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Origin and Tectonic Significance of the Metamorphic Rocks Associated with the Darvel Bay Ophiolite, Sabah, Malaysia

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Origin and Tectonic Significance of the Metamorphic Rocks Associated with the Darvel Bay Ophiolite, Sabah, Malaysia Downloaded from http://sp.lyellcollection.org/ at Royal Holloway, University of London on March 25, 2014 Origin and tectonic significance of the metamorphic rocks associated with the Darvel Bay Ophiolite, Sabah, Malaysia SHARIFF A. K. OMANG 1 & A. J. BARBER 2 1 Department of Earth Sciences, Faculty of Science and Natural Resources, Universiti Kebangsaan Malaysia, Sabah Campus, Locked Bag No 62, 88996 Kota Kinabalu, Sabah, Malaysia 2 SE Asia Research Group, Department of Geology, Royal Holloway, University of London, Egham TW20 OEX, UK Abstract: Banded hornblende gneiss, foliated amphibolite, hornblende, chlorite and siliceous schist form lenses in an 8 km wide belt within the Darvel Bay Ophiolite Complex. Foliation in the belt is generally steep to vertical, striking parallel to the trend of the belt and lineations are sub-horizontal. Mineral and geochemical studies show that the metamorphic rocks represent banded and isotropic gabbros, plagiogranites, doleritic and basaltic dykes, basaltic volcanics and cherts formed at a spreading ridge in a supra-subduction zone environment, which were deformed at high temperatures but low pressures along a transform fault. Incorporation of supracrustal cherts indicates that the transform extended for hundreds of kilometres between spreading centres. Garnet pyroxenites and amphibolites found as clasts in Miocene volcanic agglomerates formed at high pressures, and temperatures are interpreted as derived from a metamorphic sole underlying the complex, formed during subduction of ocean crust and the emplacement of the ophiolite complex on Sabah. Ophiolite outcrops are distributed throughout the (Rangin et al. 1990). Cherts from the Chert-Spilite eastern part of Sabah, East Malaysia, from Banggi Formation have yielded radiolaria of Lower Island in the north to Ranau and Telupid and the Cretaceous age (Leong 1977; Rangin et al. 1990; Lahad Datu area in the south (Fig.l, inset). The Aitchison 1994). Massive limestones associated Darvel Bay Ophiolite Complex in the south is the with the Chert-Spilite Formation contain most extensive outcrop, extending 100 km west- Cretaceous foraminifera (Leong 1974). The Chert- wards from Darvel Bay. The greater part of the Spilite Formation is interpreted as representing complex consists of peridotite, largely serpen- ocean floor sediments which were deposited on top tinized, but it also includes cumulate pyroxenites, of the ophiolite (Hutchison 1975), and carbonate layered and massive gabbros and diorites, meta- cappings to seamounts. Since the underlying morphosed to varying degrees. The complex is also oceanic crust is unlikely to be much older than the cut by dolerite dykes, although these are never so oldest overlying sediments, the Early Jurassic K-Ar abundant to be termed a sheeted dyke complex. ages are regarded as spurious (Hutchison 1988). These rock types are closely associated with out- Fragments of ophiolitic rocks are found as clasts crops of the Chert-Spilite Formation, composed of in Eocene sediments (Newton-Smith 1967; Rangin pillow basalt, banded ribbon chert, turbiditic sand- et al. 1990), suggesting that the ophiolite complex stones, mainly volcaniclastic but with some rare had been obducted onto Sabah either in the latest quartz sandstones, and a few occurrences of Cretaceous or earliest Palaeogene. In the early massive limestone. Miocene the ophiolite complex formed the base- The ophiolite complex has been well described ment to a volcanic arc, possibly related to continued in the publications of the Geological Survey of subduction of the Proto-South China Sea. Mitchell Malaysia (Reinhard & Wenk 1955; Fitch 1955; et al. (1986) and Rangin (1989) have suggested Dhonau & Hutchison 1966; Koopmans 1967). The that, as a result of continued compression, the complex has been interpreted as a segment of ocean complex was backthrust over the Celebes Sea floor floor, either of a Proto-South China Sea (Holloway to the south. 1981; Rangin et al. 1990) or of the Celebes Sea The ophiolite complex is surrounded by chaotic (Hutchison 1988). A wide range of K-Ar age dates melange deposits (Fig. 1) which contain fragments has been obtained from the rocks of the ophiolite of all the rock units represented in the complex complex from 210Ma (Leong 1971) to 137 Ma and the Chert-Spilite Formation, as well as From Hall, R. & Blundell, D. (eds), 1996, TectonicEvolution of Southeast Asia, 263 Geological Society Special Publication No. 106, pp. 263-279. Downloaded from http://sp.lyellcollection.org/ at Royal Holloway, University of London on March 25, 2014 264 s.A.K. OMANG (~ A. J. BARBER 0 5 10 r' Km Ophiolite Complex E~ Felsite ~ RecentAIluvium ~ ~'~] Metamorphic rocks E~ Chert-Spilite • " '* '° "~ "* "* "* "* "° "° "° ". "° "... - , ~ '. ". "° '. ". ". "° ". Formation ~'.'~**,' i**: (foliated metabasites ) ~~::*:i*" []'EI Sheared Serpentinite D Neogene , ,, ,, ,,, ,, ,, -° "4 "° . "° "° .o .° .° ...... sediments , ', ', ', ', ', ', "°,:*.:*.:*.:°.:*,:*,:°,:*,:*, ~ Gabbros & Cumulates [~ M6langes "°"°' ' °"°' l Peridotite ~ Thrust fault (mainly serpentinised) - - " Fault ~!~:i:ii!i:i:i:!...i.i~.:i:i:i!!iiii!i!iiiiiiiiiiiiiiii!i!iiiii!i!ii!iii!::ii!i!~ii:!:!:!:!:i: l: 8" 20' E. ::::::::::::::::::::::::::::::::::::::::::::::::::::: ===============================================================~~:i.i:i:i:i!ii!i!i!iii!iiiiii!iiiiiiii!!!iii!!!iliiiiiiiiiii Gabbro *Dolerite dyke PSI2 D~:: PS6 Irtl Pulau Sakar , ~ ~PT3 Pulau "~;K4 ! I ! rl~l ! ! ! ! | ruiau~, ' %,• ~l9 Katung- / ~1 i i : • ~. Saddle/ % Kalungan-.L l.ll.l~.l~.ll. 1.1~.13.11.1~.1~I~. ~ ~ -.L Cumulate D i i i i i i i pi--.~.,1-.-~ ,,.z.~ p C rocks Darvel Bay E t 7 4* 58'N Pulau SARAWAK 1 "~ ~, Bohayan Pulau Tabauwan _/'f / ~, P ~ f V~Silumpat / ~':*'i*' 118" 10' E. E --/- 118"20' E Dolerite dyke I Fig. 1. Geological map of the Darvel Bay Ophiolite Complex near Lahad Datu showing location of samples used in this study. Inset map shows distribution of ophiolite complexes in Sabah. B, Banggi Island; R, Ranau; T, Telupid; DB, Darvel Bay. younger sediments and volcanic rocks. Clennell Metamorphic rocks (1991) considered that the melanges were formed by processes of sedimentary slumping and Although the rocks forming the Darvel Bay diapirism, coincident with the collision of micro- Ophiolite Complex are variably metamorphosed continental blocks with the north Sabah margin and throughout, dynamically metamorphosed rocks the extension of the arc basement related to the are concentrated in an E-W belt c. 8 km wide development of the Sulu Sea in late early and early extending westwards from Lahad Datu on the north mid Miocene times. The ophiolite complex and side of Darvel Bay (Fig.l) which can be traced for the melanges are overlain unconformably by Late c. 40 km to the west. Metamorphic rocks are well Miocene to Pliocene sediments of the 'circular exposed in coastal sections around the shores of basins' and in the Quaternary again formed the Darvel Bay and particularly around the small basement to a volcanic arc which extends from islands within the bay, where they have been Mindanao in the Philippines, through the Sulu described previously by Dhonau & Hutchison archipelago to the Dent and Semporna peninsulas (1966) and Hutchison & Dhonau (1969, 1971) from of Sabah. the north side of the bay, and by Koopmans (1967) Downloaded from http://sp.lyellcollection.org/ at Royal Holloway, University of London on March 25, 2014 DARVEL BAY OPHIOLITE, SABAH 265 from the south. Inland exposures are poor, apart schistosity increases in localized shear zones. The from road-cuts, quarries and scarce river sections. banding is commonly folded into tight intrafolial The metamorphic rocks have been described as isoclinal folds which may show the closed eyed metagabbros, amphibolites, hornblende gneisses outcrop pattern characteristic of sheath folds. and schists. Reinhard & Wenk (1955) described Where folds are present the schistosity is parallel to the dynamically metamorphosed rocks as the axial planes of the folds. In the more intensely 'Crystalline Schists' and Koopmans (1967) identi- deformed shear zones aligned hornblende and fied them as the 'Crystalline Basement Complex', feldspar crystals define a mineral lineation, lying with the implication that they were the oldest rock in the plane of the schistosity. unit in Sabah. However, K-Ar dating reported by Dhonau & Hutchison (1966) showed that these Amphibolite metamorphic rocks are of Cretaceous age, the same age as the Darvel Bay Ophiolite Complex, and form Amphibolites are commonly found associated with an intrinsic part of the complex the banded gneisses in the field. These may form The structure of the dynamically metamorphosed extensive outcrops, as on the northern side of Sakar belt has been fully described by Dhonau & Island or as smaller bodies which may show cross- Hutchison (1966). The metamorphic rocks are cutting, intrusive relationships to the hornblende typically banded, schistose and lineated. Through gneisses. The grain size of these amphibolitic rocks most of the belt the banding and schistosity are is variable. Coarse grained amphibolites show the vertical or steeply dipping and strike E-W, parallel characteristic distribution of white feldspathic and to the general trend of the belt, swinging round to a black or green ferromagnesian minerals which more NW-SE trend in the islands of Darvel Bay. indicate that they have been derived from gabbros The lineation is sub-horizontal, lying in the plane (metagabbro). Medium and finer grained of the schistosity
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