2 GEOLOGY OF PENINSULAR MALAYSIA - Research UNE€¦ · 2 GEOLOGY OF PENINSULAR MALAYSIA 2.1...

2 GEOLOGY OF

PENINSULAR MALAYSIA

2.1 INTRODUCTION

Peninsular Malaysia has traditionLlly been subdivided into NNW-SSE longitudinal belts

on the basis of stratigraphy, mineralisation, geological structure, geological history and

tectonic evolution . Scrivenor (19:;8) subdivided the Peninsula into three elongate belts on

the basis of mineralisation: a western tin belt, a central gold belt and an eastern tin belt.

Hutchison (1977) divided the Peni isula into four major tectonic subdivisions on the basis

of different tectonic histories; the '1Vestern Stable Shelf, the Main Range Belt, the Central

graben, and the Eastern Belt. Fo ) (1983) divided the Peninsula into four zones on the

basis of differences in stratign phy. Khoo and Tan (1983) proposed a threefold

subdivision; a Western Belt, Central Belt and an Eastern Belt on the basis of differences in

stratigraphy and geological histoi y within Peninsular Malaysia. Within this threefold

subdivision, Khoo and Tan (1983' further divided the Western Belt into two regions: a

northwest sector and a Kinta-Ma acca sector. Tjia and Harun (1985) recognised four

structural domains within the Peninsula. They defined Northwest, West, Central and

Eastern structural domains.

Within all the above subdivision schemes, the boundary between the eastern and central

"belts" is taken as the Lebir Fault 2 one, and the boundary between the central and western

"belts" is the Bentong-Raub line of Hutchison (1975).

As previously stated (Chapter 1.5.2), Metcalfe (1988) proposed that Peninsular Malaysia

consisted of two continental terra les, a western Gondwanan affinity continental terrane

(Sibumasu) and an eastern Cathaysian affinity continental terrane (Indochina/East Malaya)

Chapter 2: Geology of Peninsular Malaysia

(Fig. 2.1). Sibumasu and Indochina/East Malaya are separated by the Bentong-Raub

suture zone, a highly-deformed ac::retionary prism containing the remnants of the Palaeo-

Tethys ocean which once divided them (Stauffer, 1974; Sengor, 1984; Hutchison, 1987;

Metcalfe, 1988; Sengor et al., 1988) (Fig. 2.1). The Sibumasu terrane is characterised by a

Palaeozoic passive margin sequence which includes a belt of Late Carboniferous - Early

Permian glacial marine diamictite ; (Stauffer and Mantajit, 1981; Stauffer and Lee, 1986;

Metcalfe, 1988). Early Permian faunas have a high-latitude, cold--water Gondwanan

affinity. Carboniferous and Permian volcanic rocks are rare. In contrast, the

Indochina/East Malaya continental terrane is distinguished by abundant Carboniferous -

Permian volcanism and equatorial tower and Upper Permian Gigantopteris floras (Asama,

1984). No post Devonian Gondwanan faunas or floras are found on this terrane.

The Malaysian part of the Sibun asu Terrane of Metcalfe (1988) corresponds with the

Western Belt of Khoo and Tan (P)83). Tie Malaysian part of the Indochina/East Malaya

Terrane of Metcalfe (1988) corresponds with the Central and Eastern Belts of Khoo and

Tan (1983) (Fig. 2.1).

The stratigraphy of Peninsular Malaysia is summarised below within the tectonic

subdivision of Metcalfe (1988), but incorporating the threefold stratigra.phic subdivision of

Khoo and Tan (1983). The rocks of the Bentong-Raub suture zone will be described

separately. Chronostratigraphic columns for the Western, Central and Eastern Belts, as

well as the Bentong-Raub suture z(me are provided in Fig. 2.2.

2.2 GENERAL GEOLOGY OF PENINSULAR MALAYSIA

2.2.1 Sibumasu Terra ne

A belt of Lower Palaeozoic rocks extends from The Shan States of Burma (Myanmar),

through South China, Thailand and Peninsular Malaysia. The southern extension of the

belt is controversial. This belt has been referred to by several names, and the most

commonly used are listed in the tal ,le below:

36

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qBentong-Raub suturezone (sensu stricto)

Semanggol Formation


Figure 2.1 Map of Peninsular Malaysia illustrating the Sibumasu and Indochina/East Malaya terranes,the Bentong-Raub suture zone that divides them, and the Semanggol Formation ofnorthwest Peninsular Malaysia.(Western, Central and Eastern Belt terminology after Khoo and Tan, 1983).

37

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Yunnan-Malaya Geosyncline Burton, 1967

West Malaya Block Stauffer, 1974

R.idd, 1980Thai-Malay Peninsular Block

Shan-Thai craton Bunopas and Vella, 1978

Metcalfe, 1986Sibumasu Block

Sinoburmalaya Gatinsky and Hutchison, 1986

Metcalfe, 1988Sibumasu terrane

Burton (1967a) referred to the b( it of Lower Palaeozoic rocks in the Malay Peninsula

which continues northward into China as the Yunnan-Malaya Geosyncline. Stauffer

(1974) renamed the Yunnan-Ma aya Geosyncline as the West Malaya Block and he

tentatively included the whole of Sumatra within the block. Ridd (1980) identified a

crustal block in west Malaya and Peninsular and west Thailand, and named it the Thai-

Malay Peninsular Block. The nor =hern and southern extensions into Burma and Sumatra

were not well defined.

Gatinsky and Hutchison (1986) defined a narrow, elongate continental block of

predominantly Palaeozoic shelf sequence rocks that extends southwards from SW China,

through the Shan States of Burma, western Thailand, into the western Malay Peninsula and

the northern part of Sumatra. The) named this block Sinoburmalaya.

Metcalfe (1986) defined the Sibu -nasu Block as comprising the Shan States of Burma,

north-west Thailand, Peninsular Burma and Thailand, Western Malaya, and north-west

Sumatra, and possibly extending northwards into western China and Tibet. It was said to

be composed of continental shelf sequences of Cambrian to Permian age and a 2000 km

elongate belt of Carboniferous-Pet mian glacial marine diamictites (Stauffer and Mantaj it,

1981; Stauffer and Lee, 1986; Metcalfe, 1988). Early Permian faunas have an affinity with

Gondwanaland (Archbold et al., 1982; Shi and Waterhouse, 1991). There is also a general

absence of Carboniferous - Permiat volcanism on Sibumasu.

2.2.1.1 Stratigraphy

Proterozoic Basement

Proven Precambrian basement is not exposed in Peninsular Malaysia (Hutchison, 1989).

The age of the underlying, but une,:posed Proterozoic crust indicated by Nd, Sr, and zircon

39


U-Pb isotopic data from granitoics of the Sibumasu terrane is 1500-1700 Ma (Liew and

McCulloch, 1985). The age of the underlying basement of the Indochina/East Malaya

terrane is 1100-1400 Ma (Liew and McCulloch, 1985). In north-west Peninsular Malaysia,

fault-bounded blocks of amphibo ite facies granitic gneiss, mica schist and calc-silicate

known as the Kupang Gneiss, havo been uplifted along the Bok Bak Fault. Burton (1972)

proposed that these rocks represer t the Precambrian, but Hutchison (1989) suggested that

metamorphic grade may not be co •relative with age and therefore the Kupang Gneiss may

not be of Precambrian age.

WESTERN BELT (Khoo and Tan 1983)

Northwest sector of the Western Belt (Figs. 2.1 and 2.2)

The northwestern sector of the We ;tern Belt of Khoo and Tan (1983) includes the areas of

the states of Kedah, Langkawi-Perlis and north Perak. Geographic subdivision and

location names within Peninsular Malaysia referred to in this thesis are found in Fig. 1.1.

Machinchang Formation (Jones, 1C 81)

The Cambrian-Ordovician Mac hinchaig Formation consists of 3000 metres of

predominantly clastic deposits (Le 1983). It is the oldest known sedimentary deposit in

Peninsular Malaysia (Jones, 1968). The base of the formation has not been observed. It is

a coarsening upward sequence of rhythmically interlayered graded siltstones and

mudstones interbedded with thic cer bedded clayey sandstones. Cross-bedding, load

structures, ripple marks, slumped bedding and bioturbation have been interpreted to be

indicative of an offshore shelf de-)osit (Lee, 1983). Trilobite and brachiopod fossils of

latest Cambrian to earliest OrdoN ician age and various types of shallow-marine trace

fossils have been found in siltstone, mudstone and fine sandstone (Lee, 1983). The overall

environment of deposition of the Machinchang Formation has been established to be a

wave-dominated delta which built over an offshore shelf deposit to produce a series of

barrier-beach sands aligned paralle to the shore line (Lee, 1983).

Jerai Formation (Bradford, 1961)

In mainland Kedah, the Jerai Formation is believed to be the oldest strata and on the basis

of structural and lithological grounds, has been correlated with the Machinchang

Formation (Jones, 1968). The regionally metamorphosed, unfossiliferous Jerai Formation

consists of two units; a lower schist series and an upper arenaceous series (Khoo and Tan,

1983). It is overlain by unfossilifc rous limestone in the Sungei Patani area known as the

Sungei Patani Formation or the IV ahang Formation, which has been correlated with the

Ordovician shelf limestone of Perli ; and Langkawi (Jones, 1968).

40


Setul Formation (Jones, 1961)

The fossiliferous Setul Formation is exposed on the eastern side of the island of Langkawi

and on the mainland in Kedah and Perlis. It forms large areas of mountainous country and

the spectacular karst topography )f the Langkawi Islands. It conformably overlies the

Machinchang Formation and cow ists of the Lower and Upper Ordovician Lower Setul

Limestone; the Lower Silurian Lower Detrital Member; and the Upper Setul limestone

overlain by the Upper Detrital M( mber which contains earliest Devonian fossils (Jones,

1973).

The Lower Setul Limestone is a st •ongly indurated, thickly bedded platform deposit. The

lower part of the unit reflects perit dal conditions, but the upper-most part reflects gradual

deepening of the shelf facies. Ord )vician, Silurian and Lower Devonian conodont faunas

were described from this unit by Ig D and Koike (1967; 1968; 1973) and Wongwanich et al.

(1983) reported chert lenses and r odules in several horizons within the upper part. The

Lower Detrital Member consists of black carbonaceous shale and siltstone which is

overlain by the Upper Setul Lime stone. The Upper Detrital Member consists of black

graptolite bearing shale (Hutchiwn, 1989). Wongwanich et al. (1983) identified a

stratigraphic break of unknown thickness representing Late Ordovician time, between the

Lower Setul Limestone and the ba ;e of the Lower Detrital Member. The Setul Formation

passes conformably into the younl;er Kubang Pasu Formation. The Setul Formation was

deposited in an environment of det pening marine sedimentation, with occasional influx of

coarse clastic sedimentation but wi :h continued carbonate deposition.

Mahang Formation (Burton, 1967b)

The Mahang Formation is exposed in central and south Kedah. It consists of strongly

folded carbonaceous shale, mudstc ne, siltstone and radiolarian chert, with minor grey and

lighter coloured quartzarenite and subgreywacke and rare calcsilicate hornfels and

limestone (Jones, 1968). Fossils indicate an age range of Silurian to Early Devonian

(Jones, 1968). Jones (1968) propcsed that these sediments were deposited in a restricted

basinal environment, shielded from open-ocean conditions by an island arc.

Kubang-Pasu Formation (Burton, 1964)

The Kubang-Pasu Formation of r orthwest Peninsular Malaysia exposed in central and

south Perlis and north Kedah is ccnsidered to be the stratigraphic equivalent of the Singa

Formation exposed at Langkawi (` rancey, 1975; Foo, 1983). Its age range is Devonian to

Permian. The Kubang Pasu Form ition consists of alternating beds of shale and siltstone

and poorly sorted sandstone and i ; conformable over the Setul and M:ahang Formations.

The Kubang Pasu Formation passe; conformably into the overlying Chuping Limestone.

41


Singa Formation (Jones, 1973)

The Singa Formation of Carboniferous-Permian age, conformably overlies Upper

Devonian red mudstones, and ccnsists of crudely laminated, dark grey, poorly sorted

mudstones with scattered megacl asts, few fossils and much soft-sediment deformation

(Stauffer and Lee, 1986). The sub ingular to angular megaclasts consist of sandstone, dark

chert, argillite, limestone, rare gr mitic plutonic rocks and metamorphic rocks, and one

documented trondhjemite boulder that has yielded a Precambrian (1029 ± 15 Ma) K-Ar

age (Stauffer and Snelling, 1977 suggesting a Precambrian continental source for the

Palaeozoic sediments in the region. The relationship of the megaclasts to the very fine

grained matrix and the soft sediment deformation of the matrix, indicate that the clasts are

dropstones of glacial origin. The pebbly mudstones of the Singa Formation have been

interpreted as being glacial marire in origin (Stauffer and Mantajit, 1981; Stauffer and

Lee, 1986). The Singa Formatior is part of a belt of pebbly mudstones that extends for

2000 km from Sumatra, north to c antral Burma (Stauffer and Lee, 1986). Gobbett (1973)

considers that the Kubang Pasu 7ormation differs from the Singa Formation in being

largely composed of thick-beddcd quartz and felspathic sandstone with interbedded

mudstone.

Hutchison (1989) states that Trias sic age sedimentary rocks are generally absent west of

the Bentong-Raub line, with the exception of a belt of epicontinental limestone - the

Kodiang and Chuping Limestone of Permian to Triassic age, the fault-bounded Triassic

Semanggol Formation and the red ed-ignimbrite sequence of Genting Sempah.

Semanggol Formation (Alexander, 1959)

The fault-bounded Semanggol Formation is exposed in three main areas of northwest

Peninsular Malaysia. It is exposed in northwest Perak, south Kedah and in central to north

Kedah and continues into Thailand (Bur:on, 1973). In part, the eastern margin of the

formation has been intruded by tilt; Main Range granite, but the stratigraphic relationship

of the Semanggol Formation to th; surrounding geology is obscure (Burton, 1973). The

Semanggol Formation has been di 3 ided into three members by Burton (1973): the Lower

Chert Member, Middle Rhythmitf Member and the Upper Conglomerate Member. The

Lower Chert Member has been &scribed as occupying the western (lower?) part of the

outcrop. The type section, locate I at Bukit Merah, just north of Gunong Semanggol is

composed of interbedded arenite acid argillite with occasional conglomerate bands (Burton,

1973). It does not include the Lower Cher Member.

The Lower Chert Member occurs as erosion-resistant, elongate ridges, several kilometres

long. The chert is generally pale n colour, and may be white, cream, yellow, tan, grey,

green, pink, red or purple. Isoclinal folding is common. The stratigraphic contact of the

42


Lower Chert Member and the Middle Rhythmite Member has not been observed, although

a structural contact has been described (Ahmad et al., 1988). Ahmad et al., (1988)

described a section from an active quarry at Bukit Barak (locality K2 of this study). The

presence of a major thrust fault is identified, juxtaposing rocks from the Lower Chert

Member against rocks from the Middle Rhythmite Member.

The Middle Rhythmite Member (turbidite sequence) is composed of alternating

successions of greywacke, subgreywacke and lutite with occasional lenticles of

conglomerate. Burton (1973), noted that the chert clasts within the conglomerate lenticles

of the Middle Rhythmite Member are generally dark in colour, unlike the pale chert of the

Lower Chert Member, but similar to the nearby Silurian to Devonian Mahang Formation.

The conglomerate exposed at Gunong Semanggol also contains generally dark-coloured

chert clasts. Sedimentary structures include graded bedding, crossbedding, sole marks and

rare ripple marks (Burton, 1973). Burton (1973) describes a general gradation between the

Middle Rhythmite and the Upper Conglomerate members (Burton, 1973).

Figure 2.3 Isoclinally folded, bedded chert from the "Lower Chert Member" of the SemanggolFormation at locality K9 near Kuala Nerang. [SUNGEI TIANG 8 - GR295594]

43


The Upper Conglomerate Member is composed of lutite and arenite with polymict

conglomerate interbeds, container g clasts of quartz, quartzite and minor proportions of

chert, mudstone, sandstone and n re volcanic clasts. Khoo (1968) notes that the Upper

Conglomerate Member is steeply f Dlded into a synclinorium with a plunge to the north and

the beds are generally steeply dipping and are open to tightly folded. The time of

deformation proposed by Khoo s post Late Triassic time. Khoo also notes that the

presence of graded bedding, sharp lower contacts, directional sole marks and slump

structures which suggest that the L pper Conglomerate Member was deposited by turbidity

currents. Burton (1973) also notcs that the Semanggol Formation rocks to the north of

Sungei Muda are overlain unconformably by a sequence of red conglomerate and

mudstone of typical continental aspect (Saiong beds), which he correlated with the

Tembeling Formation of Jurassic age.

The Semanggol Formation was, until recently, considered to be entirely of Triassic age,

including the Lower Chert Memb Kobayashi et al. (1984) have reported late Middle

Triassic (Ladinian) bivalves from the Lower Chert member, and Late Triassic (Lower and

Middle Carnian and Carno-Nori m) bivalves from the Middle Rhythmite and Upper

Conglomerate Members. Howeve (Sashida et al., 1992; Sashida et al., 1993b) recovered

Upper Permian radiolarians repres( nting the Follicucullus monacanthus and Neoalbaillella

ornithoformis Zones of Ishiga (1c90) from the Lower Chert Member of the Semanggol

Formation, and Metcalfe (1990b)i;.-,ported Late Triassic (Carnian) conodonts from bedded

pelagic limestone at the same local ity.

The Semariggol Formation, equivalent :o the Nathawi Formation of south Thailand

(Burton, 1974), lies to the east of the age-equivalent carbonate platform which is

represented by the Chuping and Kodiang Limestone.

Saiong beds (Ong, 1969; Burton, 973)

The red conglomerate and muds' one of the Saiong Beds contain Early Jurassic plant

fossils. The rocks are typical cot tinental redbeds and unconformably overly the Upper

Conglomerate Member of the Sem rnggol Formation in the Muda Dam area (Ong, 1969).

Kodiang Limestone (De Coo and S mit, 1975)

The Kodiang limestone faunal ssemblage consists of algal stromatolites, bivalves,

foraminifers, crinoids, bryozoans, Dstracods and conodonts. Limestone breccia formed by

the dissolution of evaporites ar:, common (Rao, 1988). Other rock-types include

conglomerate, mudstone and radic larian chert (De Coo and Smit, 1975). It is interpreted

to have been deposited in a warm to tropical peritidal environment (Rao, 1988). Its age

44


ranges from Late Permian to Latc Triassic (Koike, 1973; Koike, 1982; Metcalfe, 1981b;

Metcalfe, 1990b; Metcalfe, 1990c; Metcal Fe, 1992).

Chuping Limestone (Jones, 1968)

The Chuping Limestone conforma ply overlies the Singa and Kubang Pasu Formations and

was previously thought to be entiiely of Permian age, but Fontaine et al. (1988) reported

Ladinian-Carnian algae and foraininifera, and Metcalfe (1990b) reported Late Triassic

(early Norian) conodonts. The unit is composed of skeletal grains and intraclasts

interpreted to have formed in shallow, high-energy environment. The original mineralogy

of the skeletal grains and early diagenetic cements were chiefly calcite and minor aragonite

and the faunal assemblage is sin ilar to that of sub-polar carbonates. Oxygen isotope

studies of the lower part of the Chuping Limestone suggest that the temperature of

deposition 'was 2-13° C reflecting cool temperate (to ?subpolar) conditions (Rao, 1988).

This formation is now known to sr an late Early Permian to Late Triassic time and to be in

part age-equivalent to the Kodiang Limestone.

Kinta Malacca sector of the Western Belt (Khoo and Tan, 1983) (Figs. 2.1 and 2.2)

The Kiinta Malacca sector of the 17% esters Belt of Khoo and Tan (1983) includes the Kinta

Valley, and Palaeozoic rocks south to Malacca.

Dinding Schist (Gobbett, 1964)

The Diinding Schist is a 340m thic k unit of quartz-mica schist which grades upwards into

the Hawthornden Schist (Foo, 1983). The age of the Dinding Schist is uncertain

(Hutchison, 1989), but the lower p Lrt has been correlated with the Machinchang Formation

(Gobbett, 1964).

Hawthornden Schist (Gobbett, 196 1)

The Hawthornden Schist is of uncertain age and consists of mainly unfossiliferous

carbonaceous schist and phyllite Ind outcrops in the Kuala Lumpur area, east of Batu

Caves. Gan (1979) reported Ordovician gastropods and cephalopods in limestone

interbedded with the Hawthornden Schist near Tanjong Malim. It lies adjacent to the

Upper Silurian Kuala Lumpur Lin estone Jut the geological relationship between the two

units is unknown. The Hawthornden Sch:st has been interpreted by Hutchison (1989) as

being a highly compressed deeper water basin (back-arc) which lay between platform

carbonate to the west and the volc inic arc facies of the Dinding Schist to the east. It has

been correlated with the Pilah Schist (Hutchison, 1989). The undated Pilah Schist is

located on the eastern side of the IV ain Range belt of plutons. An early Palaeozoic age has

been suggested by association with adjacent shale beds containing Early Devonian

graptolites south of Karak (Jones, 1973).

45


Kuala Lumpur Limestone (Gobbet?, 1964)

The Kuala ]Lumpur Limestone has been described as marble and contains Upper Silurian

(Ludlow) brachiopods and corals (Thomas, 1963; Boucot et al., 1966). The Kuala Lumpur

Limestone overlies the Hawthorn len Schist (Hutchison, 1989) and has been correlated

with the upper part of the Setul Limestone and the lower part of the Kinta Valley limestone

(Foo, 1983).

Kenny Hill formation (informal) (S tauffer, 1973)

The Kenny Hill formation is a sequence of elastic sedimentary rocks in the Kuala Lumpur

area, although the unit has never been properly defined. No datable fossils have been

found in the Kenny Hill formation However, Lower to Middle Permian ammonoids have

been identified from rocks located south of Kuala Lumpur in rocks tentatively assigned to

the Kenny Hill formation (Abdullah, 1985). Previously the age of the formation had been

determined by relationship with tie Upper Silurian Kuala Lumpur Limestone which it

appears to overly unconformably (Hutchison, 1989). The formation consists of a sequence

of interbedded shale, mudstone and sandstone. The sandstone is composed of quartz

grains, recrystallised chert grains and rare weathered feldspars. There is an abundance of

carbonaceous fragments and an ab indance of well-rounded zircon fragments in the heavy

mineral fraction. The depositional environment has been interpreted to be in marine

waters not far from an eroding Ian Imass, such as the outer portions of a delta or shelf, or

the upper portion of a submarine sl )pe (Hutchison, 1989).

Kinta Valley limestone (informal) Gobbett, 1973)

The Kinta Valley region is underlain by quartzite and a thick sequence of limestone. The

Kinta Valley limestone forms the f oor of the valley and also predominant hills in the area.

The age of the limestone extends f -om Silurian to Permian (Suntharalingam, 1968) with a

major stratigraphic break extendin ; from latest Devonian to late Tournaisian (Lane et al.,

1979; Metcalfe, 1981a). Granite passes border the valley and are concordant with the

sedimentary rocks, but the nature of the contact is uncertain. The straight scarps along

some parts of the valley indicate that the west side of the valley is bounded by a major

fault. Minor discontinuous faults are also evident on the eastern side of the valley. The

Kinta Valley limestone is interpret( d to have formed on a stable shelf (Gobbett, 1973).

Kati Formation (Foo, 1983)

The Kati Formation, to the west of the Kinta Valley consists of interbedded phyllite,

metaquartzite, sandstone, shale and siltsto ie. The age of the formation is unknown but it

has been correlated with the Kuba ng Pasu Formation of Devonian to Permian age (Foo,

1983).

46


2.2.1.2 Granitic Intrusions

Granite constitutes about one th rd of the land surface of Peninsular Malaysia. The

granites of the Malay Peninsula NN ere originally subdivided into three belts by Hutchison

(1977); the Main Range Belt, the Central Belt and the Eastern Belt. Cobbing et al. (1986)

established that the granites of ti e Central Belt and the Eastern Bel '.t were similar and

defined two granite provinces witi in Peninsular Malaysia, each having its own distinctive

pattern of mineralisation - the Main Range Province and the Eastern Province (Fig. 2.4).

The Main Range Province of Peninsular Malaysia is composed of a concentration of major

batholiths and plutons. The Main Range Province consists of large batholiths that range in

size from 80 x 25 km 2 to 10 x 15 km 2 (Hutchison, 1989). They have a restricted

compositional range comprising i suite of tin-bearing S-type biotite: granite of mainly

Triassic age (Bignell and Snelling, 1977; I,iew and Page, 1985). The Main Range granites

are commonly coarsely porphyri- is and contain perthitic to microcline alkali feldspar

(Hutchison, 1977). The S-type Main Range Granite (granitoid belt) (Fig. 2.5) is located

along the western margin of the B ,ntong-Raub suture zone, although in places it intrudes

the suture zone itself, forming a sti:ching pluton (Hutchison, 1977). In the southern part of

the Peninsula, the Main Range Belt has been downfaulted and displaced by a series of left

lateral, Early Tertiary northwest - southeast trending faults, the most prominent of these

being the Bukit Tinggi Fault (I lutchison, 1989). The Main Range plutons intrude

isoclinally folded phyllite and marble and contact metamorphic aureoles are generally

absent suggesting emplacement in a deep seated environment which allowed very slow

cooling and permitted the alkali feldspars to invert to microcline (Hutchison, 1977). The

emplacement of the granites into isoclinally folded phyllite and marble, and the general

absence of pronounced contact aureoles indicates that the granites are mesozonal and were

emplaced at a depth of at least 4 kr 1 (Buddington, 1959).

Hutchison (1977) suggests that these features imply that the Main Range Belt has been

uplifted by several kilometres since the Triassic. The margin of the Main Range granite,

just west of the Bentong-Raub sw ure near Bentong is characterised by strongly gneissic

granite and augen structures. The shear planes dip steeply and lie parallel to the Bentong-

Raub suture. The intrusive age of the plu-:ons of the Main Range Granite indicated by U-

Pb zircon data is 198-220 Ma (latest Triassic - Early Jurassic) (Liew and Page, 1985).

Mitchell (1977), Beckinsdale (197 )) and Hutchison (1978; 1983) interpret the S-type Main

Range batholiths to have a contine It collision origin. Nd, Sr and zircon U-Pb isotopic data

47

98° 102°D, 106° no°

Main Range Province

Eastern Province

12°

Western granites (S + I types)[Cretaceous]

Central granites (S type) 8 °

[latest Triassic - Early Jurassic]

Eastern granites (I type)[Permo-Triassic and isolatedpost-orogenic plutons ofCretaceous age]

4 °

0

400 km1


Figure 2.4 Distribution of S- and I-type granitoids of Peninsular Malaysia and Thailand (after Cobbinget al., 1986).

48

'cr(r),---\L -N rt.-%

SIBUMASU -4TERRANE %

INDOCHINA/EAST MALAYA

TERRANERaub

Bentong

Karak

---,,, -\,.

\_

-----,

I102E

0 50 100 150 km1 1 1 1

N

5N -

o

\

IIIIBentong-Raub suture zone(sensu stricto)

Main Range Granite


Figure 2.5 Map of Peninsular Malaysia illustrating the Main Range belt of granite plutons.(Western, Central and Eastern Belt terminology after Khoo and Tan, 1983).

49


from granitoids of the Main Rang(' Province have indicated that the age of the unexposed,

underlying basement is within the -ange of 1500-1700Ma.

The granites found on Langkawi contain intermediate microcline and the rocks of the

Carboniferous Singa Formation have a pronounced contact metamorphic aureole. Outside

the contact aureole, the rocks are u metamorphosed (Hutchison, 1977).

2.2.1.3 Structural geology

Peninsular Malaysia is elongated in a north-northwest direction parallel to its structural

trend (Tjia and Harun, 1985). Thc northwest of the Peninsula is characterised by surface

structures that trend in a northeast direction in addition to those striking north-northwest.

Mid-Permian folding has been idc ntified in the northwest sector of Peninsular Malaysia

(Khoo and Tan, 1983). Post mid-Permian carbonates and clastics deposited in the

Northwest sector were uplifted anc folded by the culmination of the Late Triassic orogenic

event which affected the whole of ihe Peninsula (Khoo and Tan, 1983).

Tectonic transport directions in IN ninsular Malaysia are generally westwards, except for

the Central Belt where east vergem e is observed (Tjia and Harun, 1985). The general west

vergence and the east vergence e Kperienced by the rocks of the Central belt, has been

interpreted to be the result of general east-west compression related to Late Triassic plate

convergence (Tjia and Harun, 198` ).

The NW-SE structural grain of Peninsular Malaysia includes prominent faults, commonly

filled by major multiphase quartz dykes, such as the Kiang Gates which may have

experienced subsequent wrench mction (Gobbett and Tjia, 1973).

2.2.2 Indochina/East :14alaya Terrane

The Indochina/East Malaya terran is characterised by abundant Carboniferous - Permian

volcanism, and by equatorial, Low er and Upper Permian Cathaysian Gigantopteris floras

(Asama, 1984). Cathaysian Gigartopteris floras have been recovered from two localities

in east Peninsular Malaysia, Jenglci Pass in Pahang, and Linggiu in Johore (Asama, 1984).

50


Hutchison (1989) interprets the Central zone of Foo (1983) to be a shallow platform

adjacent to an island arc system developed on continental crust. He proposes that it

contained abundant limestone and submarine volcanic arcs which grew above sea level. It

is proposed that it was part of a cc nvergent margin throughout most of the Visean to Late

Triassic. Final collision orogeny and uplift took place in latest Triassic (Hutchison, 1989).

The central and southern part of tl-e Central Belt was depressed into a collisional foredeep

to be filled by the thick tuffacecus Sem antan Formation, while the northern part was

uplifted and eroded.

Metcalfe (1989) refers to the Centi al zone as an extensional graben bounded to the west by

major faults along the Bentong-Raub line and to the east by the Lebir Fault Zone.

Metcalfe reports that major normi .1 faulting, which may have begun during the Permian,

occurred along the Bentong-Raub ire and Lebir Fault Zone, produced a graben in which 2

to 3 km of marine Triassic (Seman :an Formation) and subsequently 1.5 - 2 km of Jurassic -

Early Cretaceous continental sedin tents accumulated represented by the Gagau Group.

The rocks of the Eastern zone of Foo (1983) are predominantly Carboniferous and

Permian elastics and volcanics. P: ,roclastic rocks of rhyolitic to andesitic composition are

widespread (Hutchison, 1989). Pr oterozo is continental basement does not outcrop, but its

presence is indicated by zircon radiometric dating from intruding granite plutons. The age

of the underlying continental crust is 1100-1300 Ma (Liew and McCulloch, 1985).

2.2.2.1 Stratigraphy

THE CENTRAL BELT (Khoo anti Tan, 1983) (Figs. 2.1 and 2.2)

The Central Belt of Khoo and Tan (1983) occupies the region between the Bentong-Raub

Line of Hutchison (1975) and the I ,ebir Fault zone.

Raub Group (Alexander, 1959)

The Carboniferous-Permian Raub Group has been correlated with the Kepis Formation in

the south and the Gua Musang Formation in the north. The Raub Group is composed of

limestone, calcareous shale and a -.id pyroclastic rocks (Hutchison, 1989). Some of the

rocks identified as belonging to the Raub Group may be part of the Bentong-Raub suture

zone rocks and therefore, may not form part of the Central Belt stratigraphy. The Late

Jurassic continental conglomerate and sandstone of the Raub redbeds are observed to

unconformably overly the "Raub C roup" near Raub (Fig. 2.14).

51


Gua Musang formation (informal) (Burton, 1973)

The Gua Musang formation is composed of argillaceous rocks with interbedded limestone

and volcanic pyroclastic rocks. Fossils of Middle Permian to Lower Triassic age have

been reported (Rajah and Yin, 1980) and sedimentation appears to have been essentially

continuous from Middle Permian to lower Middle Triassic (Anisian) (Hutchison, 1989),

but basal Triassic strata have yet to be confirmed.

Kepis formation (informal) (Gobbett, 1973)

The Kepis formation is described as a sequence of carbonaceous shale, siltstone, mudstone

and sandstone with minor conglomerate and local limestone. Fossils indicate deposition

from Visean to Middle Permian (Khoo, 1973; Gobbett, 1973).

Figure 2.6

Mudstone and thin interbeds of volcaniclastic sandstone of the Semantan Formation.[Scale: 5cm = 1 metre]

Semantan Formation (Ahmad, 1976)

The Middle to Late Triassic Semantan Formation is composed of a thick (approximately

1000 - 1400 metres) sequence of acid to andesitic volcaniclastics and mudstone with minor

conglomerate and limestone (Fig. 2.6). Middle Triassic (Ladinian) bivalves and

ammonites have been recovered from the Semantan Formation at Lanchang (Metcalfe et

al., 1982). Kobayashi (1963) reported Triassic Daonella from the Semantan Formation in

52


Central Pahang. The environment of deposition is interpreted to be the flank of a Triassic

volcanic island or island chain (Metcalfe et al., 1982). The Semantan Formation

unconformably overlies the Permian Kepis Formation and is folded into a sequence of

open synclines and anticlines who ie axes are subhorizontal (Hutchison, 1989). The rocks

are highly fossiliferous in places and the presence of Halobia and Posidotzia indicates

deeper water conditions (Hutchiso 1989). Metcalfe and Chakraborty (1994) suggest that

the Semantan Formation may forn i part of a forearc or inter-arc basin constructed over an

accretionary wedge.

Tembeling Formation (Koopmans, 1968)

The Late Triassic to Jurassic Tembeling Formation is a 3000 m thick sequence of

continental redbeds. The formation is seen to unconformably overlie steeply dipping

Permian limestones at Jengka Pas It has been correlated with the Raub redbeds which

unconformably overlies bedded chert and argillite in the Raub area (Hutchison, 1989).

The Tembeling Formation has also been correlated with the Saiong red beds that

unconformably overlie the Late Triassic (Carnian-Norian) part of the Semanggol

Formation of northwest Peninsular Malaysia (Ong, 1969). The basal part of the Tembeling

Formation was deposited under marine conditions, with the rest of the formation being

nonmarine (Burton, 1973). The rocks of the Tembeling Formation are folded into broad

open synclines with localised steer dips (Hutchison, 1989).

EASTERN BELT (Khoo and Tan, 1983)(Figs. 2.1 and 2.2).

The Eastern Belt of Khoo and Tar (1983) includes all rocks to the east of the Lebir Fault

zone.

Kuantan Group (Alexander, 1959)

The oldest rocks exposed east (Y . the Bentong-Raub Line are a Lower Carboniferous

(Visean to Namurian) interbedde d sequence of sandstone, siltstone and shale of the

Kuantan Group of the Eastern Belt. The Kuantan Group includes the Visean to Namurian

Charu Formation, overlain by the Namurian Panching Limestone (Metcalfe et al., 1980),

(Fig. 2.7) which is in turn, overlair by the Sagor Formation of Late Carboniferous to Early

Permian age (Metcalfe et al., 1 S80) Ripple marks, cross-bedding and shallow-water

limestone within the Kuantan G -oup are indicative of a shallow marine, near-shore

depositional environment (Hutchi on, 1989). Coal seams have also been described from

the Kuantan Group (Jennings and Lee, 1985).

53


Figure 2.7 The Namurian Panching Limestone of east Peninsular Malaysia.

Gagau Group (Rishworth, 1974)

The Gagau Group forms a succession of gently dipping incompletely consolidated

conglomerate and sandstone (Burton, 1973). It unconformably overlies Permian strata and

in places granite, and is generally flat-lying to moderately dipping with local folding. The

Group includes the Badong Conglomerate which is overlain by the Lotong Sandstone.

The Badong Conglomerate consists of red conglomerate, sandstone, siltstone and shale.

The Lotong Sandstone consists of cross-bedded sandstone and minor coal seams. Plant

fossils indicate an Upper Jurassic age to a Lower Cretaceous age (Rishworth, 1974;

Hutchison, 1989).

2.2.2.2 Granitic Intrusions

Granitoids of the Eastern Province (Cobbing et al., 1986) (Fig. 2.4) consist of smaller

batholiths of zoned and unzoned plutons of mainly I-type composition. These plutons

have a wider compositional range than do the Main Range granite plutons (Hutchison,

1973), ranging from gabbro to monzogranite (Cobbing et al., 1986). The composition of

the zoned plutons ranges from tonalite or diorite to monzogranite (Cobbing et al., 1986).

54


The plutons of the Eastern Province are of Permo-Triassic age (Bignell and Snelling, 1977;

Hutchison, 1977; Cobbing et al., 986) but isolated post orogenic plutons in northern and

southern Peninsular Malaysia arc of Cretaceous age (Darbyshire, 1988). The Eastern

Province plutons intrude a sequent:e of mudstone, siltstone and sandstone with occasional

limestone and locally thick sequences of intermediate to acid volcanic and volcaniclastic

rocks. Granitoids in the Eastern Province are generally undeformed with the exception of

the Cretaceous Kenerong Pluton of the Si:ong Complex in northern Malaysia just east of

the Bentong-Raub suture, which contains a highly deformed migmatitic component (Singh

et al., 1984).

The granites of the Eastern Province are characterised by equigranular to weakly

porphyritic texture and contain )rthoclase to intermediate microcline alkali feldspar

(Hutchison, 1977). Some plutor s contain miarolitic cavities. The country rocks are

volcanic and pyroclastic rocks with several well developed cordierite-andalusite hornfels

metamorphic aureoles. These features indicate high-level emplacement of the plutons.

Base metal mineralisation occurs within and in the marginal zones of some plutons and

there is also significant tin mineralisation, but not on such a large scale as that found from

the granites of the Main Range Prc vince..According to Rb:Sr isochron data the granites of

the East Coast Province were intruded in two episodes; at 250 Ma (Late Permian) and 220

Ma (Carnian) (Bignell and Snelling, 1977). The age of unexposed Proterozoic crust

beneath or adjacent to the Eastern Province indicated by Nd, Sr and zircon U-Pb isotopic

data from the granitoids , is 1100 - 1400 Ma (Liew and McCulloch, 1985).

The Cretaceous granites of the S :ong Complex have a compositional affinity with the

Eastern Province granites, and ft ose of Johore comprise a distinctive sub-province of

highly differentiated I-type granit ;s. Cobbing et al. (1986) proposes that these features

may suggest a degree of Cretaceoui reactivation of the Bentong-Raub suture.

2.2.2.3 Structural geology

Three main phases of deformation are recorded in Upper Palaeozoic and Lower Mesozoic

rocks of East Malaya. Upper Palaeozoic strata is generally quite severely folded along

axes which predominantly strike \INW to north. The Late Triassic-.Jurassic Indosinian

Orogeny resulted in deformation of the strata, including the continental Permian strata

(Hutchison, 1989). The earliest phase of deformation of Indochina/East Malaya is

suggested to have taken place when this region was an active convergent margin, dated

late Early Permian (255-270 Ma) by granite age (Hutchison, 1989). The Eastern zone

55


experienced a phase of regiona metamorphism, folding and uplift which probably

occurred in the Late Palaeozoic (Permian?). The Central zone experienced Late Triassic

uplift which terminated marine sedimentation (Khoo and Tan, 1983). In the central zone

of the Peninsula, Middle and Latc Triassic rocks were transported eastwards contrary to

general westwards tectonic trans Jort in other parts of the Peninsula (Tjia and Harun,

1985). Low-angle faults and fold; in the Semantan Formation suggest transport towards

the southeast (Tjia and Harun, [985). During the Late Cretaceous, the continental

Tembeling Formation were uplifted and gently folded (Khoo and Tan, 1983). By the end

of the Mesozoic or early Tertiary time Peninsular Malaysia became tectonically stable

(Tjia and Harun, 1985) and small outcrops of continental Tertiary sediments mark minor

basins, whereas the main part of the country remained above sea-level throughout the

Cenozoic (Tjia and Harun, 1985).

The Lebir fault

This prominent fault forms the t oundary between the central and eastern belts of the

Peninsular. In the north it appears to be a fault zone several kilometres wide running SSE

in and along the Lebir valley. Fui the y south the fault has a more southerly trend (Tjia and

Harun., 1985). Metcalfe and Chakraborty (1988) reported diamictite from the eastern

margin of the Central Basin. T Ie clasts consist of sandstone, tuffaceous sandstone,

carbonaceous tuff and mudstone set in muddy matrix which is sheared and foliated

(Metcalfe and Chakraborty, 1988: . Hutchison (1989) has suggested that the Bukit Ulu-

Kemapan-Gunung Besar-Bekok gi anitoid probably intrudes the Lebir fault zone. Bignell

and Snelling (1977) state the age c f the granitoid obtained from whole-rock Rb:Sr isotope

geochemistry, is 222 ± 5 Ma or Lae Triassic.

2.2.3 Bentong-Raub uture Zone (sensu stricto)

The Bentong-Raub suture zone of Peninsular Malaysia is a narrow north-south trending

zone of deformed rocks extending; from the Malay-Thailand border, just west of Tomo,

through Bentong and Raub and east of Malacca (Fig. 2.1). It has been known by a number

of names.

Bentong-Raub Line Hutchison, 1975

Bentong-Raub" medial Malaya" lit e Mitchell, 1981

Bentong-Raub suture zone Tjia, 1987a

56


The northern extension of the su ure zone is taken as the Uttaradit-Nan suture zone in

southern Thailand (Barr and Macdonald, 1987; Barr and Macdonald, 1991) and the

Changning-Menglian suture in South China (Jin, 1994; Wu et al., 1995; Metcalfe, 1996;

Metcalfe et al., in press).

The southern extension of the suture zone is controversial (Fig. 2.8). Three positions for

the southern extension of the Ben tong-Raub suture zone in the vicinity of Sumatra have

been proposed. Hutchison (1975; 1983; 1993) suggests that the suture lies parallel to the

western margin of the deformed Carnian-Norian strata of the Central Belt of Peninsular

Malaysia. It continues through the Riau and Lingga archipelagoes somewhere in the

vicinity of Bangka and Billiton I: lands. Tjia (1985; 1989) and Metcalfe (1990a; 1996)

propose that the Palaeo-Tethyan suture occupies the position of the Palaeogene Bengkalis

graben of Sumatra. Hamilton (1C 79) illustrated the suture swinging west from Malacca

(Fig. 2.8). This interpretation ha ; been rejected on stratigraphic and structural grounds

(Hutchison, 1993).

The rocks within the mélange cc nsists of olistostromal blocks of oceanic sedimentary

rocks (mainly chert, siliceous and tuffaceous argillite, minor limestone, rare conglomerate

clasts, and rare blocks of turbidit ; sandstone) set in a sheared and foliated argillaceous

matrix (Figs. 2.9 - 2.13, 2.15). Th range of rock types now juxtaposed, indicate a variety

of depositional environments. Radiolarian chert occurs as both clasts and as olistostromal

blocks of bedded chert. The clasts are generally augen-shaped and are elongated parallel to

the direction of foliation. Some )f the lenses are truncated and disrupted, while others

show the pinch and swell structure of boudinage. Foliation of the sheared matrix wraps

around the margins of the clasts a id produces a wavy, anastomosing appearance. Small-

scale tension gashes are also v sible. Competent fault-bounded blocks of bedded

mudstone, and rare bedded chert blocks that have escaped deformation are also found

within the chaotic mélange. The arger blocks of bedded siliceous marine sediments and

minor limestone with inferred fault boundaries range from metres to kilometres in size.

The rocks generally strike in a N-S direction. The blocks of radiolarian-bearing chert and

argillite are folded along norther y-trending fold axes and the foliation of the sheared

matrix is parallel to strike. Tjia a Id Almashoor (1993) noted that the rocks in the suture

zone east of Cameron Highlands ( 2.1), occur as stacked rock units or imbricate thrust

slices and they interpreted the E entong-Raub suture zone to be a highly compressed

accretionary prism. Mustaffa (1994) described the fault pattern in the same area. He notes

that there are a great number of high-angle faults that exhibit NNW strike-slip motion,

parallel or sub-parallel to the suture ; zone trend.

57

2N -- 2N

- 4N . RAUB 4N -

• BENTONG

EAST MALAYA

Position of Palaeo-._Tethys suture

1i1

SUMATRA1

- 25 1 I BANGKA100 200 I ISLAND0

I I km .

1 \


Tjia (1987b) suggested that the mélange developed near a collisional plate boundary in the

Late Palaeozoic. A 7 km wide belt of quartz-mica schist containing large lenses of

amphibolite schist is found within the western margin of the suture zone adjacent to the

Main Range belt of plutons. The amphibole schist is believed to have a mafic igneous

origin, possibly submarine lava flows (pillow lavas?) (Jones, 1973; Tjia, 1987a). Several

discontinuous, narrow, elongate bodies of serpentinised mafic-ultramafic rocks are aligned

north-south within the schist belt of the suture zone and have been interpreted as ophiolite

(Stauffer, 1974; Hutchison, 1975; 1989; Tjia, 1987a; 1989). The sporadic occurrence of

dismembered, incomplete ophiolite bodies and the absence of glaucophane metamorphism

may be attributed to post-accretion deformation, eg. strike-slip faulting. The S-type Main

Range Granite (granitoid belt) (Fig. 2.5) is located along the western margin of the

Bentong-Raub suture zone.

The Bentong-Raub suture zone (sensu stricto) is a highly compressed accretionary prism,

containing a belt of mélange and discontinuous, elongate bodies of serpentinite. This belt

of rocks may have been subject to post-accretion (Cretaceous?) strike-slip faulting. It is

proposed that the Bentong-Raub suture zone (sensu lato) is wider than presently defined.

The Raub redbeds

The ? Upper Triassic - Jurassic, continental, conglomerate/sandstone unit of the Raub

redbeds (Fig. 2.14) unconformably overlies the chert/argillite of the Bentong-Raub suture

zone in the Raub area. The Raub redbeds have also been observed to overly the schist of

the suture zone in the Cheroh area (Lim, 1972).

1HOE 104E 106E

Figure 2.8 Southern extension of the Palaeo-Tethyan suture zone of Peninsular Malaysia as proposedby various authors.

58


Figure 2.9 Conglomerate clasts within mélange at locality KLK5 near Bentong, Bentong-Raubsuture zone. [BENTONG 87 - GR755274]

59


Figure 2.10 Conglomerate clast within mélange at locality KLK5 near Bentong, Bentong-Raubsuture zone. [BENTONG 87 - GR755274]

60


Figure 2.11 Example of augen-shaped chert clasts within sheared and foliated matrix. Matrixdisplays an anastomosing foliation. Locality KLK13 near Genting Sempah, BentongRaub suture zone. [KUALA KUBU BAHARU 86 - GR588035]

61


Figure 2.12 Sheared diamictite containing clasts of chert and mudstone, and an internallyundeformed block of bedded mudstone at locality KLK13 near Genting Sempah,Bentong-Raub suture zone. [KUALA KUBU BAHARU 86 - GR588035]

Figure 2.13 Sheared and foliated matrix containing clasts of chert and mudstone at locality KLK13near Genting Sempah, Bentong-Raub suture zone. [KUALA KUBU BAHARU 86 -GR588035]

62


Figure 2.14 The conglomerate and sandstone of the Raub redbeds which unconformably overlie the"Raub Group" near Raub. [RAUB 77 - GR669555]

63


Figure 2.15 Bt. Cinta Manis is interpreted to be a large limestone clast within the tectonic mélangeof the Bentong-Raub suture zone. [BENTONG 87 - GR880166]

2.3 DISTRIBUTION OF RADIOLARIAN-RICH SILICEOUSSEDIMENTARY ROCKS

Radiolarian-bearing, chert and siliceous and tuffaceous argillite are found in two main

areas of Peninsular Malaysia, the Bentong-Raub suture zone and the Lower Chert Member

of the Semanggol Formation. Within the Bentong-Raub suture zone they occur as chert

clasts and fault-bounded blocks. The radiolarian-bearing rocks of the Lower Chert

Member occur as NNW-trending, erosion-resistant elongate ridges that are several

kilometres in length, and isoclinal folding and faulting is common. Two outcrops of

radiolarian-bearing, tuffaceous argillite were sampled in the west of Peninsular Malaysia

near Kuala Kangsar (Fig. 2.1). An isolated outcrop of chert and interbedded mudstone has

been reported by Basir Jasin and Uyop Said (1994) from Genting Serampang, Jengka,

Pahang in the Central Belt (Fig. 2.1).

64


2.4 DESCRIPTION OF SAMPLE LOCALITIES

2.4.1 Radiolarian san- ple localities from the Bentong-Raub suturezone (sensu strino)

Following are field descriptions of localities that have yielded radiolarian faunas. Barren

localities are listed with map-grid references and sample numbers in Appendix B. For

locality maps see Appendix C. Fic Id sketches illustrate the position of productive samples

only.

LOCALITY KLK1

Location: Road-cutting 1 km soutl- of Genting Sempah tunnel on the new Kuala Lumpur -

Karak Highway. (Locality map Fig. C.1)

Number of samples collected: 94.

Description,: The Kuala Lumpur-Karak Highway has exposed long outcrops of intensely

deformed tuffaceous sandstone and mudstone and minor chert lenses within a matrix of

sheared, schistose mudstone matrix. Competent fault-bounded blocks of bedded

mudstone, and rare bedded chert blocks that have escaped deformation are also found

within the chaotic mélange. The re cks at tnis locality and locality KLK13 form part of the

Genting Thrust Belt where the Gor -ibak Chert has been interpreted to have been thrust onto

the Selut schists from a general not theast toward southwest direction (Lim and Tjia, 1979).

Shear zones, mylonite and disrupted, elongated augen-shaped chert beds and clasts all

indicate intense deformation. Much of the exposure has been affected by hydrothermal

alteration and rocks contain finely disseminated sulphides. The exposure was generally

very weathered and altered and a field sketch was not attempted. Samples were taken from

the least weathered folded chert an I mudstone beds. The locality is ten "benches" high and

only the lowest bench was sample d. (Benches are cut during road-building.) Two float

samples were taken from the side c f the lo west bench and radiolarians were visible in hand

specimen.

LOCALITY KLK3A / KLK3B

Location: Road-cutting 3.3 km ft orn Kaiak on Karak-Kuala Pilah Road. (Locality map

Fig. C.2)

Number of samples collected: 38 irom KLK3A and 9 from KLK3B.

Description: Vertically dipping si iceous argillite beds becoming more tuffaceous towards

the western end of section.

65

10 m

Covered255/62E

Do

0 ,00 00

/oCo!glomerate

Covered


LOCALITY KLK4

Location: Road-cutting, 17.5 km from Karak on Karak - Kuala Pilah Road. (Locality map

Fig. C.2)


Description: This road-cutting e;:posure of bedded black chert is well camouflaged by

vines, grass and soil and the orient Ilion of the beds was unable to be determined.

LOCALITY KLK18

Location: Road-cutting 300m N o ' junction to Bt Cinta Manis on K. Lumpur - Karak Rd.

(Locality map Fig. C.2)


Description: Low road-cutting e> posing bedded chert, siliceous and tuffaceous argillite

with interbedded tuffaceous argi lite. Rocks are very weathered and outcrop is quite

indistinct at times, due also to the grass cover. A field sketch was not attempted due to

poor exposure.

LOCALITY NS2 (Fig. 2.16)

Location: 27 kms SSW of Bahau. (Locality map Fig. C.6)


Description: Steeply dipping and isoclinally folded, black chert beds are separated from

conglomerate to the west of expo ;ure, by a fault. Clasts in conglomerate are fairly well

rounded and consist of quartzite, sLndstone, siltstone and chert pebbles. Thickness of chert

beds is 2 - 5 cm. Only productive ;amples and those adjacent are illustrated.

E W

Figure 2.16 Field sketch of locality I IS2 near Kuala Pilah. [KUALA PILAH 104 - GR289185].

66


N S

Cc vered 1m

,

0 BR641 ' , , ,' / , ,' ,,

,, , - , _ _ _ , ._ , , , • ,/ ,, ,,' ,, ,, ,,' ,

L1 S30 - n' ,/ ,/,, , - - ,-uBR,28, , , , ,, , , ,',, , , _ , - , , ,

.14.1j,/ ,/ , ,• - - - 0 BR62 ,', -

tiBR626 ,' :i'0 BI3625

,{j BR624,

, , ' ' •

Figure 2.19 Field sketch of grey anti tan bedied chert clast at western end of exposure at localityKLK2. [BENTONG 87 - GR8801661. Only productive samples and those adjacent areillustrated.

LOCALITY KLK5

Location: Road-cutting, Taman D lam housing estate at Bentong. (Locality map Fig. C.3)


Description: This road-cut is an exposure of mélange. The mélange consists of weathered,

sheared, graphitic, argillite matrix: containing lenses of chert, greywacke and elliptical

shaped conglomerate clasts (Figs. 2.9, 2.10). Pebbles within the conglomerate clasts are

generally sub-rounded to well-rou Wed and consist of mudstone, chert displaying primary

lamination, and sandstone pebbit s. Many pebbles are elongated parallel to foliation.

Clasts of greywacke and finely laniinated mudstone also exhibit remnant primary bedding.

Sheared matrix foliation wraps around clasts. Black carbonaceous argillite also contains

finely disseminated pyrite. A veathered dyke cuts through the western end of the

exposure. Black, bedded chert in the northeastern end of the road-cut were sampled for

radiolarians (Fig. 2.20). Thickncss of chert beds is 3 cm. These beds are now partly

covered by a rubble slide from the level above.

69


Figure 2.20 Field sketch of black be( Med chert beds at northeastern end of locality KLK5 near Bentong.[BENTONG 87 - GR75 ;274].

70


LOCALITY KLK13

Location: Road-cutting, 78 km from Karak (47 mile-post) on the new Kuala Lumpur -

Karak Highway. (Road-cutting 3 km south of Genting Sempah tunnel on the new Kuala

Lumpur - Karak Highway). (Locality map Fig. C.1)


Description:

The rocks at locality KLK13 have been described as sheared diamictite (Metcalfe, 1987)

(Figs. 2.11, 2.12, 2.13). They consist of clasts of tuff, tuffaceous sandstone and mudstone

and minor chert lenses within a matrix of sheared, schistose mudstone matrix. Competent

fault-bounded blocks of bedded mudstone, and rare bedded chert blocks that have escaped

deformation are also found within the chaotic mélange (Fig. 2.21). The clasts are generally

augen-shaped and are elongated parallel to the direction of foliation. They may be

truncated and disrupted, while others show the pinch and swell structure of boudinage.

Foliation of the sheared matrix wraps around the margins of the clasts and produce a wavy,

anastomosing appearance. Some clasts contain a pre-existing foliation, distinct from the

foliation of the matrix. Jointing surfaces, now infilled with iron oxide, are perpendicular to

foliation. Small scale tension gashes are also visible.

The samples that yielded datable radiolarians were collected from the northern end of the

section (Fig. 2.22). Only productive samples and those adjacent are illustrated.

Figure 2.21 Sheared diamictite and internally undeformed block of bedded mudstone at localityKLK13 near Genting Sempah, Bentong-Raub suture zone. [KUALA KUBU BAHARU86 - GR588035]

71

General strike of foliation

Bedded chert and argillite

BR553n

131-2,548Covered andweathered

4m

Covered

BR547)11 BR5,..__,50 BR549

BR554 1PC552BR551

BR543 BR53S

OIBR546 BR542 _aBR540

BR544 BR541 1JBR539-0 BR545


Figure 2.22 Field sketch of pink, gre: and tan chert beds from the northern end of locality KLK13.[KUALA KUBU BAHA RU 86 - GR588035]

LOCALITY KLK31

Location: 2..6 KM east of Lee Rubber Factory on Sungei Laut Bilut Road. (Locality map

Fig. C.3)


Description:: Very weathered, disc upted chert and weathered argillite matrix (Fig. 2.23).

Tan coloured, bedded chert appears as blocks in the outcrop. In some places there is

preservation of bedding.

► 320°

Figure 2.23 Field sketch of blocks of tan, bedded chert at locality KLK31. [BENTONG 87 -GR743342]

72

320'/40*E• ••

‘, • S. • • s,•„,

•• 's

• ‘••

- UBR415 .

• •\BK414-

I- 2m

• • ••

Weathered

1-- lm

, ,

Weathered,,

,'

'•

,' , ,', • V , ‘•,

,,, , ......

„. ..., ',. •. ..

_ _ -

. BR421s. _ , - :.-, 0

- -• -.

_

, • .

... - -- -

, , •

U BR420 _ .... _/ X

/„ ,

' ." ' • . ... _

/ , ■ ' ' --....- '''' '- - _

/ / ,• ..,‘ ' t , • ---

-- „

/

..." ' . / ‘, ‘, %, %,0 BR418 -. - _ - "" .... _ -, -• - - .- - - - -

,I ‘0 312417 • - -

• .


LOCALITY CH6

Location: 60.3 km NE of Brinchar g, near Pos Mering, Cameron Highlands. (Locality map

Fig. C.5)


Description: Olistolith of bedded chert (Fig. 2.24). Beds are 5 - 10cm thick. Length of

section = 10m. Orientation of sect ton = 040°. Orientation of beds = 320°/40°E

040'

Figure 2.24 Field sketch of locality :H6. [KUALA BETIS 44 - GR044226]

LOCALITY CH7

Location: 61.1 km NE of Brinchan g, near Pos Mering, Cameron Highlands. (Locality map

Fig. C.5)


Description: Folded and faulted tuffaceous mudstone and brown chert beds (Fig. 2.25).

Beds approximately 3cm thick. Rocks within the fault zone are carbonaceous and

tuffaceous. Length of section = 8n t. Orientation of section = N-S.

S N

Figure 2.25 Field sketch of locality (7117. [KUALA BETIS 44 - GR044226]

73


LOCALITY CH13

Location: 80.1 km NE of Brinchang, near Pos Blau, Cameron Highlands. (Locality map

Fig. C.5)


Description:

Folded and faulted, green and tan laminated, siliceous argillite and weathered shale

interbeds (Figs. 2.26, 2.27). Beds are approximately 5cm thick. A weathered sill is

located at the northern end of the section. Length of the section = 60 m and orientation of

the section = N-S. Orientation of beds = 320°/30°E.

Figure 2.26 Bedded tuffaceous, siliceous argillite at locality CH13 near Pos Blau, CameronHighlands, Bentong-Raub suture zone. [KUALA BETIS 44 - GR182205]

74

•

•

•I 917118, . n

/0917218 0

6S19118

8stmarl


U

z---------

St't HU 041' „

El ,(NI

' ' 6£17 38 D,

,CEt HITa ,,

,' !Et ag.I1

Figure 2.27 Field sketch of locality ('H13. [KUALA BETIS 44 - GR182205]

C/)

75


LOCALITY CH14

Location: 80.7 km NE of Brinchang, near Pos Blau, Cameron Highlands. (Locality map

Fig. C.5)


Description: Folded and faulted tan-coloured chert, siliceous and tuffaceous argillite with

tuffaceous mudstone interbeds (Figs. 2.28, 2.29A). Beds become more tuffaceous towards

the northern end of the section. At the northern end of the section chert and tuffaceous

sandstone/mudstone interbeds beds dip steeply to the west. Chert beds are 2-5cm thick

and interbedded mudstone 2-8cm thick. Length of section = 70m. Orientation of section =

SW-NE. Generally, beds strike N-S and dip at 25° W.

Figure 2.28 Bedded tuffaceous, siliceous argillite at locality CH14 near Pos Blau, CameronHighlands, Bentong-Raub suture zone. [KUALA BETIS 44 - GR179211[

LOCALITY T3ALocation: NW road-cutting 4 km N of Teras. (Locality map Fig. C.4)


Description: Bedded, folded and faulted, siliceous argillite and chert (Fig. 2.29B). The

section is adjacent to an erosion-resistant sandstone knocker which is probably a clast

within the mélange. Length of section = 40m. The centre of the section is very

weathered, although remnants of bedding (= horizontal and gently folded) can still be seen.

Orientation of section = N-S.

76

\

// / , I\\

/// / • \

CO

\ \

\ \ \ ‘ \ \ , \

• • I \ . \ I

I I I I i I1 I I I t I I , ,,,, ,1 1 1 11 1 21

I I I / I Irni/

/ I / III

I / / / r'/I / 1

I /

I: t

` \ 1 1

\ N I 1 P ' /I / ,0 / / ,/ / c4 / ' / ./ / CO / / , 1

, 171 1 I 1

1 1 ‘ \‘ 1,, ‘ 1 \

\ \, \ \, \ 1-4I\ ‘ \ . Csi I I

I I I 1 R;1 1i I , 1 co:

i ► I I I I I /1 I II I % I I , /1 /

I I \ I 1 / //\ I % 1 I / /1 /\ ‘ ,, I / „, /

I / /

1 I

/ I % /// /i , % ///

I 1 /////

II i ‘ 1 I /// /

, I ‘ // /1 / • /// /\ ‘ ' / / \

I

5917110 uI t

I 1 9917119

\ I I \/ I

% I \.

L917119

I

II

I8917219,

I s' ■

,

I 69171119 in ‘1

\ \

1 1

1 I /I


PC)

Figure 2.29 A: Field sketch of local ty CH14 [KUALA BETIS 44 - GR179211]B: Field sketch of local ty T3A. [RAUB 771

77

4m Co' ered

, , ---N..._...--, :k

---, ,

, , , , I

, , I , , -± ,, I

, , , ' : 1 1. T. %, : I

I

i

, i

, , i

, , II

,

„ ,I

, I I tt I ICovered and

/ / / I I I I1 ” I I weathered (21 m)

1 i D u-, I ,e, NII

I (-4,rs c,

I Q , II ,-.4 . I ,,,N 0, t.... st, inI

in / / en Nc.,,,, I 0, oo I

, / I 1 (.1" cl 1 !. 1, cl '4 :_ 1 1 I (1 el 1, ' ' L'-7)

171,173 = 17:3 n= 1=1 173c 3= 7=377 TE 1 tperipc7rn= =

- „ r , I I -r, -r I I I / r/ i II

„.0 , I I I 1 / 1 I I I I,

., I I I I U II ' I I

I1 1 1

B'

------7- 1-t:, I i 1E 1 1 1 t

iI 1

I I t 1 1 II

3)i 1

i I t 'I : 11

1 I I 13 I 1a I so I Ln

1c■-,

'

ro I ev .-4 i-cs2) ; L' I 1 ; ! 1 L' L' , Ig 1 7 11=1 71 7 E I = ,U I

I, 1 I

I • U I

I I

:I v

i I%

I IIE

\ 2;i'

1 1 i i

/ I II,

00 Cr s I 0 I TS.13

Z N. s. I In Cr> 1;4 -■ , 0 as N.I

i

6" , 1=1 m =s cr, cn r.n 7= 73/L-7,/ , I , . , ,,

ROC!:


2.4.2 Radiolarian sample localities from the "Lower ChertMember" of the Semanggol Formation

LOCALITY KI

Location: 8 km NE of Pokok Sens (Locality map Fig. C.7)

Number of samples collected: 56

Description: This road-cutting is )oorly exposed due to grass cover. Beds appear to dip

subvertically with minor folding ( 'lg. 2.30). Rocktypes include grey and cream siliceous

argillite with some chert beds. Bed thickness ranges from 4 - 30 cm.

N

Length of section = 50 m

B

Length of section = 50 m

Figure 2.30 Field sketch of locality 1:1 near Pokok Sena. [KUALA NERANG 1 - GR266682]

78

I

,,,

O'i

, ,, nyir ,/

/

ul3B4', , 61 U I3135

0 09 / n BB6BB16 0 BB8 Li ,

Quarry rubble

Float samplesBB25 - BB33

BB24"-

B1313 /1'JoBB,.3 n31318

41 BB17 BB15 'BB2 BB16

BBli1B1

a 1313'20BB19 0

CoveredI- 3m --I


LOCALITY K2

Location: Bukit Barak, 11.6 km NE of Pokok Sena. (Locality map Fig. C.7)


Description: Active quarry section. Samples BB4 - BB24 = laminated grey and pink

bedded chert (Figs. 2.31, 2.32, 2.33 ). Beds strike N-S and dip at 60° E to subvertical.

Samples BB25 - BB33 = bedded pelagic limestone and silicified limestone from float

blocks on the floor of the quarry. Original relationship of these beds with the rest of the

sequence is not known. At a low level in the quarry thick (8cm) bands of limestone

contain Upper Triassic (Carnian) cc nodonts (Metcalfe, 1990c).

E

Figure 2.31 Field sketch of locality I< 2 Bukit Barak. [KUALA NERANG 1 - GR.290700]

79


Figure 2.32 Subvertically dipping bedded chert at locality K2 Bt Barak. [KUALA NERANG 1 -GR290700]

Figure 2.33 Subvertically dipping bedded chert at locality K2 Bt Barak. [KUALA NERANG 1 -GR290700]

80

-

CO

, I,

I

Chapter 2: Geology of 'Peninsular Malaysia

LOCALITY K3

Location: Bt Tembaga, 4.8 km NE of Pokok Sena. (Locality map Fig. C.7)


Description:: Tan-coloured, tuffact;ous siliceous argillite beds are tightly folded into box

folds (Figs. 2.23, 2.35, 2.36). Beds are 2 - 6 cm thick and the length of section = 43m.

Orientation of section = 310°.

>0

/41

1-4 /-1

, , F, , , ,

/ = 1 /

ii,

, ,.... g %, - - ,,,.0 U I I (-4 •

I, F.•

15

o>

I

O

ECr)

• CO' , •

• • ••\ •\.• •• •• ••

•,, , % .5p.. i_,....

I I \ ‘‘‘:'7.t‘ • -. ''' , tn.

• `, ' - ._ ....7\ , .... s‘......... , - s,....,...

•

Figure 2.34 Field sketch of locality h3, Bt Te nbaga. [KUALA NERANG 1 -GR240669]

aa

I

P:',-a

0) to 1

4 Ct4' i

/,

40) 0): l

-4,-.; e ,

iii ti 1 ,

I. I I II I ■, ,

1-. •'•‘\ .-/-‘1-'s.0\ • , co •, •,. ,E-I ‘ \• ' - 4711/4,r'I'l ‘• • ' •• , . • ‘,

‘, 1=/ • ‘• ' -• • •• • •• • • /• • • e • •• • • - • •• • • • •• • • - •• • ''.- •‘ •\‘ ,• • •‘, • •

• '0• \•‘‘2,‘2Ecr.es‘,•

NPO

, \•CO

•i/1\ p3 ,

I - 'CO• ,. , ,

• ' 00 •• •1--4

cc

cc

/

..................._

81


Figure 2.35

Tuffaceous, siliceous argillite beds from locality K3 Bt. Tembaga, near Pokok Sena,"Lower Chert Member" of the Semanggol Formation, northwest Peninsular Malaysia.[KUALA NERANG 1 -GR240669]

Figure 2.36 Close view of tuffaceous, siliceous argillite beds from locality K3 Bt. Tembaga, nearPokok Sena, "Lower Chert Member" of the Semanggol Formation, northwest PeninsularMalaysia. [KUALA NERANG 1 -GR240669]

82

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