Peninsular Malaysia Transitional Geodynamic Process

GR-02530; No of Pages 17 Gondwana Research 94 (2021) xxx–xxx

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Peninsular Malaysia transitional geodynamic process from Gondwana to Pangaea: New constraints from 500 to 200 Ma magmatic zircon U-Pb ages and Hf isotopic compositions

LongXiang Quek a,b,Yu-MingLaia,⁎, Azman A. Ghani b, Muhammad Hatta Roselee b,d, Hao-Yang Lee c, Yoshiyuki Iizuka c, Mohd Rozi Umor d,MarkPechae, Yu-Ling Lin a, Rezal Rahmat c,AzmiahJamilb a Department of Earth Sciences, National Taiwan Normal University, Taipei, Taiwan b Department of Geology, University of Malaya, Kuala Lumpur, Malaysia c Institute of Earth Sciences, Academia Sinica, Taipei, Taiwan d Department of Earth Sciences and Environmental, Faculty of Science and Technology, Universiti Kebangsaan Malaysia, Bangi, Selangor, Malaysia e Arizona Laserchron Center, Department of Geosciences, University of Arizona, AZ, United States article info abstract

Article history: The geodynamic process from the evolution of supercontinent has distinct isotope characteristics explorable Received 1 July 2020 using zircon Hf isotopic composition. Since Peninsular Malaysia associates with Gondwana dispersal and Pangaea Received in revised form 23 January 2021 formation, analyzing the U-Pb and Hf-isotopic content of its 500–200 Ma magmatic zircon could reveal the signal Accepted 2 March 2021 left by the transitional geodynamic process between the supercontinents. We collected two groups of magmatic Available online 05 March 2021 rocks from West Malaya: Ordovician meta-volcanics (n = 8), and Triassic Main Range granitoid province (MRGP) Editor: S. Kwon (n = 6); and three groups from East Malaya: Carboniferous meta-volcanics (n = 2), Permian-Triassic Eastern granite province (EGP) (n = 6), and Permian-Triassic EGP volcanics (n = 8). Difference in magmatic zircon Hf isotopic crustal model ages uphold the previous rationale which separates Peninsular into two blocks: West Ma-

Keywords: laya (part of Sibumasu terrane) magmatic zircon Hf isotopic crustal model ages (Average TDM2: 1.3 Ga) are older Zircon U-Pb age and Hf isotope than East Malaya (part of Chanthaburi-Sukhothai-Lincang arc of Indochina terrane) (Average TDM2: 0.9 Ga). Dur- Supercontinent cycle ing the ﬁnal assembly of Gondwana from 500 to 450 Ma, West Malaya and East Malaya were at the outboard of Pangaea Gondwana Proto-Tethys margin. The shift of East Malaya zircon Hf array towards higher εHf(t) (external orogenic Gondwana system) after ca.370 Ma may infers Paleo-Tethys ocean broadening and East Malaya separation from Gondwana. Peninsular Malaysia The 370–350 Ma juvenile zircon Hf isotopic composition in East Malaya is a signiﬁcant improvement over radiolarian age to show the broadening and subduction of the Paleo-Tethys ocean between the two terranes. After

ca.280 Ma, East Malaya zircon Hf array shifted towards lower εHf(t) (internal orogenic system). Coinciding with the Indosinian collision at ca.230 Ma, crustal reworking signal increases in both blocks, signifying the end in Peninsular Malaysia Gondwana to Pangaea transitional geodynamic process. As the Paleo-Tethys segment was completely subducted after 230 Ma, the peninsular crustal thickening starts from 230 to 218 Ma. The post-collision phase would begin at ca.215 Ma. © 2021 International Association for Gondwana Research. Published by Elsevier B.V. All rights reserved.

1. Introduction system, supercontinent fragmentation occurs when newly formed crust

(more radiogenic, hence trend towards higher εHf(t)) replaces the Two contrasting types of Earth's orogenic systems occur throughout lower crust and lithospheric mantle between two continent fragments the Phanerozoic according to zircon Hf isotope evolution: external and (Collins et al., 2011; Roberts, 2012). For the internal orogenic system, internal systems, which imitate two global-scale mantle convection supercontinent assembly consumes the interior ocean between the con- cells that drive the supercontinent cycle (Cawood et al., 2016; Collins tinental fragments through subsequent subduction. The continental et al., 2011; Murphy et al., 2009; Roberts, 2012). In the external orogenic fragments eventually collide, where a more “continental” lithosphere

(less radiogenic, hence the trend towards lower εHf(t)) replaces the lower crust and lithospheric mantle underneath the overriding conti- ⁎ Corresponding author at: Department of Earth Sciences, National Taiwan Normal University, No.88, Sec. 4, Tingzhou Road, Taipei 11677, Taiwan. nent fragment (Collins et al., 2011; Roberts, 2012). Detrital and mag- E-mail address: [email protected] (Y.-M. Lai). matic zircon Hf isotopic evolution from continental fragments may

Please cite this article as: L. Quek, Y.-M. Lai, A.A. Ghani, et al., Peninsular Malaysia transitional geodynamic process from Gondwana to Pangaea: New constraints from 5..., Gondwana Research, https://doi.org/10.1016/j.gr.2021.03.001 L. Quek, Y.-M. Lai, A.A. Ghani et al. Gondwana Research 94 (2021) xxx–xxx show the distinct characteristics of the internal and external orogenic Majority of Peninsular Malaysia magmatic rocks (Fig. 1) are Late Pa- systems which could unravel fine details regarding the continental frag- leozoic to Mesozoic and divided into three groups: (1) Permian-Triassic ment geodynamic transitional process between supercontinents. Eastern granite province (EGP) granitoid, (2) Late Triassic Main Range The idealized supercontinent cycle suggests periodicity in the timing granite province (MRGP) granitoid (Cobbing et al., 1992; Liew and of dispersal and re-amalgamation of supercontinents (Nance et al., McCulloch, 1985; Liew and Page, 1985; Liew, 1983; Ng et al., 2015a, 1988). Although the time lag between assembly and dispersal of the su- 2015b; Searle et al., 2012), and (3) Permian-Triassic EGP volcanic percontinent increase because of Earth's slowing radiogenic decay rocks. Also, we discovered two more previously unidentified groups of (Senshu et al., 2009), the general agreement is that Gondwana amal- Early and Middle Paleozoic magmatism with new field locations and gamation occurs from 640 Ma to 540 Ma, and that Pangaea formed at the aid of zircon U-Pb isotope analyses: (4) Early Carboniferous meta- around 250 Ma before its dispersal by around 200 Ma (Meert and volcanics in Langat river basin, and (5) Early to Middle Ordovician Lieberman, 2008; Roberts, 2012; Santosh et al., 2009; Senshu et al., meta-volcanics (Quek et al., 2018) in Gerik-Temenggor and Dinding 2009). Sizeable groups of continents underwent geodynamic transi- area. Because of terrain complexity, though Late Paleozoic to Mesozoic tional process from Gondwana to Pangaea during the time lag of around magmatic rocks are being actively studied from a decade ago, the 400 Ma (Roberts, 2012; Senshu et al., 2009). As Peninsular Malaysia is correlation between the magmatic suites and with the older Paleozoic free from significant post-200 Ma tectono-thermal events and associ- magmatic rocks remains poorly constrained. In this study, we present ates with the large groups of continental fragments in the geodynamic U-Pb ages (17 samples) and Hf isotope data (30 samples) on transitional process of Gondwana dispersal and Pangaea formation, its 500–200 Ma magmatic zircon from these magmatic rock groups, com- diverse magmatic rocks 500–200 Ma zircon might provide valuable iso- bined with unpublished data, aiming at delineating and improving topic evolution information regarding the geodynamic transitional (1) the Indosinian collision model of Peninsular Malaysia, (2) the evolu- process. tion of Peninsular Malaysia's Paleo-Tethys ocean segment, and (3) the

Fig. 1. Simpliﬁed Peninsular Malaysia geological map showing the distribution of magmatic rocks and compiled previous studies data. Previous studies data are from Liew (1983), Liew and Page (1985), Liew and McCulloch (1985), Searle et al. (2012), Oliver et al. (2014), Ghani et al. (2014), Ng et al. (2015b), Basori et al. (2016), Jamil et al. (2016), Quek et al. (2017, 2018) and Liu et al. (2020).

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Fig. 2. Representative cathodoluminescence (CL) images of selected zircon grains extracted from Peninsular Malaysia igneous rock. Small red circles indicate the U-Pb dating spot positions while larger blue circles indicate the spot sites of Hf isotope analyses. The circle diameters show the approximate laser spot sizes. (For interpretation of the references to colour in this ﬁgure legend, the reader is referred to the web version of this article.) transitional geodynamic process from Gondwana dispersal to Pangaea 2004). Sundaland regional tectonic is intricate and abstruse, as it is a amalgamation perceived in Peninsular Malaysia. combination of multiple small, ancient crust fragments. Peninsular Malaysia originates from two Gondwana-derived continental blocks, 2. Geological background and previous studies West Malaya (part of Sibumasu terrane) and East Malaya (linked to Chanthaburi-Sukhothai-Lincang arc of Indochina terrane) (Dodd et al., 2.1. Tectonic framework 2019; Gillespie et al., 2019; Metcalfe, 2013a, 2013b; Wang et al., 2018). During the Early Paleozoic, Proto-Tethys ocean subduction and Peninsular Malaysia which hinges by the Isthmus of Kra and lies at associated orogenic events take place at the north of Gondwana (Lin the southeastern tip of Asia, is the oldest core of Sundaland, a non- et al., 2013; Zhang et al., 2018). This episode leaves behind traces of cratonic and heterogeneous exposed landmass (Currie and Hyndman, magmatic rocks such as the Ordovician volcanics in West Malaya 2006; Hall and Sevastjanova, 2012; Hall, 2017; Hall and Morley, (Quek et al., 2018). The northward's migration of continental blocks

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Table 1 subduction drags Sibumasu terrane northwards, and the terrane collided LA ICP-MS operating conditions and data acquisition parameters. with Indochina terrane in Late Triassic. (Hutchison, 1975, 1994, 2014; Laboratory & Metcalfe, 2000, 2013a, 2013b). Serpentinite and Middle to Late Paleozoic Sample radiolarian chert from the Bentong-Raub suture zone (BRSZ) are the key Preparation evidence of the closed Paleo-Tethys ocean segment (Hutchison, 1977; Laboratory name Institute of Earth Sciences, Academia Sinica Jasin, 2018; Jasin and Aziz Ali, 1997; Metcalfe, 2000; Spiller and Sample Magmatic zircon Metcalfe, 1995). Although there is magmatic evidence for the Permian- type/mineral Triassic Paleo-Tethys ocean subduction and Late Triassic collision (Ng Sample Conventional mineral separation, 1-in. resin mount, 1 μm preparation polish to finish et al., 2015a, 2015b), evidence suggesting the separation of Peninsular Imaging CL, JEOL JSM-7100F Malaysia was primarily from the distinct Middle to Late Paleozoic rock formations and fossils resulting from contrasting paleo-latitude positions Laser ablation system (Metcalfe, 2000, 2011, 2013b). Make, Model & type Photon Machines Analyte G2 laser ablation system Ablation cell & volume HelEx cell 2.2. Volcanism Laser wavelength (nm) 193 nm Pulse width (ns) 4 ns − − Only 10% of Peninsular Malaysia volcanic rock is at West Malaya. Fluence (J.cm 2) 5.33 J.cm 2 Repetition rate (Hz) 5 Hz They are dominantly older than the 90% volcanic rock of East Malaya, Ablation duration (sec) 50 s the product of the Permian-Triassic Paleo-Tethys ocean subduction Spot diameter (μm) 35 μm and Indosinian orogenic events. The West Malaya Ordovician meta- Sampling mode / pattern Spot ablation volcanics is best represented by the Early Paleozoic Gerik-Temenggor Carrier gas He Cell carrier gas flow (l/min) Mass Flow Controller 1 (MFC 1): 0.5 l/min meta-volcanic rocks exposed at northern Peninsular Malaysia (Fig. 1) Mass Flow Controller 2 (MFC 2): 0.2 l/min (Hutchison, 1973; Jones, 1970, 1973; Quek et al., 2018). Contemporane- ous Early Paleozoic meta-sedimentary rocks (Jerai formation, ICP-MS Instrument Machinchang Formation, Tarutao Formation, etc.) with the meta- Make, Model & type Agilent 7500 s volcanic rocks suggest explosive volcanism under sub-aerial to marine quadrupole ICP-MS conditions (Jones, 1970). The meta-volcanic rocks include meta-lithic RF power (W) 1500 W tuff, meta-rhyolite, and meta-crystal tuff (Jones, 1970; Quek et al., Make-up gas flow (l/min) Ar 1.25 l/min Detection system Electron multiplier 2018). Unlike the meta-rhyolite and meta-crystal tuff which composed Masses measured 206–208, 232, 238 of primarily volcanic materials, the meta-lithic tuff comprises a signifi- Integration time per peak/dwell times (ms); 10 ms for 232 cant quantity of terrigenous material (Quek et al., 2018). There is a quadrupole settling time between mass jumps 15 ms for 206, 238 somehow limited presence of Middle Paleozoic (Carboniferous) 30 ms for 207, 208 Rephens meta-volcanic rocks at the south of West Malaya (Fig. 1) Sampling period (sec) ~0.12 s Instrument tuning NIST 610 for tuning. (Shu, 1989). The effects of thermal metamorphism are palpable in the ~250,000 cps in 89Y Rephens meta-volcanic rocks and earlier researchers report at least three volcanic rock types: rhyolite-like volcanic rock, meta-lithic tuff, Data Processing and meta-crystal tuff (Shu, 1989). Research into these meta-volcanics Gas blank 50 s is unfinished and reliable isotope age data is deficient because of com- š Calibration strategy GJ-1 used as primary reference material, Ple ovice & 91,500 plex terrain and dense forest. used as secondaries/validation Reference Material GJ-1 (Jackson et al., 2004) The younger Permian-Triassic EGP volcanic rocks are widespread on info 91,500 (Wiedenbeck et al.,1995) East Malaya (Fig. 1) and the volcanic distribution shows a close associa- Plešovice (Sláma et al., 2008) tion with the Middle Paleozoic meta-sedimentary rocks (Hutchison, Data processing Agilent TRA software, Glitter 4.4.4 1973; Ghani, 2009a; Ng et al., 2015b). Permian volcanic rocks have a package used wider distribution from basalt to rhyolite while Triassic volcanic rocks Common-Pb Common-Pb correction by Andersen (2002) correction are commonly felsic composition (Metcalfe et al., 1982; Metcalfe, Quality control / Plešovice – Weighted average 206Pb/238U age = 334 2013b). Metcalfe (2013b) and Hutchison (2014) interpreted the volca- Validation ± 4 Ma (2σ, MSWD = 0.15, n = 18). 91,500 – Weighted nism in East Malaya as the southern continuation of Sukhothai volcanic 206 238 average Pb/ U age = 1059 ± 12 Ma (2σ, arc in Thailand and the composition change from intermediate to felsic MSWD = 0.13, n = 16); Weighted average 207Pb/206Pb in the volcanic rocks represent a progression from subduction to colli- age = 1072 ± 14 Ma (2σ, MSWD = 0.42, n = 16); Systematic uncertainty for propagation is 2% (2σ) sion as the Paleo-Tethys ocean closed. Although the EGP volcanic rocks relate with the EGP granitoid temporally, only limited geochemical and isotopic data are available for the volcanic rocks compared to from Gondwana after Early Paleozoic closely relates to the evolution of their granitoid counterpart. Together with the EGP volcanic rocks, the the Tethyan basins. Indochina terrane rifted away from Gondwana dur- uncommon Late Triassic MRGP volcanic rocks of West Malaya are also ing the formation of Paleo-Tethys ocean in Middle Devonian, while the product of the Paleo-Tethys ocean subduction and Indosinian oro- Sibumasu terrane rifted away during the formation of Meso-Tethys genic events. They are best exemplified by Genting Sempah volcanics, ocean in Early Permian (Metcalfe, 2013a). which is about 50 km to the east of Kuala Lumpur. The volcanic rock East Malaya was free of Late Paleozoic glaciation because of Indochina mainly comprises rhyodacite and orthopyroxene rhyodacite (Ghani, terrane earlier rifting from Gondwana, and instead developed warm 2000; Ghani and Singh, 2005; Liew, 1983). The Genting Sempah volca- equatorial flora and fauna (typical Cathaysian) (Kon'no and Asama, nics are relatable with the Late Triassic MRGP granitoid magmatism be- 1970; Kon'no et al., 1971; Hutchison, 1994, 2014). As West Malaya of cause of their comparable geochemistry (Ghani and Singh, 2005) and Sibumasu terrane did not begin rifting from Gondwana until Early Perm- overlapping zircon U-Pb ages (Ng et al., 2015b). ian, it was characterized by Carboniferous-Permian cold-water fauna (Shi and Waterhouse, 1991) and Carboniferous glaciomarine diamictites 2.3. Plutonism (Metcalfe, 2011). After Early Permian, the portion of the Paleo-Tethys ocean that opened between West and East Malaya diminished from The Permian-Triassic EGP granitoid (40%) and the Late Triassic MRGP the northward subduction under East Malaya (Metcalfe, 2000). The granitoid (60%) (Fig. 1)reflect the Permian-Triassic Paleo-Tethys ocean

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Table 2 Peninsular Malaysia magmatic zircon samples data for this study.

Sample Magmatic rock group Latitude (°N) Longitude (°E) U-Pb Age (Ma) Hf analyses n, grain analyzed

West Malaya Jerai-1 Ordovician meta-volcanics 5.79597 100.43722 481 ± 4 10 Dind-1 Ordovician meta-volcanics 3.20478 101.77751 479 ± 3 16 Siput-1 Ordovician meta-volcanics 4.98164 101.17745 476 ± 4 15 Temng-1 Ordovician meta-volcanics 5.40873 101.29929 474 ± 3 16 Lebey-1 Ordovician meta-volcanics 5.43364 101.20792 473 ± 3 15 Lawin-1 Ordovician meta-volcanics 5.30656 101.05632 471 ± 5 13 Siput-2 Ordovician meta-volcanics 4.85477 101.13404 462 ± 4 15 Beru-1 Ordovician meta-volcanics 5.39363 101.33999 460 ± 2 15 Rep-1 Carboniferous meta-volcanics (xenocrysts) 3.11628 101.91567 448 ± 6 12 Carboniferous meta-volcanics 354 ± 4 9 Gab-1 Carboniferous meta-volcanics (xenocrysts) 3.17390 101.91600 444 ± 7 19 Carboniferous meta-volcanics 343 ± 4 21 9100 Triassic MRGP granitoid 5.59552 100.86842 224 ± 1 26 3300 Triassic MRGP granitoid 4.55000 101.31667 220 ± 2 10 TT11 Triassic MRGP granitoid 4.56667 101.30000 220 ± 2 10 LS1 Triassic MRGP granitoid 2.97828 102.06139 219 ± 3 10 J5 Triassic MRGP granitoid 3.06794 102.11142 218 ± 2 11 SS Triassic MRGP granitoid 5.01326 100.83483 216 ± 1 15 East Malaya BES5 Permian-Triassic EGP 2.43568 103.97854 282 ± 2 15 TG4 Permian-Triassic EGP 2.47814 103.95911 281 ± 2 13 MBJ10 Permian-Triassic EGP 5.36711 103.03097 275 ± 3 10 ENDAU Permian-Triassic EGP volcanics 2.51132 103.83485 279 ± 2 12 Kn6 Permian-Triassic EGP 3.81733 103.37414 262 ± 3 15 KYR8 Permian-Triassic EGP volcanics 5.05110 102.57939 250 ± 7 5 KUL01 Permian-Triassic EGP volcanics 1.64681 103.55322 249 ± 2 10 DIGI Permian-Triassic EGP 4.31706 103.48350 246 ± 2 15 B8 Permian-Triassic EGP volcanics 5.27453 102.26486 237 ± 1 15 TRPR Permian-Triassic EGP volcanics 1.37049 104.26455 234 ± 2 7 SY3 Permian-Triassic EGP 4.01058 101.95892 226 ± 3 12 MUQ Permian-Triassic EGP volcanics 5.39686 102.24205 225 ± 1 16 SJQR4 Permian-Triassic EGP volcanics 3.93089 102.27514 214 ± 1 13 TENG Permian-Triassic EGP volcanics 4.80797 103.67881 213 ± 1 7

subduction and subsequent Sibumasu-Indochina collision (Hutchison, Ignoring several tiny outlying plutons, two major batholiths (Fig. 1), 1977). Comprehensive geochemical investigations and age studies ad- the larger Main Range batholith, and the medium-sized Bintang batho- vocate that the EGP granitoid formed in a subduction-related setting, lith represent the MRGP granitoid. The main granitoid facies is textur- while the voluminous MRGP granitoid developed in a syn-topost- ally coarse to very coarse-grained megacrystic biotite-muscovite collisional setting (Liew, 1983; Ghani, 2009b; Ng et al., 2015a, 2015b). granite and the primary mineralogy is K-feldspar, plagioclase, quartz The EGP granitoid mainly consists of granodiorite-monzogranite with and high Al-biotite (Ghani, 2000 ; Ghani et al., 2013b; Ng et al., 2015a). predominantly I-type affinities in zoned and un-zoned plutons (Ghani, Meta-sedimentary xenoliths and biotite rich micro-granular enclaves 2005; Ghani et al., 2013b; Ng et al., 2015a). The MRGP granitoid primar- are prevalent in this granitoid facies (Ghani et al., 2013b). The ily comprises syenogranite and monzogranite with subordinate grano- melanocratic amphibole-bearing granitoid is infrequent compared to diorite with a mixed S- and I-type characters in large batholith or the main granitoid facies and appear within the Taiping (Bintang bath- complex plutons (Liew, 1983; Cobbing et al., 1992; Ghani, 2000, 2005; olith) and Kuala Kelawang granite complexes (Main Range batholith) Ghani et al., 2013b; Ng et al., 2015a; Quek et al., 2015, 2017). The varia- (Ghani et al., 2013b). Besides the regular granite mineral assemblage, tion in geochemistry likewise influences the opaque oxides in the gran- their mafic mineral content comprises low Al biotite, titanite, allanite itoid; MRGP granitoid typically include ilmenite as the principal iron and actinolitic hornblende (Ghani et al., 2013b; Quek et al., 2015, oxide phase, while EGP granitoid is a typical magnetite series granitoid 2017; Ng et al., 2015a). Although many studies have used geochronol- (Ishihara et al., 1979; Ng et al., 2015a; Yeap, 1993). ogy and geochemistry to examine the differences between the EGP Several small batholiths in the northern part and southern part of and MRGP granitoid relating to their tectonic setting, overlapping be- East Malaya represent the EGP granitoid (Fig. 1). The northern part en- tween the two regions still occurs. Time-integrated isotopic evolution compasses the Boundary Range batholith (granite to granodiorite) and data is more accurate and could present in-depth discrimination to the Kapal and Jerong batholiths (dominantly granodiorite) while the this situation (Ng et al., 2015a), but only minimal data is available for southern part includes several medium-sized plutons of hornblende- Peninsular Malaysia. bearing and hornblende-free granitoid (Ghani, 2009b). Throughout the EGP, the granitoid produces very narrow thermal aureoles and 3. Methodology some have miarolitic cavities implying a high-level emplacement (Ghani, 2005). Minor diorite, tonalite and gabbro occur alongside EGP 3.1. Zircon U-Pb geochronology granitoid (sometimes as single plutons or at the edges of granitoid bod- ies) (Cobbing et al., 1992; Ghani, 2005; Ghani et al., 2013b). Previous re- We separated zircon grains from samples using conventional mag- searchers report rare occurrences of alkaline igneous rock such as netic separation and heavy liquid techniques. We analyzed 17 samples syenite on Perhentian Island (284 Ma, Peninsular East Coast) (Ng from: Ordovician meta-volcanics (n = 5), Triassic MRGP (n =6),Car- et al., 2015a, 2015b) and in Benom (226 Ma, Central Peninsular) boniferous meta-volcanics (n = 2) and Permian-Triassic EGP (n =4). (Yong et al., 2004). The alkaline igneous rock main mineralogy is K- Besides Lawin-1 zircon grains, we mounted the other 16 zircon samples feldspar, plagioclase, hornblende, augite, quartz and biotite, in decreas- at the National Taiwan University, Taiwan. Lawin-1 zircon mount is ing abundance (Ng et al., 2015a). Geochemically, the EGP granitoid be- made in Arizona LaserChron Center, The University of Arizona, United long to an expanded calc-alkaline series (Ghani, 2005; Ng et al., 2015a). States. Trained personnel facilitated in the mount's analysis using a

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Fig. 3. (a) Concordia diagrams for zircon U-Pb isotopic ages from Ordovician meta-volcanic and Carboniferous meta-volcanic samples, (b) Triassic MRGP granitoid samples, (c) Permian- Triassic EGP granitoid samples.

Photo Machines Analyte G2 laser ablation (LA) system coupled with 335.2 ± 1.6 Ma (n = 76, MSWD = 0.39, 2σ) respectively. Our results ThermoFinnigan Element2 Inductively coupled plasma mass spectrom- are in perfect agreement with the isotope dilution thermal ionization etry (ICP-MS) and adhering to the procedure developed by Gehrels et al. mass spectrometry (ID TIMS) results reported by Wiedenbeck et al. (2008) and Johnston et al. (2009). We analyzed the zircon mounts (1995) (91,500; 206Pb/238U age: 1062.4 ± 0.8 Ma, 2σ)andSláma et al. made in the National Taiwan University using a Photo Machines Analyte (2008) (Plešovice; 206Pb/238U age: 337.1 ± 0.4 Ma, 2σ). G2 LA system coupled with Agilent 7500 s quadrupole ICP-MS housed at All U-Pb isotopic concentrations were calculated using the GLITTER the Institute of Earth Sciences, Academia Sinica, following analytical 4.4.4 data reduction software for laser ablation microprobe by Geochem- procedures described by Chiu et al. (2013). Cathodoluminescence (CL) ical Evolution and Metallogeny of Continents (GEMOC). Uncertainties images of the zircon mounts (Fig. 2) were taken using a JEOL JSM- are quoted without components related to systematic error unless oth- 7100F scanning electron microscope (SEM) at the Institute of Earth Sci- erwise stated. Systematic uncertainty for propagation is 2% (2σ). The ences, Academia Sinica, Taiwan. common lead correction was done using the procedure suggested by The operating conditions and data acquisition parameters of the LA Andersen (2002). Instead of using an arbitrary discordance filter, we ICP-MS in Academia Sinica are summarized in Table 1. We performed evaluate the issue of discordance according to Spencer et al. (2016). the laser ablation with a helium carrier gas to reduce the deposition of Analyses that overlap the concordia line within uncertainty are consid- ablated material onto the sample surface, which can significantly im- ered “concordant” despite centroid discordance, and if analyses fall off prove transport efficiency and thus increase the signal intensities. The even by a small margin, they are considered “discordant” (Spencer data acquisition time for each spot was about 100 s, i.e. 50 s gas blank et al., 2016). As discordant ages may be meaningful, they are not neces- followed with 50 s ablation. GJ-1 zircon was the standard for instrumen- sarily removed from a statistical population (Spencer et al., 2016). We tal drift correction, and two secondary standard materials (91,500 and rely on 206Pb/238U ages up to 1000 Ma and 206Pb/207Pb ages if the Plešovice) were analyzed during the experiments for consistency 206Pb/238U ages are >1000 Ma, for samples that contain a cluster of anal- check. Our LA ICP-MS 206Pb/238U age weighted average results for the yses with concordant to slightly discordant 206Pb/238U ages of ca.500 Ma secondary standard materials (91,500 and Plešovice) during our analyt- (Gehrels et al., 2006; DeCelles et al., 2007). If the condition is not met, we ical sessions are 1061.6 ± 4.8 Ma (n = 76, MSWD = 0.23, 2σ)and use an empirically derived cutoff age of 1.5 Ga (Spencer et al., 2016). The

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Fig. 3 (continued). plotting of weighted mean U-Pb ages and Wetherill concordia diagrams “juvenile” silicate melts high in 176Hf/177Hf values, while reworking of were carried out using Isoplot v. 4.15 (Ludwig, 2012). the older crust will produce lower 176Hf/177Hf values (Belousova et al., 2010). We analyzed zircon grains selected from 30 samples for 3.2. Zircon Lu-Hf isotopes Hf-isotope composition (Table 2): Ordovician meta-volcanics (n =8), Triassic MRGP (n = 6), Carboniferous meta-volcanics (n = 2), Zircon is a frequent accessory mineral in silicate crustal rocks popu- Permian-Triassic EGP (n = 6), and Permian-Triassic EGP volcanics larly employed for providing magmatic ages through U-Pb geochronol- (n = 8). We conduct Lu-Hf analyses at the same spots or the same ogy. Owing to its high Hf concentration and low Lu concentration, it is age domains for the U-Pb age dating as guided by CL images (Fig. 2). an excellent candidate in Hf isotope studies (Belousova et al., 2010). Trained personnel assisted Lawin-1 zircon Lu-Hf analyses at Arizona Hf isotopes in zircon are particularly advantageous as a tracer for study- LaserChron Center, The University of Arizona using a Nu Plasma HR ing crustal evolution because of its resistance to diffusion and isotopic ICP-MS, coupled to a Photon Machines Analyte G2 laser equipped with exchange (Cherniak et al., 1997), enabling it to preserve the isotopic a LelEX cell, and following the procedure described in Gehrels and composition of the parental magma at the time of crystallization Pecha (2014). We performed the Lu-Hf analyses on the rest of the 29 (Belousova et al., 2010). Partial melting of mantle commonly produces samples using a Nu Plasma multi-collector (MC) ICP-MS, coupled to a

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Fig. 3 (continued).

Photon Machines Analyte G2 LA system, housed at the Institute of Earth are between 1 and 0.1, suggesting they are magmatic zircon from a felsic Sciences, Academia Sinica. and intermediate melt (Hoskin and Schaltegger, 2003; Linnemann et al., Our laser spot analyses at Academia Sinica use a spot diameter of 2011). The meta-igneous rock zircon have reduced Th/U ratio values 50 μm at an energy output of 100% with densities of 5.75 J/cm2 and an (average = 0.57) compared to the igneous rock zircon Th/U ratio values 8 Hz repetition rate. Following a 30s of blank acquisition, typical abla- (average = 0.83). The zircon U-Pb isotopic analyses for each sample are tion times were around 60–90s. 176Hf/177Hf results of the Mud Tank zir- concordant or near-concordant. Weighted mean U-Pb age and con standards during the analysis of this study are 0.282495 ± 0.000028 Wetherill concordia diagrams of analyzed samples are illustrated in (2σ, n = 30), which are similar to the values given by Woodhead and Fig. 3a, b, and c. For the weighted mean ages, we report the uncertainties Hergt (2005) for solution analysis (0.282507 ± 0.000006; n =5)and at 2σ. The weighted averages are representing a single age population, laser ablation microprobe (LAM) (MC) ICP-MS analysis (0.282504 ± as the datasets dispersion fall within the acceptable range for sample 0.000044; n = 158). The stable isotope ratios for the zircon Hf data size at 2σ (neither under dispersed nor over dispersed) defined by (180Hf/177Hf and 178Hf/177Hf) were reported in the supplementary file Spencer et al. (2016). “Geological scatter” in ages are a common phe- to demonstrate the instrument was working properly (Spencer et al., nomenon, and dispersion in geochronological datasets may contain 2020). Lan et al. (2009) gave a detailed description of the analyses. meaningful information such as the magmatic residence time of the MC-ICP-MS instrumental conditions and data acquisition followed crystals (Vermeesch, 2018). All the analyzed zircon U-Pb isotope data those reported by Griffin et al. (2000, 2004).TheεHf(t) values and is in supplementary file 1. crustal model ages in the figures and supplementary file were calculated Except for the new and anomalous age from the two Early Carbonif- using the decay constant (1.867 × 10−11 per year) proposed by erous meta-volcanic sample Rep-1 (354 ± 4 Ma) and Gab-1 (343 ± Söderlund et al. (2004) and Albarède et al. (2006). Calculation of the 4 Ma) collected on the east side of West Malaya (Fig. 3a), other age re- two-stage crustal model ages (TDM2) are according to Lu/Hf ratios sug- sults are consistent with previous data (Fig. 1). These two samples also gested by Bea et al. (2018). contain a significant amount of xenocrystic zircon that form magmatic populations (Rep-1, 448 ± 6 Ma; Gab-1, 444 ± 7 Ma) (Fig. 3a). Five 4. Results Early Ordovician meta-volcanic samples (Jerai-1, Siput-1, Lebey-1, Lawin-1, and Siput-2) from West Malaya report weighted mean U-Pb 4.1. Zircon U-Pb geochronology ages ranging from 462 to 481 Ma (Fig. 3a). Six analyzed Late Triassic MRGP granitoid samples from West Malaya (9100, 3300, TT11, LS1, J5 Zircon grains extracted from 17 magmatic rock samples are and SS) yielded weighted mean U-Pb ages ranging from 220 to euhedral, prismatic to elongate, and colorless to brown-yellow. The 213 Ma (Fig. 3b). They also contain meager inherited zircon with older grains are typically larger than 100 μm and show distinctive magmatic 207Pb/206Pb ages of 1109 Ma, 1272 Ma, and 1863 Ma. Four analyzed oscillatory zoning in CL images (Fig. 2). The Th/U values for all the zircon East Malaya Permian-Triassic EGP granitoid sample provided Middle

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Fig. 4. εHf(t) violin plot for zircon Lu-Hf isotopic data presented in this research.

Permian ages (275–262 Ma from MBJ10 and Kn6) and Early to Middle zircon Hf isotopic composition depletion, with an average εHf(t) value Triassic ages (246 to 226 Ma from DIGI and SY3) (Fig. 3c). Older of −5.1. From Late Ordovician onwards, there is a noticeable shift in 207 206 Pb/ Pb ages are absent in our samples. the εHf(t) values from positive to negative as the magmatic age becomes younger.

4.2. Zircon Lu-Hf isotopes Plots of εHf(t) values vs U-Pb ages of magmatic zircon are displayed in Fig. 5 and Fig. 6a. The Ordovician and Carboniferous zircon Hf isotope We analyzed zircon grains selected from 30 samples (Table 2). All data are novel and not reported by previous studies. Our 300–200 Ma analyzed zircon Lu-Hf isotope data is in supplementary ﬁle 2. We used data point distribution is generally consistent with previous detrital zir- in-situ zircon U-Pb ages for the calculation of εHf(t) and TDM2 values. con from Sevastjanova et al. (2011) and magmatic zircon from Liu et al. The results are summarized as a violin plot in Fig. 4. The Early to Middle (2020). The more radiogenic zircon Hf isotopic composition after Ordovician meta-volcanic samples (8 samples; Jerai-1, Dind-1, Siput-1, 218 Ma was a new ﬁnding not recorded by the previous study. We

Temng-1, Lebey-1, Lawin-1, Siput-2, and Beru-1) have a relatively de- drew two distinct TDM2 evolution reference lines in Fig. 6btoshow pleted (less radiogenic) zircon Hf isotopic composition, with an average two data population; the younger TDM2 evolution line passes through εHf(t) value of −3.3. The Early Carboniferous meta-volcanic samples (2 the data population with positive εHf(t) (largely represented by zircon samples; Rep-1 and Gab-1) and its xenocrysts are more enriched (more from East Malaya) while the older TDM2 evolution line cross through radiogenic) in zircon Hf isotopic composition, with an average εHf data population with negative εHf(t) (dominantly represented by (t) value of 3.6. The East Malaya Permian-Triassic EGP granitoid (5 sam- West Malaya zircon). The zircon Hf isotope crustal model age probabil- ples; BES5, TG4, MBJ10, Kn6, and DIGI) and volcanic (7 samples; KYR8, ity density plot (Fig. 7) also demonstrates that the majority of West Ma-

KUL01, B8, TRPR, MUQ, SJQR4 and TENG) samples similarly display zir- laya TDM2 peaks are older (>1200 Ma) compared to East Malaya con Hf isotopic composition enrichment, with an average εHf(t) value of (<1000 Ma). This indicates the majority zircon from East Malaya are 2.9. Only two samples, SY3 and ENDAU are more depleted, with an av- from a source with a higher juvenile content compared to West Malaya erage εHf(t) value of −6.7. The West Malaya Late Triassic MRGP granit- zircon. Even though zircon Hf crustal model ages provide numerical es- oid (6 samples; 9100, 3300, TT11, LS1, J5 and SS) dominantly show timates of average mantle extraction ages, they are not quantiﬁable ages

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Fig. 5. Plots of εHf(t) values vs U-Pb ages of magmatic zircon from Peninsular Malaysia igneous rock samples. This diagram is plotted using HafniumPlotter by (Sundell et al., 2019)andR detzrcr by (Kristoffersen et al., 2016). The crustal evolution reference lines were calculated using Lu/Hf ratios suggested by Bea et al. (2018).

in strict geochronological sense and are best interpreted qualitatively Indochina terrane which yielded ages suggestive of Late Ordovician (Vervoort and Kemp, 2016). magmatic event, Early Carboniferous tectono-metamorphic event and Permian-Triassic magmatism (Metcalfe, 2013a; Nagy et al., 2001). The 5. Discussion repositioning of Carboniferous meta-volcanics to East Malaya would suggest a Peninsular Malaysia collision model where East Malaya 5.1. Implication to Peninsular Malaysia Indosinian collision model over-thrust over West Malaya. The tectonic model by Oliver et al. (2014) suggested that following the Indosinian collision, West Malaya Our results divide Peninsular Malaysia magmatic zircon into two overrides East Malaya which resulted in the partial melting of the thick- groups using zircon Hf isotopic composition (Fig. 6b). Although the Car- ened crust to generate the MRGP granitoid magma. There are several boniferous meta-volcanics are located at West Malaya, we grouped it weaknesses to this claim. First, the distribution of the Paleo-Tethys with East Malaya magmatic zircon due to similarities in TDM2 evolution ocean accretionary complex on the West Malaya suggests that it should trend or zircon Hf crustal model ages. West Malaya houses two mag- be the other way around. Second, it is unlikely for East Malaya's lower matic rock zircon clusters: (1) Ordovician meta-volcanics, and (2) Trias- crust to be the source of the MRGP granitoid, as MRGP granitoid did sic MRGP granitoid, while East Malaya hosts three magmatic rock zircon not inherit East Malaya's younger magmatic rocks zircon Hf crustal clusters: (1) Carboniferous meta-volcanics, (2) Permian-Triassic EGP, model ages. Ng et al. (2015a) whole-rock Sr isotopic data also suggest and (3) Permian-Triassic EGP volcanics. West Malaya zircon Hf crustal it is unlikely MRGP granitoid elevated 87Sr/86Sr ratios (>0.710) is model ages (average: 1342 Ma) are generally older than East Malaya sourced by the lower 87Sr/86Sr ratios East Malaya lower crust. The over (average: 868 Ma) and this agrees with previous magmatic zircon Hf thrusting model is consistent with several studies of Peninsular isotopic data (Liu et al., 2020)(Fig. 7). The younger crustal ages suggest Malaysia (Ghani et al., 2013a; Metcalfe, 2000; Ryall, 1982), which East Malaya incorporated signiﬁcant juvenile material during its crustal have advocated that West Malaya is thicker than East Malaya and there- evolution. Although Sevastjanova et al. (2011) shows overlapping zir- fore it is more adept in containing the rise of a mantle-derived melt fol- con Hf crustal model ages where West Malaya (1.9 to 2.0 Ga) is only lowing the Indosinian post-collision (Ghani et al., 2013a). marginally older than East Malaya (1.7 to 2.0 Ga), studies using whole-rock Nd isotope on granite (Liew and McCulloch, 1985; Ng 5.2. The evolution of Peninsular Malaysia's Paleo-Tethys Ocean segment et al., 2015a) revealed that West Malaya (1.6 to 2.0 Ga) is older than East Malaya (0.9 to 1.4 Ga). Our results cleared up the inconsistency East Malaya recorded a noticeable juvenile (more radiogenic Hf iso- by using zircon Hf isotopic data to vindicate the idea which separates tope) crust input signal from 370 to 350 Ma (Fig. 6b), indicating the for- Peninsular Malaysia into two distinctive blocks. mation of a new crust. The beginning of this period (ca.370 Ma) Our magmatic record on East Malaya is consistent with the East Ma- coincided with the age of the oldest radiolarian recorded within oceanic laya detrital zircon record (Basori et al., 2016) and previous results on ribbon-bedded chert accreted by the Paleo-Tethys ocean subduction in

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Fig. 6. (a) Zoomed in plots of εHf(t) values vs U-Pb zircon ages of 500–200 Ma magmatic zircon from Peninsular Malaysia igneous rock samples. (b) Re-interpretation of data points from the plot into East and West Malaya.

the BRSZ, which is Famennian (Late Devonian) (Metcalfe, 2000, 2013b). general westerly younging magmatic trend across the Peninsular Metcalfe (2013b) hypothesize that the evolution of Paleo-Tethys ocean (Oliver et al., 2014; Ng et al., 2015b). began in Early Devonian (ca.410 Ma) when Indochina terrane rifted There is evidence of northward Paleo-Tethys ocean subduction as away from Gondwana, and by 370 Ma, a deep Paleo-Tethys ocean has early as Early Carboniferous in Central Qiangtang (Dan et al., 2018; already formed. Although there is inadequate information to support Jiang et al., 2015; Liu et al., 2018; Wang et al., 2017; Wu et al., 2020; an Early Carboniferous subduction in Peninsular Malaysia, presence of Zhai et al., 2018)(Fig. 8a). If subduction started on the west side of Early Carboniferous (ca.350 Ma) obducted ophiolite remnants are re- East Malaya during Early Carboniferous, a peculiar mechanism such as ported at the Longmu Co-Shuanghu suture zone (LSSZ) (Zhang et al., ﬂat slab subduction would have been involved to explain the dormancy 2016), the postulated northern extension of the BRSZ. To date, the and migration of volcanism (Axen et al., 2018; Gutscher, 2018; Gutscher oldest subduction-related magmatic rock discovered in Peninsular et al., 2000). Although this hypothesis remains speculative without fur- Malaysia is Early Permian on the eastern coast of the peninsular (east ther magmatic rock geochemistry and structural evidences, such a side of East Malaya) (ca.292 Ma, zircon U-Pb isotope; ca.296 Ma, mechanism was applied in LSSZ to explain the magmatic migration whole-rock Ar-Ar isotope) (Basori et al., 2016; Ghani, 2009a), with the and dormancy that existed between 345 and 275 Ma (Wang et al.,

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suggests the diachronous closing of the Paleo-Tethys ocean branch, we urge caution in the overinterpretation of these data.

The increase of εHf(t) values at ca.215 Ma (Event 2) in East Malaya after the crustal thickening period could signify the collapse of the orogen (Fig. 6b). West Malaya did not observe such a signature, even though the amalgamation of Peninsular Malaysia begins after 230 Ma. However, in Northern Thailand, the 217–215 Ma extensional collapse is an important feature of Sibumasu terrane (Morley, 2018). The ca.215 Ma juvenile zircon Hf isotope signature is likely pronounced in East Malaya as its crust is thinner compared to West Malaya (Ghani et al., 2013a). This is evident by the conﬁnement of Post-Triassic basaltic dikes in East Malaya (Ghani et al., 2013a). Due to the prolonged arc development in East Malaya, the crust away from the suture zone has weakened; therefore, it is less capable of containing the rise of a mantle-derived melt. In summary, we suggest the contraction phase of the Indosinian collision occurred in Peninsular Malaysia from 230 to 218 Ma, with signiﬁcant zircon preservation potential during this stage, and the post-collision phase started ca.215 Ma.

5.3. Transitional geodynamic process signal from Gondwana to Pangaea

The mildly negative εHf(t) values of the Ordovician meta-volcanics suggest West Malaya endured a crustal reworking from 500 to

450 Ma. On the other hand, the positive εHf(t) values of xenocrystic zircon from Carboniferous meta-volcanics suggest an episode of juvenile crustal input in East Malaya during ca.440 Ma (Fig. 8b). During this period, West Malaya along with the rest of the Sibumasu terrane is at East Gondwana Proto-Tethys margin and underwent widespread magmatism from the subduction of Proto-Tethys ocean (Lin et al., 2013). Although some researchers argue that the Early Paleozoic magmatism on the Proto-Tethys margin represents a magmatic result of the Gondwana breakup (Murphy and Nance, 1991), the majority suggest that they are the artifact of collision during the ﬁnal assembly of Gondwana (Cawood and Buchan, 2007; Hu et al., 2013; Li et al., 2016; Meert and Van Der Voo, 1997). After the collision of the outboard Asian micro-continental fragments end the subduction on the Proto- Tethys margin at ca.490 Ma, crustal thickening occurred at the margin Fig. 7. Probability density plot of zircon Hf crustal model age of magmatic zircon for from 490 to 475 Ma, followed by crustal delamination at 475 to samples from Peninsular Malaysia igneous rocks. The zircon Hf crustal model ages are cal- 450 Ma (Li et al., 2016). The timing of contraction and juvenile crustal culated according to Lu/Hf ratios suggested by Bea et al. (2018). This diagram is con- input in Peninsular Malaysia support the hypothesis that the assembly structed using Isoplot by Ludwig (2012). of the southern supercontinent might have continued beyond the suggested 540 Ma for Gondwana ﬁnal assembly (Fig. 8b).

East Malaya's increasing and decreasing εHf(t) trends during ca.370 Ma and ca.280 Ma are similar to those variations of the external ﬂ 2017). According to Gutscher (2018), the process of attening the and internal orogenic system, respectively (Fig. 8b). Researchers often subducting slab would squeeze out the asthenosphere mantle wedge, link the global zircon database external and internal orogen patterns ending arc magmatism and driving compressional deformation far in- with the dispersal and assembly of supercontinents (Collins et al., board of the trench. It is conceivable that such compressional deforma- 2011; Gardiner et al., 2016), and this transition from an external orogen tion is recorded as a pronounced short-term contraction phase at to an internal orogen is most likely related to the dispersal- ca.280 Ma (Event 1) on East Malaya (Fig. 6b). amalgamation process of Gondwana-Pangaea. The shift of the zircon ε At ca.280 Ma, the Hf(t) values of East Malaya show a decreasing Hf array in East Malaya at 370 Ma towards more primitive composition ﬁ ε trend and nally meets up with the negative Hf(t) values of West Ma- coincides with the timing of dispersal for Gondwana and broadening of laya at 230 Ma (Fig. 6b). The addition of crustal material (less radiogenic the Paleo-Tethys ocean (Fig. 9a). As successive northward-directed oce- Hf isotope) from 230 to 218 Ma indicates crustal thickening from a con- anic subduction (300–250 Ma) continuously transports the rifted Gond- tinental collision (characteristic of an internal orogenic system). We wana continental fragments from the south to Laurussia (the northern propose Peninsular Malaysia's Paleo-Tethys ocean segment ceased to landmass), the dragging force from the subduction will rupture the exist after 230 Ma, and the ensuing continental collision form the major- Gondwana margin to form new continental fragments (Cimmeria) ity of the Triassic MRGP granitoid. This is consistent with previous geo- and oceanic basin (Meso-Tethys ocean) (Wan et al., 2019; Yin, 2010) chemistry and zircon U-Pb age data which show the closure time of (Fig. 9b). The decreasing εHf(t) trend after 280 Ma indicates a higher de- Paleo-Tethys ocean in Peninsular Malaysia and the end of subduction- gree of crustal recycling resulting in evolved magma and zircon Hf iso- related Andean-type magmatism is at 230 Ma (Ng et al., 2015b). Our tope composition (Fig. 8b). As Pangaea amalgamates, crustal suggested collision period for Peninsular Malaysia is slightly younger reworking processes signal in Peninsular Malaysia become increasingly than the syn-collision period suggested by Wang et al. (2018) for the dominant. By ca.230 Ma, the signal of transitional geodynamic process northern extension of the BRSZ, Changning-Menglian and Inthanon su- from Gondwana to Pangaea in Peninsular Malaysia ended when West – ture zone (Thailand), which is 237 230 Ma (Fig. 8a). Although the result Malaya collided with East Malaya.

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Fig. 8. (a) Comparison of εHf(t) values vs U-Pb zircon ages of magmatic zircon from Peninsular Malaysia igneous rock samples with magmatic zircon from Carboniferous Central Qiangtang igneous rock samples (arc-related) and magmatic zircon from Triassic Thailand igneous rock samples (the northern extension of BRSZ). (b) The conceptual evolution of Peninsular Malaysia zircon Hf isotope composition concerning the stages of supercontinent assembly and breakup (modiﬁed after Gardiner et al., 2016).

6. Conclusion 2. The oldest Paleo-Tethys ocean magmatic record in Peninsular Malaysia is East Malaya juvenile crust input signal at 370 to 1. Zircon U-Pb and Hf-isotopic studies performed on 500–200 Ma mag- 350 Ma. They coincided with the age of the oldest radiolarian re- matic zircon from Peninsular Malaysia reveal that West Malaya (part corded within oceanic ribbon-bedded chert accreted by the Paleo- of Sibumasu terrane) which houses: (1) Ordovician meta-volcanics, Tethys ocean subduction in the BRSZ. The short-term contraction and (2) Triassic MRGP granitoid display older zircon Hf crustal phase at ca.280 Ma on East Malaya could be related to a hypothetical model age compared to East Malaya (part of Chanthaburi- mechanism such as ﬂat-slab subduction. Sukhothai-Lincang arc of Indochina terrane) which host: (1) Carbon- 3. Around 230–218 Ma West Malaya collided with East Malaya, coin- iferous meta-volcanics, (2) Permian-Triassic EGP granitoid, and ciding with Indosinian collision. Compiled zircon Hf-isotope evolu- (3) Permian-Triassic EGP volcanics. Our result justiﬁes the previous tion shows West Malaya substituted East Malaya's lower crust in an

model which divides Peninsular Malaysia into two separate terranes. internal orogenic system. The increase of zircon εHf(t) values at ca.215 Ma at East Malaya signiﬁes the collapse of the orogen. The

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Fig. 9. (a) 350 Ma paleogeographic reconstruction showing the dispersal of Gondwana and location of the terranes with simplified plate boundaries (b) ca.280 Ma paleogeographic reconstruction showing amalgamation of Pangaea and the location of the terranes with simplified plate boundaries. The reconstruction is modified after Domeier and Torsvik (2014).

ca.215 Ma juvenile signature is only perceptible in East Malaya be- Review & Editing; Hao-Yang Lee: Methodology, Validation, Resources; cause of crustal thinning from the prolonged arc development. Yoshiyuki Iizuka: Methodology, Resources; Mohd Rozi Umor: Supervi- 4. Ordovician magmatic zircon in Peninsular Malaysia is the artifact of sion, Funding acquisition; Mark Pecha: Methodology, Validation, Re- collision from the final assembly of Gondwana. The assembly of the sources; Yu-Ling Lin: Writing - Review & Editing, Visualization; Rezal southern supercontinent may have continued until Middle Ordovi- Rahmat: Formal Analysis, Writing - Review & Editing; Azmiah Jamil: cian, beyond the previously suggested 540 Ma. East Malaya zircon Investigation. Hf array shifting to external orogenic system ca.370 Ma reflects its dispersal process from Gondwana. The signal of crustal reworking became increasingly dominant after ca.280 Ma and the transitional Declaration of Competing Interest geodynamic process from Gondwana to Pangaea in Peninsular Malaysia end at ca.230 Ma, when West Malaya collided with East The authors declare that they have no known competing financial Malaya. interests or personal relationships that could have appeared to influ- ence the work reported in this paper. Credit Acknowledgment Long Xiang Quek: Conceptualization, Formal analysis, Investigation, Writing - Original Draft, Visualization; Yu-Ming Lai: Writing - Review We would like to express our special thanks of gratitude to Prof. & Editing, Supervision, Project administration, Funding acquisition; Sun-Lin Chung who gave us the golden opportunity to do this project Azman A. Ghani: Investigation, Writing - Review & Editing, Supervision; on Peninsular Malaysia magmatic zircon. We also thank Jui-Ting Tang, Muhammad Hatta Roselee: Investigation, Formal Analysis, Writing - Chien-Hui Hung and Yi-Ju Hsin for their help with the analyses and

14 L. Quek, Y.-M. Lai, A.A. Ghani et al. Gondwana Research 94 (2021) xxx–xxx technical assistance. Furthermore, we thank the editor and anonymous Ghani, A.A., 2005. Geochemical characteristics of S- and I-Type Granites: example from Peninsular Malaysia granites. BGSM 51, 123–134. https://doi.org/10.7186/ reviewers for their careful reading of our manuscript and their many in- bgsm51200515. sightful comments and suggestions. This research was financially sup- Ghani, A.A., 2009a. Plutonism. In: Hutchison, C.S., Denis, N.K.T. (Eds.), Geology of Peninsu- ported by the Ministry of Science and Technology, Taiwan (MOST lar Malaysia. University of Malaya and the Geological Society of Malaysia, Kuala – 108-2116-M-003-005 and MOST 108-2811-M-003-511). Lumpur, pp. 211 231. Ghani, A.A., 2009b. Volcanism. In: Hutchison, C.S., Denis, N.K.T. (Eds.), Geology of Penin- sular Malaysia. University of Malaya and the Geological Society of Malaysia, Kuala Appendix A. Supplementary data Lumpur, pp. 197–210. 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