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Sedimentation and Tectonics of Paleogene Sediments in Central Sarawak

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Sedimentation and Tectonics of Paleogene Sediments in Central Sarawak AnnllaLGeoLogicaL Conference '96 .............-;;:::a:a_ JUlle 8-9, 1996, Kota KillaOaiu, Sahah Sedimentation and tectonics of Paleogene sediments in central Sarawak FELIX TONGKUL Earth Science Department Universiti Kebangsaan Malaysia Abstract: The deposition of the Paleogene sediments in Central Sarawak occurred in four successive stages, its axis of depocentre generally advancing and younging to the northeast in response to progressive southwest subduction-accretion of a Mesozoic oceanic lithosphere and its sedimentary cover under West Sarawak. The younger sediments were deposited on top or in front of an older accreted sediments. The timing of deposition and accretion is uncertain due to lack of precise age indicators. However, based on regional considerations, the accretion is interpreted to have occurred sometimes during the Early Paleocene, Middle Eocene, Upper Eocene and Upper Oligocene, respectively, along major fault zones, producing four tectono-stratigraphic units. The older sediments were subjected to polyphase deformation as younger units were accreted. INTRODUCTION TECTONIC AND GEOLOGICAL SETIING I was first introduced to the rocks of Sarawak Central Sarawak, occupying the northwestern during the 1991 GSM post-conference field trip, part of Borneo lies at the intersection ofthree major from Batang Lupar to Miri town. At that time the plates, the Eurasian, Indo-Australian and exposures were excellent and I was really Philippines located to the north, south and east, determined to do some work in this region. respectively (Fig. 2). The movement of the three Unfortunately, due to other commitments, I was major plates relative to one another in a complex unable to do much fieldwork, until 1993. For the and poorly understood pattern has resulted in the past two years, I have visited and studied the good accretion of terranes and creation of marginal basins exposures, mainly along the north-south Sri Aman­ since early Tertiary times. Central Sarawak Bintulu Highway, totalling about 20 fieldwork days. represents part of an accreted terrane, lying Fieldwork along the Balui River, a major tributary adjacent to an extended continental margin to the ofthe Rajang River, totaling 10 days was also carried north. The continental margin, presently occupied out to have some kind of lateral comparisons with by the Luconia and Dangerous Grounds Platform those rocks exposed along the highway. As part of is believed to have rifted from the southeastern the regional study, 4 undergraduate students (Jaul, margin of the Eurasian Plate or locally called the 1996; Lim, 1996; Freddy, 1995; Lau, 1995) were Sundaland Craton (Taylor and Hayes, 1983; assigned to map in detail critical areas along the N­ Hutchison, 1989). S highway to understand the stratigraphical The accreted terrane in Central Sarawak and relationships of the rock units, their depositional Sabah, commonly referred to as the NW Borneo environments and tectonic history (Fig. 1). The fold-thrust belt or NW Borneo subduction complex field survey was also supplemented by regional (Hamilton, 1979) extends over a distance of more structural study of Central Sarawak using high than 1,000 km along strike and reaches a width of resolution synthetic aperture radar (SAR) over 300 km. Its northwestward margin ends imageries, kindly made available by PETRONAS. somewhere along the NW Borneo Trough, whereas This paper presents an overview of the main its southern margin lies near the international findings ofthe study. Although there still remains border of West Sarawak and West Kalimantan. a lot of work to be done, an attempt has been made The southern margin being marked by the presence to show the sedimentation and tectonics of the of ophiolitic melange (Tan, 1979; Williams et al., Paleogene sediments, based on plate tectonic 1986). concepts of subduction-accretion. In Central Sarawak the accreted sediments have Geo l. Soc. MaLaYJia, Bulletin 40, JuLy 1997; pp . 155-155 o 50 100 150km Areas mapped in detail , ! Lau (1995) Jaul (1996) South China Lim (1996) Sea D Freddy (1995) N-S Highway "Tl Fig. 3 m r- X o-i z G) A C r- Figure 1. Map of Sarawak showing the study area. SEDIMENTATION AND TECTONICS OF PALEOG ENE SEDIM ENTS IN CENTRAL SARAWAK 137 Pre- Tertiary Continental Crust Extended D Continental Margin Terrane accreted or formed since Late D Cretaceous D Oceanic Crust / Subduction Zone Z~ Transcurrent ~ Fault 11 Direction of Plate / /" Movement Extensional Basin Ophiolite ~ PHILIPPI NES PLATE o 500km Figure 2. Geological and tectonic setting of Sarawak. Central Sarawak represents part of an accreted terrane, commonly referred to as the NW Borneo fold-thrust belt. JuLy I!)!) 7 138 FELIX TONGKUL been mapped as the Rajang Group flysch sediments regional approach using age, lithology and degree in the Sibu Zone (Haile, 1969, 1974), dated to range of structural deformation as a criteria for in age from late Cretaceous to Oligocene. The differentiation might be helpful. Rajang Group sediments is in faulted contact with Based on the above criteria, the Paleogene older rocks (mostly Mesozoic) ofWest Sarawak. along sediments of Central Sarawak. have been grouped the Lupar Line (Haile, 1974) and are Qverlain by'. into four informal ~ectono-str~tigraphic units (Figs. Neogene shallow marine deposits to the northwest 3 and, 4,). The oldest unit includes the Layar Member in the Miri and Baram area (Haile, 1962;,Hamilton, of the Belaga Formation which range in age from 1979; James, 1984). The Rajang Group sediments Upper Cretaceous to Middle Paleocene. The second includes the Lupar, Belaga, Kelalanand Mulu unit includes the Kapit and Metah Members of the Formations. Belaga Formation, Lupar and Engkilili Formations (renamed as the LuJ:>okA.ntu Melange by Tan, 1979) TECTONO-STFiATIGRAP~IC UNITS which range in age from Late' Paleocene to Early Eo'c.ene. The third UIlit includes the Pelagus Existing geological map ofSarawak(Yin, 1992), Member of the Belaga. Fprmation which range in shows that the central part of Sarawak. is occupied age from Middle to Upper Eocene. The fourth unit by several rock units, the oldest being· the Lupar includes the Tatau, Buan and Silantek Formations Formation, followed by the Belaga ]formations and which range in age from Uppermost Eocene to Upper subsequently the Melinau Limesio:tu~; Tatau; Buan . Oligocene. The four units generally corresp6I1Q.s and Nyalau Formations: The stratigraphical .' with Stages I-IV mentioned earlier. Except for relationships between the formatiollS have not been minor $anges in geological boundaries, the fully resolved yet, due to lack precise age indicators. distribution of each unit generally follows the The Belaga Formation vihi"ch' occupies an distribution ofeach roCk units'as mapped by Leichti enormous .area (about 90%)' of Ceritral Silrawak-' etal., (1960) and Wolfenden (19'60). was subdivided into foUr :.nembers, nainely the' Layar, Kapit, Pelagus ;and :M:etab Members based on differences in. theh- lithglogy 'by Leichti et al., UNIT I (1960). The four members broadly corresponds to" (LATE CRETACEOUS-MIDDLE Stag~8 I, Ii, III and IV proposed earlier by Kirk ' . ~ALEOCENE) (1957) and later adopted by Wolfenden (1960':' Stages I, II, III and, IV, broadly represen~s the time . period of Upper' Cretaceous" Lower E"Ocene~ Distribution' 'and LithOlogy' Paleocene, Middle·;Epcene t.o .L!>wer Eoc.ene·!IDd This.unit, represented by the Layar Member of Upper Eocene, resp~ctively. ~other member, the~ '. the Belaga Formation occUr in the Batang Layar~ Bawang'Meinber, whl.ch co~e~pono.s to Stage,lV: ,Buldt Sebangkoi bel~, with an approximate width was added later by 'Wolfenden (.19.{}0) .. The , of abQut 80 ,km.~, Most of the unj.t has undergone striitigraphical relationship between, eaehmembers met.amorphism to slate and sub-phyllite and' shows or. stages is also not fully resolved. La..cking concrete the de'\t.Qlopment of slaty cleavage. field ··evidences, up to now they . are" gen~r.ally The best outcrop for the unit occurs near Bukit assumed to be conformable with each other. Sebangkoi, where the lithologic8.l sequence can.still Wolfenden (i960) however, pointed out that the be measured. In'this area; the unit comprised of sudden influxes of coarse-grained sediments in the interbedded slate and thin metasandstone with lower' part of Stages II and III, may suggests occasional' occurr(m,ce of thick sandstone beds, instability and the:refo:r~ uncoriformable" .reaehlng more 'than 10 metres (Fig. 8). Lim (1996) . relationshIp. Kirk (1957) suggested that.Stage III measured about 250 metres of section (Fig; 5). The in the Upper Rajang area might be unconformable sequence is typical of a deep water sediments, on Stage II., . .shoWing; typical turbidite facies with numerous DUring the present study, attemptwa.sriiade to fining, and coarsening upward sequences, diff~rentiate .. the rock formations in 'Central representing prograding and migrating outer fan Saraw.ak."; . Whereas the Nyalau Formation was lobes. The overall predominance of muddy sequence easily recogn~ "in thefi~ld, because of its in the unit suggests an open basin plain depositional distinctive lithology and simple structure, the older setting. formations proved to be difficult to differentiate. It Towards the south near Batang Layar, the became even more difficult, if one were to separate sequence commonly includes slump beds, channeled each formation based on varied description of their sand beds, pebbly to conglomeratic beds and vertical lithologies and structures in different areas by burrows suggesting deposition on slope settings previous researchers. It became apparent, that a (Freddy, 1995). The source of the sediments is GeoL. Soc. MaLaYJia, BuLletin 40 A .....r r, ./Al __ -::. _ :. '""/,:,/./ ~A.. ~~ .,..-q"'::xi ---\-1"'\".,..,.... ,...-.".. __--- _ N . .... ,:., 'A'"1x~ ~ ;'Y.YA' / I ...,,/ ~~v::..-:::--;:::::-- -=_ ..... "/ Tatau..:-"',4' " oJ-4.4' -v- / I )" 11~ _ _ _ ~ 1# A<...<" / .At' I ./ ::. <2- -6 ~~~-v--.r--r /~/1' ~_ ....... Y A /Z-X .-A:::-<...r A' ~ ~~ //' /;/ __ ~ .. "-,-.r--<r..A-:, ::1:.Y-r-<-r~~""-Y"'~A// __........ y A_./' /0-~ /" -..
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