address: [email protected] (I. Sevastjanova). provinces of similar age.

1342-937X/$ – see front matter © 2010 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved. doi:10.1016/j.gr.2010.10.010 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1025

Fig. 1. Principal basement features (after Hall, 2008; Metcalfe, 2009) and potential sources of granitoid detrital zircons (after Cobbing, 2005; Cobbing et al., 1992; Thuy et al., 2004; Williams et al., 1988) in Sundaland. Dashed line shows the approximate boundary of Sundaland.

2. Geological setting continental blocks that form Sundaland occurred during the Late Palaeozoic and Mesozoic as a result of separation of continental slivers 2.1. Sundaland from the Gondwana margin and successive opening and closure of Tethyan oceanic basins (e.g. Metcalfe, 1996b, 1998, 2009). Palaeozoic Sundaland, the continental core of SE Asia (Hall, 2002; Hamilton, and Mesozoic reconstructions are based on multidisciplinary evidence 1979; Hutchison, 1989), comprises Indochina, the Thai–Malay that includes palaeomagnetism, lithofacies correlations, faunal pro- Peninsula, Sumatra, Java, Borneo and the shallow shelf between vinces, magmatic episodes, and dating of tectonic events. These data these landmasses (e.g. Hall and Morley, 2004). Amalgamation of the are complex and difficult to interpret, especially with regard to the 1026 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039

Tethyan oceans, which have been destroyed by subuction (Hall et al., 1995). This is supported by general tectonostratigraphical similarities 2009). However, despite disagreements on the exact origin of the between Sibumasu and the Canning Basin of NW Australia (e.g. blocks, the timing of their departures and arrivals, it is now accepted Metcalfe, 1996b, 2000). In East Malaya, only Ordovician and Silurian that the core of Sundaland comprises the Indochina–East Malaya, but not younger faunas show Gondwanan affinities. It has therefore West Burma, and West Sumatra Blocks that separated from been suggested that East Malaya separated from Gondwana in the Gondwana in the Devonian and together formed a composite Devonian (e.g. Metcalfe, 2000). Sibumasu and East Malaya are Cathaysia Block in the Permian (Barber and Crow, 2009; Metcalfe, separated by the Bentong–Raub Suture Zone, which includes a 2006, 2009). The Sundaland core also includes Sibumasu, which was tectonic mélange with ribbon-bedded cherts, schists, and minor accreted to Indochina–East Malaya, most likely in the Late Permian– ophiolites that represent Palaeo-Tethys remnants (Hutchison, 1975, Early Triassic (Barber and Crow, 2009; Metcalfe, 2009). The Sukhothai 1977, 2009; Metcalfe, 2000). Volcanic Arc that lies between the Indochina–East Malaya and Late Palaeozoic and Early Mesozoic subduction of the Palaeo- Sibumasu Blocks is interpreted to be a continental sliver that Tethys oceanic crust and the collision of the Sibumasu and East separated from the Indochina–East Malaya margin by back-arc Malaya Blocks resulted in active magmatism (Metcalfe, 2000). The spreading in the Permian (Metcalfe, 2009, 2010; Sone and Metcalfe, products of this magmatism are Permian and Triassic granitoids of 2008)(Fig. 1). Another important episode of rifting around northern two provinces, the Main Range Province and the Eastern Province Australia occurred in the Jurassic and the blocks that separated from (which includes the Central and Eastern Belts) (Fig. 2). Predominantly this area are now in Borneo, Java, and Sulawesi (Hall et al., 2009). I-type and rare S-type Permian and Triassic granitoids of the Eastern The Banda and Argo Blocks collided with the SE Asian margin in Province are considered to be subduction-related, produced in a Cretaceous time. Collision of the Woyla intra-oceanic arc with the volcanic arc that formed on the East Malaya Block (Metcalfe, 2000). Sumatra Block in the Late Cretaceous terminated subduction beneath Triassic S-type granitoids, intruded into the Sibumasu Block, are Sundaland (Clements et al., in press; Hall et al., 2009) and it interpreted as syn- and post-collisional (Hutchison, 1977; Metcalfe, resumed only in the Eocene (Hall et al., 2009). West Sumatra and 2000). Triassic volcaniclastic turbidites were sourced from the East West Burma, that originally formed one block, became separated by Malaya Volcanic Arc and are now exposed near the Bentong–Raub the opening of the Andaman Sea in the Miocene (Barber and Crow, Suture Zone (Metcalfe, 2000; Metcalfe et al., 1982; Roslan, 1989). 2009). Upper Cretaceous granitoids were emplaced locally in the Central Belt Abundant subduction-related and syn- to post-collisional Permian– (Cobbing et al., 1992). Based on stratigraphical and structural Triassic, Jurassic and Cretaceous granitoids are intruded into the core of differences the Malay Peninsula is divided into three geological Sundaland. The granitoids that extend from Thailand, through the Malay zones (belts): the Eastern Zone, Central Zone, and Western Zone that Peninsula and Indonesian Tin Islands are tin-bearing and are known as are bounded by major fault zones (e.g. Hutchison, 1975, 1977; Khoo the SE Asian tin belt (e.g. Cobbing et al., 1992). These granitoids are and Tan, 1983)(Fig. 2). The Western Zone lies on the Sibumasu Block probably a major source of detrital zircons in Sundaland. and is intruded by the granitoids of the Main Range Province. The Few studies have attempted to date the basement in the SE Asian Central and Eastern Zones lie on the East Malaya Block and are region. Hamilton (1979) mapped the extent of the Cretaceous intruded by Eastern Province granitoids. continental crust from well data in the Java Sea and traced the Upper Mesozoic and Cenozoic rocks in the Malay Peninsula are Sundaland margin from West Java to SE Borneo. Based on U–Pb continental. Alluvial and fluvial sequences of the Upper Jurassic– SHRIMP zircon dating of Cenozoic igneous and sedimentary rocks, Lower Cretaceous Tembeling and Gagau Groups were deposited in the Smyth et al. (2007) confirmed that there is a change in basement central part of the Malay Peninsula (Gobbett and Hutchison, 1973; character from West to East Java. However, inherited Archaean, Harbury et al., 1990; Racey, 2009; Rishworth, 1974). Palaeocurrent Proterozoic, and Palaeozoic zircons suggest that East Java is underlain data from the Tembeling Group in the Malay Peninsula suggest by Gondwana-derived continental crust and not by Cretaceous sediment transport from the northwest (Harbury et al., 1990). The accreted material as has been suggested previously (e.g. Hamilton, Tembeling Group and Khorat Group in NE Thailand are correlatable 1979). Previous Nd–Sr and U–Pb zircon dating of Permian–Triassic (Racey, 2009) and form a regionally extensive, laterally continuous granitoids in the Malay Peninsula (Liew and McCulloch, 1985) stratigraphic sequence over much of the region (e.g. Racey, 2009). suggested that the crust beneath the Sibumasu Block is 1500– However, in the Malay Peninsula much of the Post-Triassic succession 1700 Ma old and the crust beneath the East Malaya Block is 1100– has been eroded as a result of prolonged emergence during the Late 1400 Ma. Based on U–Pb dating and Hf-isotope analysis of detrital Cretaceous and Early Palaeogene (Clements et al., in press). Cenozoic zircon and baddeleyite from large rivers draining mainland SE Asia – coal-bearing lacustrine and fluvial basins have a very limited the West Burma, Sibumasu and Indochina Blocks – Bodet and Schärer distribution on land (Stauffer, 1973). (2000) identified five Proterozoic crustal growth events in the area at around 2.5 Ga, 2.3 Ga, 1.9 Ga, 1.1 Ga and 0.8 Ga. Based on radiogenic 3. Sample selection isotope analyses, radiometric age studies, and petrographic data from the Malino and Palu Metamorphic Complexes, van Leeuwen et al. Zircons from nine modern river samples draining the Malay (2007) suggested that Northwest Sulawesi is underlain by crust that Peninsula (Fig. 2) were dated using U–Pb techniques. Six of these was derived from the New Guinea–Australian margin of Gondwana. samples were selected for Hf-isotope analyses based on the nature of source lithologies and catchment of the particular river, and on the 2.2. The Malay Peninsula composition of heavy mineral assemblages (Sevastjanova, 2007) with the aim of covering all potential source areas. Source lithologies were The Malay Peninsula is situated in the heart of Sundaland and lies characterised based on the published literature, SRTM-derived digital on the Sibumasu and East Malaya Blocks (Fig. 1). The Sibumasu Block elevation models (DEM), and geological and river maps (Gobbett and extends from western Yunnan to Burma, Thailand, western Peninsular Hutchison, 1973; Hutchison and Tan, 2009 and references therein; Malaysia, and northeast Sumatra. East Malaya is a southwards Senathi Rajah et al., 1976) that were digitised using GIS software. extension of the Indochina Block (Metcalfe, 2000). Lower Palaeozoic Sample details are summarised in Table 1. Permian–Triassic zircons in rocks of the Sibumasu Block show Gondwanan biogeographic samples IS37 and IS40 characterise detritus eroded from the Eastern affinities. This and the presence of Lower Permian glaciomarine Province granitoids. Samples IS14, IS18, IS19, IS31, and IS41 diamictites indicate that Sibumasu was part of Gondwana until the characterise various sedimentary, igneous and metamorphic source Early Permian (Metcalfe, 1988, 1996b, 1998, 2009; Schwartz et al., rocks common in the Central Zone, while samples IS2 and IS26 that I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1027

Fig. 2. Simplified geological map of the Malay Peninsula (modified from Gobbett and Hutchison, 1973). White dots show the locations of river sand samples analysed from the Malay Peninsula. were collected from the first-order streams draining granitoids in the Maurer (1992). The heavy mineral fraction was separated using Western Zone are representative of the Main Range Province detritus. sodium polytungstate (SPT) solution (density 2.89 g/cm3) and run through a Franz Magnetic separator at 20° tilt angle, and 0.1, 0.4, and 4. Analytical techniques 1.7 μA voltages. Non-magnetic fractions (N1.7 μA) were separated in diiodomethane (DIM) with a density 3.3 g/cm3. Zircons were hand- 4.1. Sample preparation picked from the residual DIM heavy fraction, mounted in araldite resin on labelled glass slides or resin discs, and polished. Samples IS2, Heavy minerals were separated from the 63 to 250 μm grain-size IS18, IS37, IS40 and IS41 were imaged with CL-SEM prior to Hf-isotope fraction following a standard procedure described by Mange and analyses. 1028 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039

Table 1 Descriptions of the samples analysed from the Malay Peninsula.

Geological zone Sample Longitude Latitude Drainage

Eastern IS40 102.49112 5.73763 Eastern Province granitoids, Carboniferous schists and phyllites and recent coastal sediments IS37 103.43609 4.64011 Eastern Province granitoids, Carboniferous schists and phyllites, recent coastal sediments and minor Mesozoic clastic rocks. Central IS41 101.69095 5.66084 The Cretaceous Stong Migmatite Complex IS14 102.11230 5.53565 Eastern Province granitoids, the Stong Migmatite Comples, Mesozoic and Permian clastic and volcaniclastic rocks, and minor basic volcanics and limestones IS19 102.01583 4.09164 Mesozoic and Permian clastic and volcaniclastic rocks, Eastern (the Central Belt), and Main Range Province granitoids, and Permian limestones IS18 102.19065 4.04281 Mesozoic and Permian clastic and volcaniclastic rocks, minor basic volcanics, Eastern (including the Central Belt), and Main Range Province granitoids, and Permian limestones IS31 102.68436 3.55614 Jurassic‐Cretaceous fluvial‐alluvial rocks (the Tembeling Gp) Western IS2 101.34138 4.42584 Main Range Province granitoids IS26 101.89650 3.44557 Main Range Province granitoids

4.2. LA-ICP-MS U–Pb dating The 176Lu decay constant (1.865×10−11) calculated by Scherer et al. (2001) from terrestrial samples, the chondritic values of 176Hf/ U–Pb dating was performed at University College London using a 177Hf=0.0332 and 176Lu/177Hf=0.282772 (Blichert-Toft and Albarède, New Wave 213 aperture-imaged frequency-quintupled laser ablation 1997), and zircon ages determined by U–Pb dating techniques were system (213 nm) coupled to an Agilent 7500 quadrupole-based ICP- used for further calculations. MS. Grains typically were ablated with 55 μm laser spot and a 30 μm Epsilon Hf (εHf) describes the deviation of the initial 176Hf/177Hf laser spot was used for finer-grained samples. Background was ratio from the evolution line defined by chondritic meteorites (CHUR) 176 177 measured for 30 s, followed by 30 s of data collection, and a 30 s purge (Faure and Mensing, 2004). In the granitoid magmas high Hf/ Hfi 176 177 cycle after each run. Real-time data were processed using the (εHf≫0) indicates mantle-derived input and low Hf/ Hfi GLITTER® software package (Griffin et al., 2008). PLESOVIC zircon (εHfb0) suggests crustal reworking (Belousova et al., 2006). Hf

(TIMS reference age 337.13±0.37 Ma; (Sláma et al., 2008)) and NIST model ages (TDM) represent a minimum age for the source material of C SRM 612 silicate glass (Pearce et al., 1997) were used as external the zircon parental magma. Crustal model ages (TDM) assume that standards for correcting mass fractionation and instrumental bias. At zircon parental magma was produced from an average continental least 60 grains were analysed in each sample. 204Pb could not be crust (176Lu/177Hf=0.015), that originally was derived from the measured for common lead correction because of interference from depleted mantle (Belousova et al., 2006), and provides a more realistic 204Hg in the carrier gas. The correction of Andersen (2002), which estimate of its source age. assumes that measured 206Pb/238U, 207Pb/235U and 208Pb/232Th ratios are discordant due to a combination of common lead contamination 5. Results and lead loss at defined time, was used instead. A 10% cutoff was adopted to reject discordant data. 238U/206Pb ages are used for zircons 5.1. U–Pb dating b1000 Ma and the 207Pb/206Pb ages were used for older zircons. 752 U–Pb zircon ages were collected from nine modern river-sand 4.3. Hf-isotope analyses samples from the Malay Peninsula. Results are illustrated in Figs. 3 and 4. Sample locations were chosen with the aim of covering zircon age Hf-isotope analyses were performed at GEMOC ARC National Key variations in all three geological zones. Centre at Macquarie University, Australia. 176Hf/177Hf ratios in zircons were measured with a New Wave Research 213 nm laser-ablation 5.1.1. The Eastern Zone microprobe attached to a Nu Plasma multicollector ICPMS. The Two samples (IS37 and IS40) were analysed from the Eastern analytical procedure is described in detail by Griffin et al. (2000, Zone. There are two major Phanerozoic zircon populations: Late 2006a). Time-resolved analyses were processed using Nu Plasma Permian–Late Triassic (199 to 260 Ma) and Early-Middle Permian software. Analyses were carried out at 5 Hz frequency with a beam (266 to 296 Ma). A Late Permian-Late Triassic population is present in diameter of 55 μm and energies around 0.1 mJ per pulse. Background both samples. An Early-Middle Permian population is prominent only was measured for 60 s. The length of the analysis varied between 30 in sample IS37, collected from the southern part of the zone. and 140 s depending on the thickness of the grains. Repeated analyses of Mud Tank (long-term running average 176Hf/ 5.1.2. The Central Zone 177Hf value 0.282523±43, (Griffin et al., 2006b)) and 91,500 (long- Five samples, IS14, IS18, IS19, IS31, and IS41, were analysed from term running average 176Hf/177Hf value 0.282307±58, (Griffin et al., the Central Zone. There are five Phanerozoic zircon populations in the 2006b)) zircon standards were used to monitor data quality (Table 2). Central Zone samples: Late Cretaceous (70 to 84 Ma), Jurassic (162 to

Table 2 Precision and accuracy for reference standard zircons (91,500 and Mud Tank) used in this study.

Reference Technique n 176Hf/177Hf ±2σ 176Lu/177Hf ±2σ 176Yb/177Hf ±2σ

91500 Griffin et al., 2006b LA‐MC‐ICPMS 632 0.282307 ±58 0.000317 ±54 0.0115 ±50 This study LA‐MC‐ICPMS 7 0.282319 ±29 0.000321 ±1 0.0128 ±2

Mud Tank Griffin et al., 2006b LA‐MC‐ICPMS 2190 0.282523 ±43 This study LA‐MC‐ICPMS 87 0.282464 ±19 0.000059 ±2 0.0027 ±1 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1029

60 30 40 20 20 10

60 30 40 20

Eastern

Eastern 20 10

60 60 40 40 20 20

60 30 40 20 20 10

60 30 40 20 20 10

Central

Central 60 30

Number of grains 40 20

Number of grains 20 10

60 30 40 20 20 10

60 30 40 20 20 10

60 30 40 20

Western

Western 20 10

0 500 10001500 20002500 3000 3500 4000 0 100 200 300 400 500 Ages are shown in Fig.4. Age, Ma Age, Ma

– – Fig. 3. Histograms showing detrital zircon U–Pb ages in river sediments from the Malay Fig. 4. Histograms showing the 0 500 Ma U Pb ages in detrital zircons from the Malay – Peninsula. Bin width is 50 Ma. Peninsula. Grey area highlights zircons derived from local Permian Triassic granitoids. Bin width is 10 Ma. Note that the vertical scale for IS41 is 0 to 60 and for all other samples 0 to 30. 190 Ma), Late Permian–Late Triassic (224 to 258 Ma), Early-Middle Permian (267 to 299 Ma), and Ordovician–Silurian (423 to 458 Ma). A Late Cretaceous population is prominent in samples IS14 and IS41, CL-imaging reveals cores in euhedral/subhedral zircons from the collected from rivers draining the Stong Migmatite Complex. Jurassic Western Zone of the Malay Peninsula and U–Pb dating shows these grains form a small population in sample IS31, collected from a river have Precambrian ages. Both Precambrian cores and rounded grains draining Mesozoic alluvial sedimentary rocks. A significant Late are common in the Eastern and Central Zones of the Malay Peninsula Permian–Late Triassic population is present in all samples. An Early- (Fig. 5). Middle Permian population is present only in sample IS18 collected from the southern part of this zone. A minor Ordovician–Silurian 5.2. Hf-isotope composition population is found only in sample IS31. During this study 243 of the dated zircon grains were analysed for Hf-isotope composition. Results are summarised in Figs. 6 and 7. 5.1.3. The Western Zone Two samples (IS2 and IS26) were analysed from the Western Zone. 5.2.1. The Eastern Zone Two major Phanerozoic zircon populations can be identified: Late Samples IS37 and IS40 were analysed from the Eastern Zone. Late 176 177 Triassic (212 to 228 Ma) and Middle Permian–Middle Triassic (229 to Permian–Late Triassic grains yield Hf/ Hfi values that are higher 270 Ma). The Late Triassic population is dominant in both samples. A than those in zircons of similar age from the Western Zone. 176Hf/ 177 Middle Permian–Middle Triassic population is prominent only in Hfi values of these grains plot both above and below CHUR (εHf sample IS26, which was collected in the southern part of this zone. range from −4 to +8) (Figs. 6 and 7). This suggests a mixed crust- 176 177 Devonian–Carboniferous grains are present in all zones, but do not and mantle-derived source. Low Hf/ Hfi values of Early-Middle form major populations (Fig. 4). Small numbers of Late Archaean–Late Permian zircon grains suggest a crustally-derived source and those of Proterozoic grains are consistently present in all samples analysed. Precambrian plot both above and below CHUR. Sample IS31 contains minor latest Neoproterozoic (598 to 646 Ma), Meso-Neoproterozoic (793 to 1171 Ma), late Palaeoproterozoic (1732 5.2.2. The Central Zone to 1888 Ma) and Neoarchaean–early Palaeoproterozoic populations Samples IS18, IS31, and IS41 were analysed from the Central Zone. 176 177 (2196 to 2722 Ma). There is one Eoarchaean (3750±56 Ma) zircon in Late Cretaceous grains yield low Hf/ Hfi values that plot below sample IS37. CHUR (Figs. 6 and 7). This suggests a crustal source and is consistent 1030 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039

Fig. 5. CL-images of detrital zircons from rivers draining the Malay Peninsula. The top three rows show morphology and zoning of Precambrian zircons derived from the Eastern Province. Note that many of the zircons are rounded, but subhedral grains with older cores are also common. The following row shows zoning in the Late Carboniferous–Middle Permian zircons derived from the Eastern Province. The presence of cores suggests a reworked crustal source. The bottom two rows show zoning in Precambrian zircons derived from the Main Range Province. These are cores in euhedral/subhedral zircons. Scale bar 100 μm.

with a provenance from granitoids within the Stong Migmatite 5.2.3. The Western Zone 176 177 Complex. Hf/ Hfi values for Jurassic grains suggest a mixed Sample IS2 was analysed from the Western Zone. Late Triassic 176 177 176 176 177 source. Hf/ Hfi values for Triassic and Permian grains have Hf/ grains in this sample yield Hf/ Hfi ratios lower than CHUR 177 Hfi values that plot both above and below CHUR and are (εHfb0). This suggests a crustal source for the parental granitoids of 176 177 comparable to zircons of similar age from the Eastern Zone. Early these zircons. The high Hf/ Hfi values of Mesoproterozoic grains 176 177 Palaeozoic grains yield predominantly low Hf/ Hfi values that suggest minor ‘juvenile’ crust production around 1.1–1.2 Ga and 176 177 176 177 suggest crustally-derived source rocks, while Hf/ Hfi values of 1.6 Ga. The low Hf/ Hfi values of Palaeoproterozoic grains suggest Precambrian zircons plot both above and below CHUR. a crust-derived source for these grains. I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1031

a 0.2835 EASTERN 0.2830 ZONE C IS40 TDM 0.2825 C IS37 1.55 Ga TDM 1.97Ga T C 0.2820 DM 2.17Ga C TDM 0.2815 2.73 Ga

BLOCK

0.2810 DM

EAST MALAYA 0.2805 CHUR

0.2800

0.2835 b CENTRAL 0.2830 ZONE C T C IS18 DM T 0.2825 1.41 Ga DM IS31 1.51 Ga C TDM

Hfi IS41 1.88 Ga 0.2820 C

177 TDM 2.53 Ga

Hf/

0.2815 BLOCK

176 0.2810

DM EAST MALAYA 0.2805 CHUR

0.2800 0.2835 c WESTERN 0.2830 ZONE T C IS2 0.2825 DM 1.58 Ga C TDM 0.2820 2.0 Ga T C 0.2815 DM 2.97 Ga

BLOCK

0.2810 DM SIBUMASU 0.2805 CHUR

0.2800 0 500 1000 1500 2000 2500 3000 3500 T(Ma)

Fig. 6. Plots of U–Pb ages versus initial Hf-isotope composition in detrital zircons from the Eastern (a), Central (b) and Western (c) Zones in the Malay Peninsula. Dashed lines show crustal model ages for significant zircon populations.

6. Discussion 12 Ma, and that Permian and Triassic granitoids are most abundant. Most published datasets indicate that the Main Range Province 6.1. Late Palaeozoic–Early Mesozoic granitic magmatism in the Malay granitoids are 200–230 Ma old (Fig. 8G). However, some ages are Peninsula Jurassic and some are as young as Cretaceous. There are a few Main Range granitoids that are older than 230 Ma in the Langkawi Islands Morphology, oscillatory growth-zoning, and ages of Permian and (242 Ma (Krähenbuhl, 1991)) and in Melaka (253–305 Ma (Gobbett, Triassic zircons in the river sediments indicate that they were derived 1973; Krähenbuhl, 1991)). predominantly from local granitoids. Therefore, U–Pb ages for these U–Pb zircon data presented in this study reveal two distinct zircons constrain the timing of magmatism throughout the Malay episodes of magmatism (Fig. 8D and F) in the Eastern Province during Peninsula. Detrital zircon is resistant to tropical weathering and the Permian and Triassic. This bimodal age distribution has not been therefore we suggest that these ages are more robust than the identified in previous studies. Zircons sourced from the Main Range previous K–Ar and Rb–Sr ages (e.g. Ahmad and Yap, 1976; Bignell and Province granitoids are predominantly Late Triassic (Fig. 8H). One Snelling, 1977; Cobbing et al., 1992; Gobbett, 1973; Krähenbuhl, sample in the Western Zone (IS26) contains a small number of Late 1991; Schwartz et al., 1995; Seong, 1990; Yap, 1986) reported for the Permian–Middle Triassic grains (Fig. 4), although it is not clear Malay Peninsula granitoids. K–Ar ages need to be treated with caution whether these grains were sourced from Main Range Province in tropical settings (e.g. Macpherson and Hall, 2002) such as those granitoids or from granitic clasts in the Bentong–Raub Suture Zone. that prevailed in the Malay Peninsula through the Mesozoic and Our new data do not support the hypothesis that Jurassic granitoids Cenozoic (e.g. Morley, 1998). Rb–Sr ages can also be problematical as are present in the Malay Peninsula (Fig. 8B). Although samples IS31 these isochrones date hydration events that are often difficult to and IS14 from the Central Zone (Fig. 4) have a small number of interpret. Jurassic grains (n=5 and 2 respectively) and there is one Jurassic core A summary of previously published data (Fig. 8A) suggests that in sample IS41, we suggest these grains were most likely reworked granitoids of the Malay Peninsula range in age from 65±2 Ma to 406± from Upper Jurassic alluvial–fluvial ‘redbeds’ that are exposed over 1032 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 a 20 T C DM T C T C 15 1.55Ga DM DM C 1.97Ga 2.17Ga TDM 10 2.73Ga 5 0 -5

εHf

-10 BLOCK -15 Eastern

Zone EAST MALAYA -20 -25 -30 b 20 C C C TDM T DM TDM 15 1.41Ga 1.51Ga T C 1.88Ga DM T C 2.53Ga DM 10 2.94Ga 5 0 -5

εHf

-10 BLOCK Central -15

Zone EAST MALAYA -20 -25 -30 c 20 C TDM T C 15 1.58Ga DM C 2.0Ga TDM 10 2.97Ga 5 0 -5

εHf

-10 BLOCK Western -15 SIBUMASU Zone -20 -25 -30 0 500 1000 1500 2000 2500 3000 3500 Age(Ma)

CHUR Depletedmantle IS2 IS18 IS31 IS41 IS40 IS37

Fig. 7. Composite plots of U–Pb ages versus initial epsilon Hf values for detrital zircons from the Eastern (a), Central (b) and Western (c) Zones in the Malay Peninsula. Dark shaded areas show major episodes of crust production in the Sibumasu and East Malaya Blocks. Light shaded areas show other possible episodes of magmatism in the SE Asian basement fragments. However, granitoids produced during these episodes are not abundant, and some of the grains may have been recycled from sources outside the Malay Peninsula. large areas of Central and SE Laos, Cambodia, NE Thailand, and the 6.2. Magma sources for Permian–Triassic granitoids in the Malay Peninsula (Harbury et al., 1990; Racey, 2009). Provenance Malay Peninsula studies of these ‘redbeds’ in Thailand, referred to as the Khorat Group and lateral equivalents (e.g. Carter and Bristow, 2003; Racey, 2009), Compositions of magma sources are governed by the tectonic suggest that they were sourced from the Qinling Orogenic Belt processes by which they are produced and therefore may be matched immediately to the north and deposited in a foreland basin setting. A to individual geodynamic settings. Granitoids can be produced in a northerly provenance is supported by palaeocurrent data from the range of settings that include mid-ocean ridges, intraplate settings Malay Peninsula (Harbury et al., 1990). Five U–Pb zircon age (oceanic islands, continental rifts and hotspots), subduction zones populations are recognised from the Khorat Group in Thailand (Carter (continental margin arcs, and island arcs), and continent–continent and Bristow, 2003; Carter and Moss, 1999): Jurassic (161 to 170 Ma), collision zones. Mantle-derived sources are commonly associated Permian–Triassic (242 to 261), Ordovician–Silurian (433 to 467 Ma), with mid-ocean ridges, oceanic island arcs, and hotspot settings, late Palaeoproterozoic (1799 to 1839 Ma), and early Palaeoproterozoic whereas crustal reworking is the primary source for magma (2450 to 2500 Ma). Presence of Jurassic zircons in the Khorat Group generation in continental collision zones. Sources for subduction- supports our interpretation that its equivalents are the most likely related magmas may be complex, since many processes such as partial sources for the Jurassic zircons in river sands from the Malay Peninsula. melting of subducted sediments and oceanic lithosphere, melting There is therefore no firm evidence for major magmatism in the area of the mantle wedge, mantle flow, magma mixing, and crustal between the Late Triassic and Cretaceous. contamination can all contribute to subduction-related melts. Most I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1033

CARBO- SI- ORDO- subduction-related magmas are produced by a combination of several CRETA- JURAS- TRIAS- PERM- DEVO- CENOZOIC NIFE- LU- VICI- CEOUS SIC SIC IAN NIAN of these processes (e.g. Condie, 1989; Pearce and Peate, 1995). Some ROUS RIAN AN 100 authors have emphasised that newly generated crust has a different A* preservation potential in different tectonic settings. For instance, Hawkesworth et al. (2010) suggested in subduction zones the volume 50 of the continental crust that can be recycled back into the mantle may be comparable with the volume of crust that is generated in these 0 settings. 100 Permian–Triassic granitoids of the Malay Peninsula are commonly B interpreted as subduction-related and syn-to post-collisional (e.g.

All Peninsula Metcalfe, 2000). Hf-isotope data obtained for Permian and Triassic 50 zircons allow the recognition of three major magmatic suites: (a) Permian crustally-derived granitoids, (b) Early-Middle Triassic granitoids with 0 a mixed mantle–crust source, and (c) Late Triassic crustally-derived granitoids. This suggests three major Permian–Triassic episodes of 60 * C magmatism in the Malay Peninsula. Two of these episodes (a and b) 40 occurred in the Eastern Province. Evolved Hf-isotope compositions (εHf values vary from −8to 20 −13) of Triassic zircons from the Sibumasu Block (Western Zone of 0 the Malay Peninsula) indicate a reworked crustal source and a syn- to post-collisional setting for their parental granitoids. The older D 60 crystallisation ages of Permian–Triassic zircons from the East Malaya Eastern-I 40 Block (Western and Central Zones of the Malay Peninsula) support a subduction-related setting for their parental granitoids. Abundant 20 crustally-derived granitoids are unusual in a subduction-related 0 setting and their presence may indicate derivation from old 30 continental basement beneath the East Malaya Block. E* 6.3. Different tectonic models Number of grains 15

There are several tectonic models for the Permian and Triassic 0 evolution of the Thai–Malay Peninsula. Most of these models 30 acknowledge that tin belt granitoids were produced during the closure F of Palaeo-Tethys and the resulting collision between Sibumasu and Eastern-II East Malaya–Indochina (e.g. Barber and Crow, 2009; Hutchison, 1977; 15 Metcalfe, 2000, 2009). However, the exact timing of this collision remains contentious, and is the focus of this section. Three main ages 0 have been suggested for the Sibumasu–East Malaya collision: 1) Late 50 – * Triassic Jurassic (Hirsch et al., 2006; Kamata et al., 2002; Sashida et al., G 1995), 2) Middle-Late Triassic (Sone and Metcalfe, 2008), and 3) Late – 25 Permian Early Triassic (Barber and Crow, 2009; Metcalfe, 2009) (Table 3).

0 6.3.1. Late Triassic–Jurassic collision 50 – H Proposals for a Late Triassic Jurassic collision between Sibumasu and East Malaya are based on radiolarian biostratigraphy from cherts

25 Main Range in the Semanggol Formation of northwestern Malay Peninsula and its equivalents in Thailand. Hirsch et al. (2006) suggest that the Sibumasu–East Malaya collision occurred in the latest Triassic–Early 0 Jurassic, Kamata et al. (2002) argued for the collision after the Early 0 100 200 300 400 500 Carnian (early Late Triassic), and Sashida et al. (1995) suggest Age (Ma) collision occurred after the Middle Triassic. These studies base the timing of collision on the assumption that radiolaria from cherts Fig. 8. Histograms showing previously published granitoid ages and new U–Pb detrital zircon ages from the Malay Peninsula. A: a summary of published ages* for the whole represent pelagic open-ocean sedimentation and therefore must be region. B: a summary of all analysed detrital zircon U–Pb ages that are younger than older than collision. Metcalfe (2000) however suggests that Triassic 500 Ma. C: published ages* for the Eastern Province granitoids (both Eastern and Semanggol Formation cherts were deposited in a foredeep basin and – Central Belt). D: 0 500 Ma old zircons that are sourced from the granitoids of the therefore do not represent true Palaeo-Tethyan oceanic deposits. Eastern Belt (IS37 and IS40) and the Stong Migmatite Complex (IS41). These are representative of the Eastern Province source. E: published granitoid ages* for the Furthermore, Metcalfe (2000) draws attention to a major structural Eastern Province, excluding the Central Belt. F: 0–500 Ma old zircons sourced from the discontinuity between Palaeozoic and Mesozoic rocks in the Peninsula Eastern Belt Granitoids (IS37 and IS40). G: published ages* for the Main Range Province as evidence for collision at this time and Metcalfe (2003) provides granitoids. H: 0–500 Ma old zircons from the Western Zone of the Malay Peninsula (IS2 additional conodont colour and textural alteration data that support and IS26) that are representative of the Main Range source. Bin width is 10 Ma. collision at the end Permian. Barber and Crow (2009) also point out *Previously published data from Ahmad and Yap (1976), Bignell and Snelling (1977), Cobbing et al. (1992), Gobbett (1973), Krähenbuhl (1991), Schwartz et al. (1995), that in many occurrences the studied radiolarian cherts were Seong (1990) and Yap (1986). deposited in intracontinental basins on the Sibumasu continental crust and not on Palaeo-Tethyan oceanic crust. Therefore, the timing of collision between Sibumasu and East Malaya–Indochina, and the 1034 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039

Table 3 A summary of different tectonic models proposed for the timing of the Indosinian Orogeny (Sibumasu and East Malaya–Indochina collision).

Collision timing Evidence Arguments against This study

Latest Triassic–Early Jurassic Radiolarian chert ages • In many instances, cherts deposited • Do not support this timing; in the inter-continental basins; • These models require Jurassic syn- • Do not constrain the timing to postcollisional magmatism; Permian Triassic Jurassic of the Paleo-Tethys destruction • Only a few Jurassic grains present Hirsch et al. (2006) (Barber and Crow, 2009). in the analysed samples. After the Early Carnian

Permian Triassic Jurassic Kamata et al. (2002) After the Middle Triassic

Permian Triassic Jurassic Sashida et al. (1995) Late Permian- Middle-Late • Chronostratigraphic occurrence of • Different deformation styles of • Reveal two episodes of magmatism Early Triassic Triassic pelagic or deep-sea sediments 1) Carboniferous–Permian and in the Eastern Province; (arc) (main) in Nan and Sra Kaeo sutures in Thailand; 2) Triassic rocks; • Do not resolve the arguments with • Granitoid ages and geochemistry. • Permo-Triassic unconformity regard to these timings, but suggests Permian Triassic Jurassic (Barber and Crow, 2009); a more complex subduction history. Sone and Metcalfe (2008) Late Permian–Early Triassic • Different deformation styles of • Up to 30 Ma time lag between 1) Carboniferous–Permian and the collision and a major phase 2) Triassic rocks of post-collisional magmatism. Permian Triassic Jurassic • Permo-Triassic unconformity • However, this time lag is possible Barber and Crow (2009) Metcalfe (2009) (Barber and Crow, 2009). (e.g. England and Thompson, Late Permian–Early Triassic. • Three Permian–Triassic episodes of magmatism 1984; Thompson and England, 1984). The main collision occurred 1) Permian crustderived granitoids shortly after the collision • 2) Early-Middle Triassic granitoids with with the arc a mixed mantleand crust-derived source • 3) Late Triassic crustderived granitoids • Two Permian–Triassic episodes of magmatism Jurassic Permian Triassic (1 and 2) in the Eastern Province. This study

destruction of Palaeo-Tethys, cannot be determined by these both contain ophiolitic rocks, melange and radiolarian cherts of radiolarian ages. Furthermore, collision in the Late Triassic is not Permian age and are interpreted as a remnant back-arc basin by Sone supported by other lines of evidence. Our new detrital zircon U–Pb and Metcalfe (2008). ages presented here indicate unequivocally that collision occurred Our new detrital zircon data do not contradict the model that prior to the Late Triassic. assumes Permian–Triassic collision of East Malaya with the Sukhothai Arc was followed by Sibumasu–East Malaya collision (the major continent–continent collision) in the Middle–Late Triassic. A Late 6.3.2. Middle-Late Triassic collision Permian–Early Triassic gap in magmatism and a subsequent change of Sone and Metcalfe (2008) interpret the Eastern Province grani- zircon Hf-isotope compositions could be explained by the collision toids as remnants of the Sukhothai Arc (including the Linchang, between the Sukhothai Arc and East Malaya. The predominantly Late Sukhothai, and Chanthaburi Blocks). According to Sone and Metcalfe Triassic ages of zircons sourced from the Main Range Province and (2008) this arc developed on an elongate fragment of continental their crustally-derived Hf-isotope signatures are consistent with the crust in the Permian that collided with Indochina (East Malaya) by the Middle Triassic–early Late Triassic major continent–continent colli- Early Triassic – a model that places the major continent–continent sion. However, this timing is not supported by structural evidence collision (Sibumasu–East Malaya) later than initial collision and prior (Barber and Crow, 2009). to the Middle Triassic–early Late Triassic. It is likely that the Eastern Province granitoids represent the southerly continuation of the Sukkothai Arc into the Malay Peninsula and Sumatra. However, this 6.3.3. Late Permian–Early Triassic collision proposed continuation of the Sukhothai Arc (Chanthaburi Block) Several authors (Barber and Crow, 2009; Harbury et al., 1990; southward into the Malay Peninsula (Metcalfe, 2009) requires the Metcalfe, 2009) support Late Permian–Early Triassic collision between presence of a second suture zone (between the Sukhothai Arc and East the Sibumasu and East Malaya Blocks. These arguments are based Malaya Block) east of the Bentong–Raub suture zone. This inference is mainly on the different structural deformation styles of Late supported by a zone of sheared diamictite along the eastern margin of Palaeozoic and Triassic rocks in the Malay Peninsula and Sumatra the Central Belt of the Malay Peninsula (referred to as the Lebir Fault (Barber and Crow, 2009; Harbury et al., 1990). Late Palaeozoic, and Zone), that is interpreted by Metcalfe and Chakraborty (1988) as especially Carboniferous rocks show multiphase folding and regional either olistostromes that formed along the fault scarps of a developing metamorphism (Harbury et al., 1990). Permian rocks show intensive graben or as a suture zone mélange. Although there are no reports of internal deformation, whereas Triassic rocks are only tilted and gently ophiolitic-type rocks or radiolarian cherts within the sheared folded (Barber and Crow, 2009). In Sumatra end-Permian collision is diamictites of the Lebir Fault Zone, we prefer to interpret these supported by the absence of uppermost Permian and lowermost mélanges as tectonic in origin, and representative of a major suture. Triassic fossils (representing an unconformity) within a sequence of This interpretation fits very well with observations further north, Permian–Triassic limestones (Barber and Crow, 2009). where the Chanthaburi and Sukhothai Blocks are separated from In the new interpretation for Thailand (Sone and Metcalfe, 2008), Indochina by the Sra Kaeo and Nan Sutures respectively. These sutures this tectonic event corresponds to the collision of the Sukhothai Arc I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1035 with the East Malaya Block and not collision between Sibumasu and (Krähenbuhl, 1991), the Langkawi Islands, and Bangka (Barber and East Malaya. An alternative interpretation is that Sibumasu–East Crow, 2009). Malaya collision occurred in the Late Permian–Early Triassic, shortly after, or contemporaneously with, the collision of East Malaya and the 6.3.4. Collision timing supported in this study Sukhothai Arc. The Lebir Fault Zone therefore marks the boundary Our data do not contradict the interpretation that the Sukhothai between the Sukhothai Arc and East Malaya (and represents a Arc collided with East Malaya at the end of the Permian and was then – remnant oceanic basin as suggested by Sone and Metcalfe (2008) followed by the main collision between Sibumasu and the newly – further north), whereas the Bentong Raub suture zone separates accreted Sukhothai Arc and East Malaya in the Middle to Late Triassic Sibumasu from the Sukhothai Arc and East Malaya and represents the (e.g. Sone and Metcalfe, 2008). However, other lines of evidence (e.g. main Palaeo-Tethys Suture. Two issues require explanation for this gently deformed Triassic deposits overlaying intensely deformed model to be valid: (a) the tectonic setting of the Eastern Province Palaeozoic rocks (Barber and Crow, 2009; Harbury et al., 1990) and – granitoids and (b) the time lag between Sibumasu East Malaya missing latest Permian to earliest Triassic fauna from within Permo- – – collision (Late Permian Early Triassic, ~250 254 Ma) and the major Triassic limestones (Barber and Crow, 2009) – discussed above) phase of post-collisional magmatism in the Main Range Province support major collision at the end of the Permian/earliest Triassic. We – (200 230 Ma). In this model, collision between the Sukhothai Arc and favour this interpretation and suggest that Sibumasu was accreted to East Malaya was shortly followed by Sibumasu collision and the the Indochina margin at the end Permian and that this collision was Permian Eastern Province granitoids are interpreted as subduction- broadly contemporaneous with the collision between the Sukhothai 176 177 related despite their crustal Hf/ Hfi values that are unusual for Arc and East Malaya (Fig. 9). 176 177 such tectonic settings. These Hf/ Hfi values are easily explained by derivation from old continental crust beneath East Malaya (which C 6.4. Ages of Sundaland basement is supported by the Palaeoproterozoic TDM of these zircons – see later discussion). If the Permian Eastern Province granitoids are subduc- The parental magmas of many granitoids are produced from mixed tion-related then it seems unlikely that the deep oceanic basin that lay sources or incorporate a significant proportion of inherited material. between the Sukhothai Arc and East Malaya was a back-arc basin as Crustal model ages calculated for zircons produced from a mixed suggested by Sone and Metcalfe (2008) further north. The generation source give only an average age of the source material and should not of subduction-related granitoids through the Permian would be be treated as crustal-formation ages (Arndt and Goldstein, 1987; expected to result in the destruction of a significant sized oceanic Kemp et al., 2006). However, when crustal model ages are supported basin, much larger than that expected for a typical back-arc basin. by other lines of evidence, such as U–Pb zircon ages, they can be used Furthermore, the absence of pre-Permian radiolaria from this zone is as an indicator of the true age of the basement rocks. interpreted by Sone and Metcalfe (2008) to indicate back-arc rift initiation in the Early Permian between the Sukhothai Arc and East Malaya. In our model there is eastward-directed subduction beneath 6.4.1. The Eastern Zone East Malaya at this time and associated generation of crustal Eastern Late Permian-Late Triassic zircons from the Eastern Zone have ε Province granitoids. We therefore prefer to interpret the Sukhothai both positive and negative Hf values and a spread of crustal model ε Arc as intra-oceanic and not the result of slab rollback and back-arc ages from 0.72 to 1.55 Ga. The spread in Hf and age discrepancies – basin formation processes. The arc developed on a sliver of between crustal model ages and U Pb ages suggest a mixed source. continental crust that was then accreted to the Indochina margin at Therefore, the crustal model ages of these grains may not provide a the end Permian. Sone and Metcalfe (2008) point out that Permian meaningful estimate of the basement ages. C marine faunas associated with this continental sliver are of warm TDM of Early-Middle Permian zircon grains indicate that their – water Tethyan type and support the interpretation of a back arc origin. parent granitoids were produced from a 1.97 Ga old source. Six U Pb fi These observations however, do not require the Sukhothai Arc to have ages between 1.7 and 2.1 Ga con rm a Palaeoproterozoic age for the C – been attached to the East Malaya Block before the Permian, although basement. TDM suggest a 2.17 Ga source for Devonian Carboniferous – these warm water Tethyan marine faunas do suggest a Cathaysian zircons, but the U Pb ages do not support a 2.17 Ga age for the affinity. Therefore, this evidence cannot be used to argue for the back- basement. These grains are not abundant and may have been sampled C arc tectonic history of the Sukhothai Arc and does not contradict our from Palaeozoic sediments overlying the basement. TDM of Palaeo- – interpretation. proterozoic grains around 2.73 Ga and one 2.5 Ga U Pb for a zircon The Triassic Eastern Province granitoids may be post-collisional, core may indicate a minor Neoarchaean basement contribution. 176 177 despite their mixed ‘crustal’ and ‘juvenile mantle’ Hf/ Hfi values. Using the example of the Woyla Arc collision, Barber (2000) has 6.4.2. The Central Zone shown that in the case of oblique subduction granitic rocks can be River sediments in the Central Zone of the Malay Peninsula contain intruded into an active shear zone that developed as the result of zircons from local granitoids and Mesozoic siliciclastic rocks, and some collision. Examples of foliated granitoids intruded into the (Inthanon) of these zircon grains are likely to be sourced from outside the Malay C suture zone in northern Thailand (Baum et al. (1970) support such Peninsula. TDM from Permian–Triassic zircons are similar to those of the arguments. We suggest that it is likely that the Triassic Eastern Eastern Zone and are likely to have been produced from the same mixed C Province granitoids were emplaced along the Lebir Fault Zone in a source. TDM of Early Palaeozoic detrital zircons indicate the presence of similar fashion to that described by Barber (2000); these granites Mesoproterozoic (1.88 Ga) crust beneath the East Malaya Block. This is were sourced from the upper mantle and crustal melts. supported by nine U–Pb zircon ages ranging from 1.7 to 1.9 Ga. Metcalfe (2000) states that the age of melting of the Sibumasu Several small Meso-Neoproterozoic detrital zircon populations continent probably occurred tens of millions of years prior to the Main (Fig. 7) suggest numerous minor episodes of magmatism. Some of Range Province granitoid emplacement. Such a time lag between the these zircon grains are rounded with frosted surfaces (Fig. 5) and collision and post-collisional magmatism is not unlikely. Some studies therefore are likely to have been recycled from Mesozoic and (e.g. England and Thompson, 1984; Thompson and England, 1984) Palaeozoic sedimentary rocks. The majority of these grains have C C suggest that it may take several tens of millions of years to generate TDM around 2.5 Ga (Fig. 6), similar to TDM in the Eastern Zone. This melts in a thickened crust. Syn-collisional plutons are expected, but may indicate the contribution of Neoarchaean basement in the East may not be abundant. This is consistent with the presence of rare Late Malaya–Indochina Block. Nine U–Pb zircon ages that range from 2.3 to Permian–Middle Triassic Main Range Province granitoids in Melaka 2.7 Ga support this suggestion. 1036 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039

EARLY PERMIAN Paleo-Tethys Sukhothai Arc East Malaya Arc crust-derived granitoids

GONDWANA SIBUMASU EAST MALAYA

MIDDLE PERMIAN

SIBUMASU EAST MALAYA

LATE PERMIAN LFZ

SIBUMASU EAST MALAYA

EARLY TRIASSIC strike-slip BRSZ faults

SIBUMASU EAST MALAYA

mixed mantle-andcrust- MIDDLE TRIASSIC crust-derived derivedgranitoids granitoids

EAST MALAYA

mixed crust-derived LATE TRIASSIC mantle-andcrust- granitoids derivedgranitoids Neo-Tethys (Meso-Tethys) EAST MALAYA Main Range Province Central Eastern Belt Belt 250 km (approx.) Eastern Province

Fig. 9. A schematic conceptual model that provides a possible explanation for the Permian–Triassic subduction of the Palaeo-Tethys Ocean and the Sibumasu–East Malaya collision: modified from Metcalfe (2000, 2009), Sone and Metcalfe (2008) and Barber and Crow (2009). The major difference of this model is that it identifies two distinct Permian–Triassic magmatism episodes in the Eastern Province produced from different sources. Permian ‘crustally’ derived granitoids intruded into the East Malaya Block were most likely subduction- related, whereas Triassic mixed ‘crustally’- and mantle-derived Eastern Province granitoids were emplaced along the faults in the Lebir Fault Zone. We also suggest that the Sukhothai Arc did not separate from the East Malaya by back-arc spreading, but is an intra-oceanic arc built on a continental sliver. BRSZ – the Bentong–Raub Suture Zone; LFZ – the Lebir Fault Zone.

Late Cretaceous zircons present in the river sediments are most of the lack of isotopic dating of these rhyolites firm conclusions cannot likely derived from the Stong Migmatite Complex. The origin of the be drawn at present. Jurassic zircons in river sands is less clear and we interpret these to be recycled from the Mesozoic fluvial–alluvial ‘red-beds’. Palaeocurrent 6.4.3. The Western Zone ‘ ’ – C data suggest that these red-beds are derived from the north north- TDM and εHfb0 in Triassic detrital zircons from the Western Zone east (Harbury et al., 1990). However, there is no firm evidence for suggest that the Main Range Province granitoids (the source rocks of abundant acid igneous rocks of Jurassic age in this region that could these grains) were produced by remelting 1.9–2.0 Ga old crust. This is have been a primary source for Jurassic zircons in the sedimentary supported by the presence of Palaeoproterozoic cores in younger rocks. Although Jurassic granitoids are common in Sumatra (Cobbing, euhedral/subhedral zircons (Figs. 5 and 6). Triassic zircons have a 2005; McCourt et al., 1996), there is no other evidence to support spread of εHf values that can be produced either by the introduction of provenance of the Mesozoic ‘red-beds’ from this region. The most ‘juvenile’ material into the melt (e.g. Belousova et al., 2006)orby likely primary source rocks for the Jurassic zircons in the Mesozoic melting of inhomogeneous basement (e.g. Howard et al., 2009). fluvial–alluvial sedimentary rocks and, hence in river sands recycled However, there is no evidence of juvenile component in this zone and from them, are minor rhyolites that are locally interbedded with these the presence of the old zircon cores supports the latter mechanism. ‘ ’ C red-beds (e.g. Hutchison, 1989; Racey, 2009). Nevertheless, because TDM and εHfN0 in Mesoproterozoic cores suggest a minor mantle- I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039 1037 derived input at around 1.1–1.2 and 1.6 Ga (Fig. 7). However, there Malay Peninsula samples. These grains are most likely recycled from are few zircons of these ages in the samples analysed, which may areas outside the SE Asian region. C indicate that Mesoproterozoic granitoids are not abundant. TDM of three Palaeoproterozoic grains between 2.64 and 2.97 Ga suggest a 6.5. Detrital zircon as an indicator of the tin belt provenance minor contribution from Neoarchaean basement beneath the Sibu- masu Block. This is supported by the observation of two zircon cores Sundaland has been emergent or submerged to very shallow water with ages of 2.5 and 2.8 Ga. depths since the Early Mesozoic (Hall, 2009a). Throughout this period local landmasses have shed large volumes of detrital material to nearby areas. Different Phanerozoic histories of the Sundaland 6.4.4. Summary basement fragments have generated provenance-diagnostic detritus, – U Pb and Hf-isotope data presented in this study support previous specific to particular source provinces. interpretations that NW Sundaland lies on chronologically heteroge- Previous provenance studies in Sundaland (Clements, 2008; van neous basement (Fig. 10). The basement of the Sibumasu Block is Hattum, 2005; van Hattum et al., 2006) have shown that the tin belt – mostly Palaeoproterozoic, around 1.9 2.0 Ga old. There are also granitoids, including the Malay Peninsula, were an important source probably minor Mesoproterozoic (1.6 Ga) and Neoarchaean (2.8 Ga) of siliciclastic detritus in the region. Despite this, almost no studies crustal components. The basement of the East Malaya Block is also have attempted to characterise material derived from this significant – Palaeoproterozoic, around 1.7 2.0 Ga, but younger than that of the SE Asian source area. The purpose of this section is therefore to Sibumasu Block. Late Archaean to Early Proterozoic crustal compo- identify detrital zircon signatures characteristic to different source nents, ranging from 2.3 to 2.7 Ga, are also present in the East Malaya provinces in the Malay Peninsula. Block. It is difficult to distinguish between the Main Range and Eastern Data presented in this study are broadly consistent with the three Province based on U–Pb dating alone, as there is an overlap in the fi Palaeoproterozoic crust-formation episodes identi ed in mainland SE zircon ages. However, distinctively different 176Hf/177Hf values of – Asia by Bodet and Schärer (2000), taking place at 2.5 Ga, 2.2 2.3 Ga Triassic zircons derived from the Eastern and Main Range Provinces – – and 1.9 2.0 Ga. A number of Mesoproterozoic Early Palaeozoic can be used to refine provenance interpretations based on U–Pb episodes of granitoid production can also be recognised in detrital methods. Negative εHf (−7.8 to −13.4) values are typical of zircons zircon populations from the Sibumasu and East Malaya Blocks. Some from crustally-derived Triassic Main Range Province granitoids, of these zircons show rounded morphologies and frosted surfaces and whereas Late Permian–Late Triassic zircons sourced from the mixed are therefore best interpreted as recycled from sedimentary rocks. crust- and mantle-derived Eastern Province granitoids have εHf These grains may therefore represent magmatic episodes outside the around −4.5 and +9.2. This difference can be used as a provenance area of Sibumasu and East Malaya. indicator. The lack of Mesoarchaean and Palaeoarchaean grains is a striking Cretaceous granitoids are only locally common in the Malay C feature of both blocks. Ten Precambrian grains have TDM between 3.21 Peninsula and their erosional products are not expected to be and 4.18 Ga, but there is only one 3.34 Ga detrital zircon core in the consistently abundant in the material derived from this area. However, if present, zircons from the Stong Migmatite Complex can be distinguished from those of other Cretaceous sources in Sundaland by their 70–85 Ma age. Most Cretaceous granitoids in Sundaland are older than 80 Ma (Hall, 2009b). Small amounts of Precambrian zircons are expected in detritus derived from the tin belt, but their similar U–Pb and Hf-isotopic compositions do not allow more precise provenance identification. Some of the material from the Malay Peninsula is likely to be recycled from the Mesozoic and Palaeozoic siliciclastic sedimentary rocks that overlie the basement in places. Therefore, the presence of the Early Palaeozoic and Precambrian zircons is also expected in the detrital material derived from such pre-existing sediments. We suggest that our method of assessing the provenance characteristics of the Malay Peninsula by the sampling of river sediments is arguably more robust than U–Pb and Hf investigations of the granitoids themselves, since Condie et al. (2009) point out that there may be instances when detrital rocks contain zircons from basement lithologies that have been completely removed by erosion, or are hidden beneath younger sedimentary/volcanic cover. By sampling river sands in close proximity to the granitoids we are also confident that these ages reflect a granitoid signature typical to each region rather than to a restricted sampling locality that perhaps represents only an individual magmatic event in the complex development of the pluton as a whole.

7. Conclusions

1. U–Pb detrital zircon ages reveal that magmatism in the Eastern Province of the Malay Peninsula occurred in two distinct episodes: Permian and Early-Middle Triassic. Hf-isotope data identify Fig. 10. Cartoon showing age of basement fragments beneath the Malay Peninsula. Base different magma sources for these zircon populations, suggesting map modified from Sone and Metcalfe (2008). a complex history for the Palaeo-Tethyan subduction of oceanic 1038 I. Sevastjanova et al. / Gondwana Research 19 (2011) 1024–1039

crust and the Sibumasu–East Malaya collision and destruction of Terrane Assemblage, Germany — U–Pb and Hf isotope evidence from detrital – – zircons. Gondwana Research 17, 223 235. Palaeo Tethys. Barber, A.J., 2000. The origin of the Woyla Terranes in Sumatra and Late Mesozoic 2. The data presented here do not resolve the argument as to whether evolution of the Sundaland margin. Journal of Asian Earth Sciences 18, 713–738. the Sibumasu–East Malaya collision occurred in the Late Permian– Barber, A.J., Crow, M.J., 2009. Structure of Sumatra and its implications for the tectonic – assembly of Southeast Asia and the destruction of Paleotethys. Island Arc 18, 3–20. Early Triassic or in Middle Triassic Late Triassic time. However, Baum, F., von Braun, E., Hahn, L., Hess, A., Koch, K.-E., Kruse, G., Quarch, H., Siebenhüner, detrital zircon ages do not support tectonic models that argue for M., 1970. On the geology of northern Thailand. Beihefte zum Geologischen collision after the Late Triassic. Jahrbuch 102, 23. fi 3. The basement of the Malay Peninsula is chronologically heteroge- Belousova, E.A., Grif n, W.L., O'Reilly, S.Y., 2006. Zircon crystal morphology, trace element signatures and Hf Isotope composition as a tool for petrogenetic modelling: neous. The basement of the Sibumasu Block is ~1.9–2.0 Ga old examples from Eastern Australian granitoids. Journal of Petrology 47, 329–353. including some components around 2.8 Ga. The basement of the Belousova, E.A., Reid, A.J., Griffin, W.L., O'Reilly, S.Y., 2009. Rejuvenation vs recycling of – Archean crust in the Gawler Craton, South Australia: evidence from U–Pb and Hf- East Malaya Block is ~1.7 2.0 Ga old with some older (2.7 Ga) – fi isotopes in detrital zircon. Lithos 113, 570 582. components. There is no rm evidence of Archaean basement older Bignell, J.D., Snelling, N.J., 1977. K–Ar ages on some basic igneous rocks from Peninsular than 2.8 Ga beneath the Malay Peninsula. Malaysia and Thailand. Bulletin. Geological Society of Malaysia 8, 89–93. 4. U–Pb ages and Hf-isotope compositions in detrital zircons from the Blichert-Toft, J., Albarède, F., 1997. The Lu–Hf isotope geochemistry of chondrites and the evolution of the mantle–crust system. Earth and Planetary Science Letters 148, Malay Peninsula suggest that juvenile magmatic input increases 243–258. eastwards. The major feature of the Western Zone is reworking of Bodet, F., Schärer, U., 2000. Evolution of the SE-Asian continent from U–Pb and Hf pre-existing Proterozoic crust and the lack of firm evidence for isotopes in single grains of zircon and baddeleyite from large rivers. Geochimica et – fi Cosmochimica Acta 64, 2067 2091. juvenile magmatism. The Central Zone has a signi cant contribu- Carter, A., Bristow, C.S., 2003. Linking hinterland evolution and continental basin tion of both Proterozoic and Archaean crustal components with a sedimentation by using detrital zircon thermochronology: a study of the Khorat minor juvenile contribution. The Eastern Zone has the most Plateau Basin, eastern Thailand. Basin Research 15, 271–285. Carter, A., Moss, S.J., 1999. Combined detrital-zircon fission-track and U–Pb dating: a significant juvenile input during the Triassic magmatism, mixed new approach to understanding hinterland evolution. Geology 27, 235–238. with Proterozoic and Archaean crustal components. Clements, B., 2008. Paleogene to Early Miocene tectonic and stratigraphic evolution of 5. U–Pb and Hf-isotope signatures of Permian, Triassic and Cretaceous West Java, Indonesia. PhD Thesis, Royal Hollloway University of London, p. 431. – zircons are useful indicators of provenance from different granitoid Clements, B., Hall, R., 2008. U Pb dating of detrital zircons from West Java show complex Sundaland provenance, Indonesian Petroleum Association. Thirty-Second provinces within the SE Asian tin belt. Triassic zircons derived from Annual Convention and Exhibition, Jakarta, pp. 1–18. the Main Range Province granitoids can be distinguished from Clements, B., Burgess, P.M., Hall, R., Cottam, M.A., in press. Subsidence and uplift by similar-age zircons shed from the Eastern Province granitoids by slab-related mantle dynamics: A driving mechanism for the Late Cretaceous and ‘ ’ Cenozoic evolution of continental SE Asia, In: Hall, R., Wilson, M.E., Cottam, M.A. their crustal Hf-isotope signatures. (Eds.), The SE Asian gateway: history and tectonics of Australia-Asia collision. Geological Society, London, Special Publications. Cobbing, E.J., 2005. Granites. In: Barber, A.J., Crow, J., Milsom, J.S. (Eds.), Sumatra: Acknowledgements Geology, Resources and Tectonic Evolution: Geological Society Memoirs, No. 31, pp. 54–62. London,. Cobbing, E.J., Pitfield, P.E.J., Darbyshire, D.P.F., Mallick, D.I.J., 1992. The granites of the South- We would like to thank Dr. Anthony Barber and Dr. Michael Crow East Asian tin belt: Overseas Memoir of the British Geological Survey, 10, p. 369. for the critical reviews and useful discussions of possible tectonic Condie, K.C., 1989. Plate tectonics & crustal evolution. Pergamon Press plc, Oxford, models that significantly improved our interpretation. We are also p. 476. Condie, K.C., Belousova, E., Griffin, W.L., Sircombe, K.N., 2009. Granitoid events in space grateful to everybody in the SE Asia Research Group and GEMOC ARC and time: constraints from igneous and detrital zircon age spectra. Gondwana National Key Centre, particularly to Dr. Michael Cottam, Dr. Ian Research 15, 228–242. Watkinson, Simon Suggate, Lanu Cross, Duncan Witts, Professor Tom England, P.C., Thompson, A.B., 1984. Pressure–temperature–time paths of regional metamorphism I. Heat transfer during the evolution of regions of thickened Andersen, Shelley Alchurch, and Dr. Ayesha Saeed. Dr. Andrew Carter continental crust. Journal of Petrology 25, 894–928. is thanked for help with the analytical work. Dr. Azman Ghani is Faure, G., Mensing, T.M., 2004. Isotopes: Principles and Applications. Wiley, p. 897. thanked for help with fieldwork. Professor Matthew Thirlwall and Gobbett, D.J., 1973. Carboniferous and Permian correlation in Southeast Asia. Bulletin. – Dr. David Alderton are thanked for the helpful discussions. We also Geological Society of Malaysia 6, 131 142. Gobbett, D.J., Hutchison, C.S., 1973. Geology of the Malay Peninsula (West Malaysia and thank Dr. Maria Mange and Professor Ian Metcalfe for their Singapore). Wiley Intersciences, New York, p. 438. constructive reviews that improved the final version of the manu- Griffin, W.L., Pearson, N.J., Belousova, E., Jackson, S.E., van Achterbergh, E., O'Reilly, S.Y., Shee, script. 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