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4 Implications for the Tectonic History of Peninsular Malaysia and the Southeast Asian Region

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4 Implications for the Tectonic History of Peninsular Malaysia and the Southeast Asian Region 4 IMPLICATIONS FOR THE TECTONIC HISTORY OF PENINSULAR MALAYSIA AND THE SOUTHEAST ASIAN REGION 4.1 INTRODUCTION The Southeast Asian region, of which Peninsular Malaysia is part, is a complex collage of terranes comprising fragments of continental affinity, island arcs, accretionary complexes containing disrupted ocean basins with abundant radiolarian-bearing chert, and siliceous and tuffaceous argillite, marginal basin:; and oceanic crust. Peninsular Malaysia consists of two continental fragments separated by ;in accreionary complex. The western continental fragment is distinguished by a belt of Gondwana-derived Carbo- Permian glacial-marine diamictites and a lack of Carbo-Permian volcanics. Early Permian faunas have a cold water Gondwar an affinity (Archbold et al., 1982; Shi and Waterhouse, 1991). The eastern fragment, Ind china/East Malaya is distinguished by abundant Carbo- Permian volcanics and Carbo-Pei mian Gigantopteris floras of low latitude, Cathaysian affinity (Asama, 1984). Zircon it heritance ages of the unexposed basement Proterozoic crust indicated by Nd, Sr and zircon U-Pb isotopic data from granitoids in the west of the Peninsula are 1500 - 1700 Ma (Lie Al and McCulloch, 1985) and in the east of the Peninsula they are 1100 - 1400 Ma (Liew an I McCulloch, 1985). The granitoids located west of the Bentong-Raub suture zone (sensu :tricto) are S-type in composition, while those in the east are generally I-type. Chapter 4: Implications for the Tectonic History of Peninsular Malaysia and the Southeast Asian Region There has been considerable debatc about the amalgamation/accretion history of the terranes that constitute Peninsular Malaysia and many tectonic models have been proposed to explain the geology of this region (see Chapter 1.5.1). Authors who interpret the western Thailand/Malaysia tin-bearing gra -lite to be collision-related propose an eastward-dipping subduction model (Mitchell, 1977; 1981; Gatinsky and Hutchison, 1986; Hutchison, 1989). A west-dipping subduction model is preferred by authors who view the tin-bearing granite belt as evidence of an east-facing nagmatic arc (Bignell and Snelling, 1977; Bunopas and Vella, 1978; Macdonald and Barr, 1978; Sengor, 1979; Ridd, 1980) whilst Khoo and Tan (1983) propose an aborted rift mod This study sampled many localities along the Bentong-Raub suture zone (sensu stricto), the Semanggol Formation and some of her localities within Peninsular Malaysia with the aim of determining the age duration and history of the ocean that once separated the Gondwanan affinity terrane and the Cathaysi in affinity terrane of Peninsular Malaysia. Evidence presented in this thesis has provided constraints for the timing of suturing of the western Siburnasu and eastern Indochina/East Malaya terranes of Peninsular Malaysia. Palaeontological evidence helps co -"strain the age duration of the Palaeo-Tethys ocean in the Southeast Asian region and the tect 3nic models that have been proposed for the formation of Peninsular Malaysia. 4.1.1 Significance of Radiolarian Studies Radiolarian-bearing chert and ar, ;illite comprise a significant part of accreted oceanic terranes. They occur as clasts and fault bounded units within accretionary complexes and the mélange of suture zones. The y are the remnants of a former ocean obliterated during plate convergence. These rocks cc ntain the siliceous skeletons of varied radiolarian faunas that provide information about thy; age, depositional environment and tectonic history of allochthonous terranes and add to our understanding of the history of the Southeast Asian region, including the history of the Palaeo-Tethys ocean. Until recently, the ages of the chef t clasts and fault-bounded units of sedimentary rocks of oceanic affinity found within the Lentong-Raub suture zone were poorly known. Tectonic models used to interpret the evolution of Peninsular Malaysia within the Southeast Asian tectonic framework have been pi oposed without age control. In order to establish an objective tectonic model to aid the understanding of the geology of Peninsular Malaysia it was necessary to obtain radiolariar biostratigraphic age data for the fault bounded blocks of 235 Chapter 4: Implications for the Tectonic History of Peninsular Malaysia and the Southeast Asian Region bedded chert and argillite found w thin the Bentong-Raub suture zone -. the remnant of the Palaeo.-Tethys ocean that divided th east and west parts of Peninsular Malaysia. 4.2 PENINSULAR MALAYSIA 4.2.1 Radiolarian biostratigraphy of Peninsular Malaysia 4.2.1.1 Bentong-Raub ,Suture Zone (sensu strict()) Faunas indicative of Upper Devonian (Famennian), Lower Carboniferous (Tournaisian and Visean), and Lower Permian (Wolfcampian and Leonardian) ages have been recovered. These ages are represented by eight radiolarian zones from twelve localities along the suture zone. The well preserved radiolarians represent eight radiolarian zones. These are; Holoeciscus 2 - 3 Assemblage Zones, Albaillella deflandrei Zone, Albaillella cartalla Zone, Pseudoalbaillella u-forma rr . II Zone, Pseudoalbaillella lomentaria Zone, Pseudoalbaillella scalprata m. rhomboihoracata Zone, Albaillella sinuata Zone and Pseudoalbaillella longtanensis 2 one. The range of rock types of diverse depositional environments including deep open-ocean, arc-influenced deposition and continental margin proximity, now juxtaposed, sugge q that the Bentong-Raub suture zone is an accretionary complex. 4.2.1.2 The Semanggol Formation The "Lower Chert Member" of the Semang,gol Formation of northwest Peninsular Malaysia has yielded latest Lower Permian )r early Upper Permian, Upper Perrnian (Guadalupian) and Middle Triassic (Anisian anc Ladinian) radiolarian assemblages. Five radiolarian biostratigraphic zones are represented. These are the ?Pseudoalbaillella longtanensis Zone, Follicucullus porrectus Zone, N. ornithoformis Zone, Triassocampe coronata Zone and the Triassocampe deweveri Zone. 236 Chapter 4: Implications for the Tectonic History of Peninsular Malaysia and the Southeast Asian Region 4.2.1.3 Other Localities within Peninsular Malaysia Two exposures of marine sedimen ary rocks from outside the Bentong-Raub suture zone (as delineated by previous authors), in licate that the accretionary complex may be wider than is presently known. An isolated blo,;k of isoclinally folded tuffaceous chert exposed along a road cutting near Kuala Kangsar is found within the Kati Formation. These rocks have been recrystallised and although abunth nt radiolarians, were visible in hand specimen, they were generally unable to be extracted. However, one sample yielded very poorly preserved specimens tentatively assigned to he Lower Carboniferous radiolarian species ?Albaillella sp. cf. A. deflandrei GOURMELON Upper Permian (Guadalupian) radi D1 ari ans have been reported from an isolated exposure of interbedded chert and highly weathered mudstone near Genting Serampang, Jengka, Pahang (Basir Jasin and Uyop Said, 1994). This locality is within the central part of Peninsular Malaysia known as the Central Belt which consists of Carboniferous - Late Triassic rocks. The Permian and Early Triassic is represented by shallow marine argillite, tuff, limestone, dolomite, conglomerate and volcanic flows of andesitic to rhyodacitic composition. The Middle Triassic of the Central Belt is represented by slope-deposited interbeds of mudstone, coarse and fine tuffs/tuffaceous ndstone, conglomerate and minor limestone (Metcalfe, 1989). The stratigraphic relationsh p of the block of bedded chert and interbedded mudstone to the adjacent rocks is unknown, but its presence in the Central Belt is an enigma. One possible explanation is that the Cen :ral Belt is underlain by rocks of an accretionary complex and the anomalous occurrence of a block of interbedded chert and mudstone is a rare exposure of the underlying rocks. 4.2.2 Significance of these results in relation to previous tectonic model; 4.2.2.1 Review of previous tectonic models in the light of present results As previously discussed (Chapter 1.5.1), rnany authors have proposed tectonic models to explain the geology of Peninsular P Ealaysia. Within these models several aspects have been the subject of much debate. These i 237 Chapter 4: Implications for the Tectonic History of Peninsular Malaysia and the Southeast Asian Region • the time of separation of the various blocks that comprise Peninsular Malaysia from the parent craton (northeast margin of Gondwana); • the time of amalgamation of the tectonic blocks that comprise Peninsular Malaysia, and the time of closure of the Pali Leo-Tethys ocean; • the direction of subduction beneath the tectonic blocks that comprise Peninsular Malaysia; • the tectonic relationship between the Bentong-Raub suture zone and the Semanggol Formation of northwest Peninsular Malaysia; the lateral (East-West) exten : of the remnant of the Malaysian segment of the Palaeo- Tethys ocean. These aspects are discussed below. The time of separation of the various blocks that comprise Peninsular Malaysia from the parent craton (northeast margin of Gondwana). Various times have been put forward for the separation of Indochina/East Malaya and Sibumasu from Gondwana (Table 1-.1). Indochina/East Malaya is said to have separated in the Silurian or Early Devonian (Metcalfe, 1994a). Limited palaeomagnetic data (Wu et al., 1989; Lin and Fuller, 1990) also upports this timing. Carboniferous and Permian floras have equatorial, Cathaysian affir ity (Asama, 1984; Metcalfe, 1986) so Indochina/East Malaya must
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