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Post-Conference Field Excursion to Northwest Peninsular Malaysia: Third International Conference on Palaeontology of South East Asia: ICPSEA 3 10 th -13 th October 2013 Meor Hakif Amir Hassan Geology Department University of Malaya [email protected]

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Page 1: Post-Conference Field Excursion to Northwest · PDF filePost-Conference Field Excursion to Northwest Peninsular Malaysia: ... Kubang Pasu Formation ... The topography of Northwest

Post-Conference Field Excursion to Northwest

Peninsular Malaysia:

Third International Conference on Palaeontology of South East Asia: ICPSEA 3

10th-13th October 2013

Meor Hakif Amir Hassan

Geology Department

University of Malaya

[email protected]

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Contents:

Overview 4

Geological Overview 4

The Stratigraphy 5

Locality 1: Sanai Hill B, Kampung Guar Jentik, Perlis 13

Locality 2: Sanai Hill C, Kampung Guar Jentik, Perlis 15

Locality 3: Bumita Quarry, Kampung Hutan Aji, Perlis 17

Locality 4: Bukit Chondong, Perlis 18

Locality 5: Bukit Tungku Lembu, Perlis 20

Locality 6: Bukit Tuntung, Pauh 21

Locality 7: Machinchang Cambrian Geoforest Park 22

Locality 8: Teluk Mempelam, Pulau Langgun, Langkawi 23

Figures:

Fig. 1: Palaeozoic stratigraphy of Northwest Peninsular Malaysia (Meor et al., in prep.)

Fig. 2: Geological map of Perlis and north Kedah, Northwest Peninsular Malaysia, with field trip

localities marked. Modified from Jones (1981).

Fig. 3: Geological maps of the Perlis localities. (A) Sanai Hill B, Kampung Guar Jentik. (B) Sanai Hill C,

Kampung Guar Jentik. (C) Hutan Aji (Meor et al., in prep.).

Fig. 4: Sanai Hill B, Kampung Guar Jentik. Late Frasnian Sanai limestone (on the left) overlain by

folded chert and black mudstone of the Tournaisian Telaga Jatoh Member, Kubang Pasu Formation

(on the right).

Fig. 5: (A) Cross section of Sanai Hill C. (B) Western face of Sanai Hill C, showing contact between the

Early Devonian Timah Tasoh Formation and Early Carboniferous Chepor Member, Kubang Pasu

Formation (Meor et al., in prep.).

Fig. 6: Mudstone and sandstone of the Early Carboniferous Chepor Member, Kubag Pasu Formation.

Fig. 7: Geological map of the Bukit Chondong and Bukit Tungku Lembu outcrops, central Perlis (Meor

et al., 2013b).

Fig. 8: Sedimentary logs of the Bukit Chondong and Bukit Tungku Lembu outcrops. Location in Fig. 7

(Meor et al., 2013b).

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Fig. 9: (A) View of Bukit Tungku Lembu from the North. (B) Giant symmetrical ripples on bedding

plane of Monodiexodina bed.

Fig. 10: Panorama of the Bukit Tuntung outcrop, Pauh, eastern Perlis.

Fig. 11: Outcrop localities on Langkawi Island.

Fig. 12: N-S transect of Teluk Mempelam, northwest Pulau Langgun, Langkawi. Modified from Jones

(1981).

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Overview

The topography of Northwest Peninsular Malaysia is mostly flat coastal plain. Granite forms the

highest mountains, but is only represented by a small exposure in north Perlis (the Bukit China

granite). However, it makes up the central core of Langkawi Island, rising up to an elevation of 890 m

(Gunung Raya). Limestone forms several N-S trending karstic ridges in Perlis state. The most

impressive is the Setul Boundary range, composed of Palaeozoic limestone, which is a steep,

continuous mountain range with peaks reaching 553 m high and forming a natural border between

West Perlis and Thailand. Numerous small karst hills also crop out of the flat coastal plain. The

Chuping Hills form a N-S trending belt of limestone in the middle of Perlis state. The ridge has been

dissected by several east-west trending rivers to form numerous small isolated hills. Clastic

sedimentary rocks form undulating in many parts of Perlis and North Kedah, with more arenaceous

strate forming more pronounced escarpments, ridges and mountains, again generally trending N-S.

Most spectacular is Mount Machinchang on the western side of Langkawi Island, which is about 700

m high and mainly composed of folded Cambrian quartzite.

Geological Overview

Unlike most other parts of the Western Belt, Northwest Peninsular Malaysia preserves an almost

complete Palaeozoic sedimentary succession, from the Cambrian to the Permian. The sedimentary

succession in Langkawi is strongly deformed by granitic intrusion, but a relatively well preserved

succession is exposed on Pulau Langgun. Cambrian strata are also better represented in Langkawi.

However, the post-Cambrian succession is better preserved on mainland Perlis state and North

Kedah, which are areas far away from extensive granite intrusion. On the mainland, Ordovician to

Permian strata form a roughly N-S trending fold belt. More specifically in Perlis, the stratigraphic

succession generally youngs eastwards starting from the Setul Boundary Range, but repeats itself in

the opposite direction east of the Chuping Hills, which forms the axis of a broad syncline (Jones,

1981). Exposures of carbonates are mainly in the form of steep karst hills and towers, which can

either be isolated or form part of long ranges. Exposures of clastic strata commonly crop out as

small hills or ridges, which have been uplifted due to thrusting and transpressional deformation

(Zaiton and Basir, 2000).

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The Stratigraphy

The geology of Northwest Peninsular Malaysia is dominated by four major stratigraphic divisions: (1)

The Machinchang Formation; (2) The Setul Group; (3) The Kubang Pasu and Singa formations, and;

(4) The Chuping Limestone. There are also several minor, informally designated stratigraphic which

are discussed, as they are important in understanding the Palaeozoic history of the region.

Fig. 1: Palaeozoic stratigraphy of Northwest Peninsular Malaysia (Meor et al., in prep.)

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Machinchang Formation

The Machinchang Formation is an approximately 3 km thick unit of quartzitic sandstone with

subordinate conglomerate, siltstone and mudstone (Lee, 2009). Brachiopods and trilobites indicate a

latest Cambrian to earliest Ordovician age. The succession generally coarsens upward and include

features such as cross beds, wavy bedding, load casts, ripple marks, slump beds and parallel bedding

with fossil and heavy mineral concentrated bands. The Machinchang Formation is interpreted as the

deposits of a highly desctructive, wave-influenced delta and associated estuary and beach-ridge

complex (Lee, 1983; 2009). Regionally metamorphosed equivalents of the unit exposed in central

Kedah are known as the Jerai Formation (Bradford, 1972).

The Setul Group

This is the Setul Limestone Formation of Jones (1981). Lee (2009) upgraded it to Group, as the Lower

and Upper Setul and intercalated “Detrital Members” of Jones (1981) were previously upgraded to

formation status (Cocks et al., 2005). The Setul Group is characterised by a thick succession of

bedded shelly limestone with minor intercalated bands of clastic and siliceous sedimentary rocks,

conformably overlying the Machinchang Formation. The Setul Group is divided into several

formations: (1) Kaki Bukit Limestone; (2) Tanjong Dendang Formation; (3) Mempelam Limestone,

and; (4) Timah Tasoh Formation.

Kaki Bukit Limestone

This is the Lower Setul Limestone of Jones (1981). The Setul Boundary Range of West Perlis is mainly

composed of the Kaki Bukit Limestone. It is also exposed along the eastern side of the the main

Langkawi Islands and adjacent small islands. The Kaki Bukit Limestone has an estimated thickness of

over 1100 m. It is mainly composed of thick bedded, finely crystalline limestone, with sporadic fossil

horizons. The uppermost 150 m, exposed on Pulau Langgun, is composed of reddish stylolitic and

nodular limestone. Brachiopods, gatsropods, cephalopods, trilobites give an Ordovician age (Arenig

to Ashgill) for the Kaki Bukit Limestone (Cocks et al., 2005). Conodonts give a Middle to Late

Ordovician (Arenigian-Ashgillian) age range (Agematsu et al., 2008). The Kaki Bukit Limestone

represents a transgressive succession, from a middle shelf depositional environment during the Mid

Ordovician, to outer shelf or slope during the Late Ordovician (Agematsu et al., 2008).

Tanjong Dendang Formation

The is the Lower Detrital Member of Jones (1981). This is a very thin unit (approximately 60 m thick)

exposed only at Pulau Langgun and Pulau Tanjong Dendang. The unit is composed of well bedded ,

black to dark coloured quartzite, siltstone, shale and chert. The beds contain a latest Ordovician

Hirnantia fauna, which includes the trilobite Mucronaspis mucronata (Cocks et al., 2005). Graptolites

are very common in the unit, and include characteristic of the persculptus, vesiculosus, cyphus,

gregarious, convolutes and sedgwickii Zones, indicating that the Tanjong Dendang Formation ranges

from the Ordovician (Hirnantian) to Silurian (Llandovery) in age (Jones, 1973; Cocks et al., 2005). The

Tanjong Dendang deposits probably represent hemipelagic deposits laid down in an outer shelf of

slope setting (Agematsu et al., 2008).

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Mempelam Limestone

This is the Upper Setul Limestone of Jones (1981). The Mempelam Limestone is well exposed on

Pulau Langgun and also on the mainland at the Sanai Hills (Hills A and B) and Kampung Hutan Aji,

Perlis (Cocks et al., 2005; Meor and Lee, 2005). The unit is composed of dark, well bedded, styolitic

and nodular limestone, with synaeresis cracks. Conodonts are common in the limestone, with a

horizon containing taxa of of the celloni-amorphognathoides Zone indicative of a late Llandovery

age. (Igoe and Koike, 1966; 1968) near the base of the unit. A rich trilobite assemblage (the

Prodontochile fauna) containing 15 species is also present in the basal beds. The upper are also rich

in conodont, with Wenlock or Ludlow age taxa, and taxa spanning the Pridoli-Lochkov boundary near

the top of the Mempelam Limestone. The scyphocrinoid Camarocrinus or Marhoumacrinus is also

present in the topmost beds of the Mempelam Limestone on Pulau Langgun and the Sanai Hills (Hill

A), mainland Perlis (Lee, 2001), which also supports a latest Pridoli or earliest Lochkov age. The

predominance of wackestone and mudstone, associated with stylolites and nodular texture,

combined with the mainly pelagic fossil assemblage indicates a pelagic depositional environment,

possibly in an outer shelf, slope or basinal setting.

Timah Tasoh Formation

This is the black mudstone interval in the lower part of the Upper Detrital Member of Jones (1981).

The unit is up to 40 m in thickness, and is exposed on Pulau Langgun, Langkawi, and on the mainland

in the Sanai Hills in Kampung Guar Jentik and Kampung Hutan Aji, Perlis. The Timah Tasoh Formation

conformably overlies the Mempelam Limestone, with bedded limestone gradually transitioning

upwards into black tentaculitid and graptolite-bearing mudstone. Tentaculitids are abundant and

include taxa such as Nowakia (T.) acuaria acuaria, Nowakia (T.) acuaria posterior and Nowakia (A.)

matlockiensis. Also characteristic of the black mudstone are the graptolite Monograptus

langgunensis, the brachiopod Plectodonta (P.) forteyi and the trilobite Plagiolaria. The tentaculitids

and graptolites indicate a late Pragian or earliest Emsian age (Meor et al., 2013). The Timah Tasoh

Formation is interpreted as representing hemipelagic, dysoxic-anoxic, marine outer shelf deposits,

based on the fine grained lithology, abundance of pelagic taxa and black colour (Meor and Lee,

2005).

Sanai limestone

The Sanai limestone, previously designated Sanai Limestone Member and Sanai Limestone

Formation (Meor and Lee, 2003; 2005), is for now downgraded to an informal unit based on

comments that it is not mappable (Ong and Basir, 2007). The limestone is exposed only at Sanai Hill

B, Kampung Guar Jentik (Meor and Lee, 2003). It unconformably overlies the Timah Tasoh

Formation. The Sanai Limestone resembles the older Mempelam Limestone, in being composed of

bedded stylolitic mudstone and wackestone. However, the Sanai limestone contains Late Devonian

conodonts (Meor and Lee, 2003; Meor et al., in prep.). An initial study suggested a Famennian age,

based on the presence of Palmatolepis glabra and Polygnathus quadrantinodosalobata (Meor and

Lee, 2003). However, present work conducted by Prof. Aye Ko Aung (Meor et al., in prep. And Aye-

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Ko, in prep.) identified the presence of Palmatolepis, Polygnathus, Icriodus, Ancyrodella and

Ancyrognathus. The Sanai limestone is therefore most likely to range from the Middle to Late

Frasnian until Famennian. The interpreted depositional environment is similar to that for the

Mempelam Limestone, i.e. pelagic carbonates deposited in an outer shelf, slope or basinal setting.

Kubang Pasu Formation

The geology of Perlis east of the Setul Boundary and north Kedah is dominated by the mainly

siliciclastic Kubang Pasu Formation (Jones, 1981). The Kubang Pasu Formation is mainly composed of

mudstone of various colours interbedded with quartz and feldspathic sandstone. There appears to

be a continuous succession in Perlis, where clastic strata are sandwiched between Setul Group in the

west (Setul Boundary Range) and the Chuping Hills in the east. Based on this, the estimated

thickness of the unit is approximately 4800 m (assuming there are no major intervals of repeated

strata). The Kubang Pasu Formation unconformably overlies the Timah Tasoh Formation in most

exposures (Pulau Langgun, Sanai Hills A and C, Kampung Hutan Aji), although it conformably overlies

the Sanai limestone at Sanai Hill B. The Kubang Pasu Formation is divided into three sub-units, from

oldest to youngest: (1) Telaga Jatoh Member; (2) Chepor Member; (3) Undifferentiated Kubang Pasu

Formation; (4) Uppermost Kubang Pasu Formation.

Telaga Jatoh Member

Previously referred to as the Telaga Jatoh Formation (Meor and Lee, 2005), the unit is downgraded

to Member status in the Kubang Pasu Formation, based on comments that it is too thin and limited

in extent to be considered a formation (Basir et al., 2010). The Tournaisian chert bed unit is an

important marker bed separating the underlying Devonian units from the Carboniferous Kubang

Pasu Formation, and is widely exposed in Perlis and north Kedah. It is considered to be the base of

the Kubang Pasu Formation, unconformably overlying the Timah Tasoh Formation in most

exposures, but overlies the Sanai limestone locally at Sanai Hill B. The unit can be up to 11 thick, but

commonly pinches out laterally to form discontinuous lenses (Basir et al., 2010). The unit comprises

rhythmically alternating, cm-thick beds of dark coloured chert and black mudstone. Radiolarians

from the chert give an Early Carboniferous (late Tournaisian) age (Basir, 1995; Basir and Zaiton,

2001, 2011; Basir et al., 2003; 2010). The chert beds represent pelagic deposition in an outer shelf to

deep marine setting and maybe associated with high plankton productivity triggered by upwelling of

coldatwr circulating from glacial Gondwana (Basir and Zaiton, 2011b).

Chepor Member

This unit encompasses all the previously described ‘red bed’ formations of Meor and Lee (2005),

including the Bukit Raja, Chepor, Binjal and Wang Kelian formations. This is based on more refined

stratigraphic mapping and correlation, and a better understanding of the biostratigraphy (Meor et

al., 2013). The Chepor Member abruptly overlies the Tournaisian chert bed unit in most outcrops, or

where the chert beds pinch out, directly overlying the Timah Tasoh Formation (e.g. Pulau Langgun,

Kampung Hutan Aji). Rocks of similar lithology and fossil composition are known as the Langgun Red

Beds in Langkawi (Kobayashi and Hamada, 1973). The Chepor Member comprises thick fossiliferous

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mudstone interbedded with mainly tabular beds of quartzitic and feldspathic sandstone and

occasional bedded diamictite. The sandstones display abundant current and wave generate features,

including cross-bedding, symmetrical and asymmetrical ripples, hummocky cross-stratification and

parallel lamination. Dropstones are common in the mudstone and sandstone and are interpreted as

ice rafted debris deposits. The mudstone is rich in fossils, including the bivalve Posidonia,

brachiopods, cyrtosymbolid trilobites, crinoids and ammonoids. The cyrtosymbolid trilobites include

Diacoryphe? sp., which is very similar to Weyeraspis and suggestive of an Early Carboniferous age

(Meor et al., 2013). The discovery of the ammonoids Goniatites and Praedaraelites further restricts

the age of the Chepor Member to the Visean (Meor et al., in press). The Chepor Member probably

represents the deposits of a glacial marine shelf system, with ice rafted debris deposited by icebergs

derived from Australian Gondwana (Meor et al., in prep.).

Undifferentiated Kubang Pasu Formation

Beds of the Kubang Pasu Formation overlying the basal Chepor Member are poorly described and

poorly fossiliferous. Thus, most of the thickness of the Kubang Pasu Formation is lumped together as

the Undifferentiated Kubang Pasu Formation. Lithologically it is similar to the Chepor Member, with

thick mudstone and interbedded sandstone and diamictites (Jones, 1981). Fossils are rare, although

fossil bivalves, brachiopods and crinoid ossicles have been reported. Jones (1981) briefly reported

the occurrence of ammonoids identified as ?Agathiceras and ?Paralegoceras, but these have never

been described in detail. However, the ammonoids and the stratigraphic position of the unit

overlying the Chepor Member suggest a Late Carboniferous age.

Uppermost Kubang Pasu Formation

The Kubang Pasu Formation is conformably overlain by carbonates of the Chuping Limestone. The

uppermost 80m of the unit, commonly known as the “Passage Beds” (Jones, 1981), is exposed at the

foot of the Chuping Hills in central Perlis. The boundary with the Chuping Limestone is gradational,

with clastcis being gradually replaced by limestone upsection. The uppermost Kubang Pasu

Formation succession is composed of several coarsening upward cycles, represented by wave and

storm generated facies (bioturbated mudstone, hummocky cross-stratified sandstone, swaley cross-

stratified sandstone and shell lag deposits). The uppermost Kubang Pasu Formation is interpreted as

representing deposits of a coastal, wave- and storm-influenced shoreface-shelf system (Meor et al.,

2013b). The uppermost Kubang Pasu Formation contains and abundant fossil assemblage, including

algae, fenestellid polyzoa, brachiopods and molluscs (Jones, 1966). The brachiopod Cancrinella cf.

cancrini is also common in the calcarenite beds (Ishii et al., 1972), associated with the nautiloid

Mooreoceras (Niko et al., 2005). Also characteristic of the uppermost Kubang Pasu Formation is the

presence of a 2 m thick bed composed of a dense monospecific concentration of the fusulinid

Monodiexodina shiptoni (Monodiexodina bed). The Monodiexodina bed displays giant symmetrical

ripples on its top surface, with wavelengths of up to 1 m. These also represent storm deposits, with

the Monodiexodina fossils acting as coarse grains, resulting in the formation of giant wave ripples

rather than hummocky beds, which commonly form in finer grained sand (Cummings et al., 2009).

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The presence of Monodiexodina shiptoni indicates a late Early Permian (Kungurian-Roadian) age for

the uppermost Kubang Pasu Formation (Basir and Zaiton, 2001, 2011; Basir et al., 2003; Ueno, 2006).

Singa Formation

The Singa Formation is the lateral equivalent of the Undifferentiated Kubang Pasu Formation. It is

restricted to Langkawi Island. It conformably overlies the Langgun Red Beds on Pulau Langgun, which

is indistinguishable in lithology and fossil content from the Chepor Member of Perlis. The Singa

Formation is lithologically distinct from the Kubang Pasu Formation, being composed of thin bedded,

rapidly alternating black mudstone, silty shale and lithic to quartzitic sandstone, with pebbly

mudstone intervals. Poorly sorted diamictites and megaclasts are common in the middle and upper

part of the formation. The megaclasts and pebbly mudstone have been interpreted as glacial

dropstones deposited as ice rafted debris and diamictites. The Singa Formation is interpreted as

glacial marine deposits (Stauffer and Lee, 1986). A cold water brachiopod assemblage is

characteristic of the Singa Formation in the Kilim area, Langkawi, which includes Spirelytha

petaliformis and Spinomartinia prolifica. The brachiopods indicate an Early Permian (Sakmarian) age

(Basir et al., 1995; Mohd Shafeea Leman, 1996; Shi et al., 1997).

Chuping Limestone

This is the youngest Palaeozoic unit exposed in Northwest Peninsular Malaysia. The Chuping

Limestone forms a series of N-S trending hills in central Perlis and north Kedah. It is also exposed on

Pulau Dayang Bunting, Pulau Jong and Pulau Singa Besar in Langkawi. The Chuping Limestone is

estimated to be about 600 m thick and conformably overlies the uppermost Kubang Pasu Formation

in mainland Perlis and the Singa Formation in Langkawi. It is composed of mainly massive, light

coloured limestone, rich in skeletal grains. The basal beds of the Chuping Limestone contain stacked

grainstone beds displaying hummocky cross-stratification. This indicates a shallow marine, wave-

and storm-influenced depositional setting (offshore/shelf). The basal part of the Chuping Limestone

is rich in fossils, including foraminifera, molluscs, productid brachiopods, echinoderms, rugose corals

and bryozoa. Rao (1988) interpreted a cool temperate climate for the depositional setting of the

Chuping Limestone, based on fossil assemblage, occurrence of detrital quartz grains (possible ice

rafted debris) and δ18O and δ12C values.

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Palaeozoic Outcrops in Perlis

Several localities will be visited in Perlis, mainly exposures of the Late Silurian-Devonian succession

(Sanai Hills B, C, Kampung Hutan Aji and Bukit Tuntung, Pauh) with some Permo-Carboniferous

exposures (Bukit Chondong and Bukit Tungku Lembu).

Fig. 2: Geological map of Perlis and north Kedah, Northwest Peninsular Malaysia, with field trip

localities marked. Modified from Jones (1981).

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Fig. 3: Geological maps of the Perlis localities. (A) Sanai Hill B, Kampung Guar Jentik. (B) Sanai Hill C,

Kampung Guar Jentik. (C) Hutan Aji (Meor et al., in prep.).

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Locality 1: Sanai Hill B, Kampung Guar Jentik, Perlis

Summary: Good exposure of the Devonian-Carboniferous succession, including the Late Devonian

Sanai limestone.

Access: About 14km north of Kangar town centre. Take the Hospital road toeard the north onto Jalan

Abi Tok Hashim. Hill B is the highest hill along the left side of the road, just before the junction to the

Timah Tasoh Dam. It is part of an earthworks quarried which is active at certain times of the year.

There are two sub-localities: (1) southern face; (2) northern face. The southern face is accessed by

walking along the quarry dirt road. A small road connects the northern face to the main road.

Geology: Hill B exposes the most complete Devonian-Carboniferous succession in Perlis state. The

section is approximately 80 m thick, with beds striking NNW-SSE and dipping 23-62 degrees towards

the E. The beds are well bedded, although significant bed thickness variations suggest the presence

of faults along bedding planes. The lowermost 15 m of the section, exposed on the northern side of

the hill, is represented by the topmost beds of the Late Silurian Mempelam Limestone. The topmost

Mempelam Limestone comprises fine grained, cm- to dm- thick, bedded, stylolitic and nodular

limestone, which is dark coloured but weathers to a reddish colour. The unit becomes shalier

upsection, with thinner limestone beds alternating with black mudstone.

The Mempelam Limestone is then gradually overlain by black tentaculitid-bearing shale of the Timah

Tasoh Formation. The unit is only 3 m thick at Hill B. The black shale contains abundant tentaculitid

fossils, including taxa such as Nowakia (T.) acuaria acuaria, Styliolina sp., poorly preserved

monograptids and the brachiopod Plectodonta (P.) forteyi (Ong and Basir, 2007). The tentaculitids

indicate a Late Pragian or earliest Emsian age (Meor et al., 2013).

The Sanai limestone abruptly overlies the Timah Tasoh Formation at Hill B (Meor and Lee, 2003). It

is an approximately 11 m thick unit compsiring cm- to dm-thick, bedded, fine grained and dark

coloured stylolitic limestone. Macrofossils are rare and are mainly in the form of straight-cone

nautiloids. Conodonts from the limestone indicate a Late Devonian age. Previously, the beds were

considered Famennian in age, based on an initial study (Meor and Lee, 2003). More recent collection

and study by Prof. Aye Ko Aung (Univ, Malaya) recovered Frasnian conodonts including Icriodus,

Ancyrodella, Ancyrognathus, Palmatolepis, Polygnathus and Belodella. The conodonts are also

associated with tentaculitids. Most of the tentaculitids appear to be a species of Styliolina, while a

few specimens resemble Nowakia. More detailed work is required to identify these taxa. The top of

the Sanai limestone is well preserved on the southern part of Hill B. Here, the topmost bed contains

a fossil horizon comprising unidentified brachiopods. The stratigraphic position of the Frasnian Sanai

limestone, abruptly overlying the Early Devonian Timah Tasoh Formation, with no abrupt change in

bed orientation between them, indicates the presence of a paraconformity/disconformity.

The Telaga Jatoh Member of the Kubang Pasu Formation overlies the Sanai limestone. It is

approximately 5 m thick and composed of cm-thick, rhythmically alternating beds of chert and black

mudstone. The beds display moderate intraformational folding, and possibly represent slump

deposits. The mudstone is unfossiliferous, but the chert contains radiolarians indicating an Early

Carboniferous (Tournaisian) age (Basir et al., 2010).

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The Chepor Member of the Kubang Pasu Formation directly overlies the Tournaisian chert bed unit.

An approximately 44 m thick section of the unit is exposed at Hill B, which is mainly composed of m-

thick fossiliferous mudstone of various colours, interbedded with dm- to m-thick beds of sandstone

and bedded diamictites. The sandstone beds display sedimentary structures such as symmetrical and

asymmetricl ripples and cross-lamination, cross-bedding, parallel lamination, hummocky cross

stratification and normal grading, and are interpreted as representing ridges, bars and shoal on a

marine shelf. Isolated pebbles and granules commonly penetrate sandstone and mudstone laminae.

The diamictite bed near the top of the section has a muddy sandstone matrix, with floating quartzite

megaclasts. The isolated pebbles and diamictites probably represent dropstones and resedimented,

ice rafted debris deposited in a glacial marine setting. The mudstone is rich in fossils, including

cyrtosymbolid trilobites (Macrobole kedahensis), chonetid and ambocoeliid brachiopods

(Malayanoplia, Echinocoeliopsis), the bivalve Posidonia and disarticulated crinoid ossicles. Also

present is a thin horizon containing abundant unidentified ammonoids.

Fig. 4: Sanai Hill B, Kampung Guar Jentik. Late Frasnian Sanai limestone (on the left) overlain by

folded chert and black mudstone of the Tournaisian Telaga Jatoh Member, Kubang Pasu Formation

(on the right).

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Locality 2: Sanai Hill C, Kampung Guar Jentik, Perlis

Summary: Good exposure of the Devonian-Carboniferous succession, diverse black shale fauna

Access: This is a hill ridge just north of Hill B, and can be accessed using the same road to the

northern part of Hill B.

Geology: The general strike of the beds is similar to Hill B, but the western side of the Hill C ridge

represents the limb of an overturned fold. The lowermost beds exposed on the western side are

present by black shales of the Timah Tasoh Formation. The beds here are particularly rich in fossils,

including the dacryoconarid tentaculitids Nowakia (T.) acuaria acuaria, N. (T.) acuaria posterior;

N.(A.) matlockiensis, Metastyliolina cf. lardeuxi, Styliolina sp, the trilobite Plagiolaria, the brachiopod

Plectodonta (P.) forteyi and the monograptid Monograptus langgunensis, indicative of a Late Pragian

or earliest Emsian age.

The Tournaisian chert bed unit is present at Hill C only as a thin lens pinched between the underlying

Timah Tasoh Formation and overlying Chepor Member, Kubang Pasu Formation. The chert beds are

strongly folded and disappear below a possible thrust fault or decollement surface, which marks the

boundary between the unit and the Chepor Member. The Chepor Member at Hill C is again

composed of thick mudstone interbedded with clean sandstone beds displaying ripple marks and

normal grading. The mudstone contains fossils such as chonetid brachiopods (Malayanoplia,

Tournquistia), trilobites (?Diacoryphe), rugose corals, Posidonia and unidentified gastropods, again

indicative of an Early Carboniferous age.

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Fig. 5: (A) Cross section of Sanai Hill C. (B) Western face of Sanai Hill C, showing contact between the

Early Devonian Timah Tasoh Formation and Early Carboniferous Chepor Member, Kubang Pasu

Formation (Meor et al., in prep.).

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Locality 3: Bumita Quarry, Kampung Hutan Aji, Perlis

Summary: Fossiliferous red mudstone and glacial marine deposits

Access: The quarry is in the middle of the Kampung Hutan Aji Village, about 6km south of Kangar.

Drive south along Jalan Raja Syed Alwi.

Geology: The quarry exposes numerous NNWE-SSE trending sandstone and limestone ridges. The

beds generally dip 70 degrees eastward, although there are also positive flow structures, folded and

thrusted strata. Again, a relatively complete Devonian-Carbonifeorus succession is preserved. The

lowermost beds exposed on the southwestern end of the quarry is represented by bedded nodular

and stylolitic limestone of the Silurian Mempelam Limestone. The limestone is then overlain by black

shale of the Early Devonian Timah Tasoh Formation, which contains fossils of Monograptus

langgunensis and Nowakia (T.) acuaria acuaria. The Tournaisian chert bed unit is absent at Bumita

Quarry. The Timah Tasoh Formation is overlain by the Chepor Member of the Kubang Pasu

Formation. The two units are separated by a fault zone. The Chepor Member succession exposed at

Bumit Quarry is similar to that at Kampung Guar Jentik, with thick mudstone of various colours

interbedded with clean sandstone displaying symmetrical and asymmetrical ripples, planar

lamination and hummocky cross-stratification. The mudstone also contains isolated, subvertically

oriented pebbles penetrating laminae and also onlapped by laminae, interpreted as representing

glacial dropstones. Isolated pebbles in sandstone are subhorizontal and probably represent wave or

current modified ice rafted debris. These again represent glacial marine shelf deposits. Early

Carboniferous fossils are abundant in the mudstone, including cyrtosymbolid trilobites (Waribole,

Langgonbole), brachiopods (Malayanoplia, Tournquistia, Echinocoeliopsis, Emanuella) the bivalve

Posidonia, an unidentified pectinid, rugose and tabulate corals (Michelinia), gastropods, ammonoids

(Goniatites) and disarticulated crinoid ossicles.

Fig. 6: Mudstone and sandstone of the Early Carboniferous Chepor Member, Kubag Pasu Formation.

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Locality 4: Bukit Chondong, Perlis

Accesss: Approximately 13 km north of Kangar. Take Jalan Kaki Bukit road and drive north toward

Padang Besar. Drive until Beseri Town, Turn right at the triple junction to the Maktab Rendah Sains

MARA school. Bukit Chondong is just east of the school. Turn left into quarry entrance.

Geology: Bukit Chondong is a small steep hill forming part of the N-S trending Chuping Hills in central

Perlis. The hill represent the hinge line of a gentle, N-S trending synclinorium extending throughout

the whole of Perlis. The western face of the hill exposes eastward dipping (30-60 degrees) strata of

the uppermost Kubang Pasu Formation and overlying Chuping Limestone. The quarry exposes the

topmost 80 m of the Kubang Pasu Formation and the basal beds of the Chuping Limestone. The

uppermost Kubang Pasu Formation is represented by an approximately 80 m thick succession of

predominantly siliciclastic rocks which can be divided into 11 facies: (1) Mudstone; (2) Graded

Siltstone; (3) Wavy bedding; (4) Rippled sandstone; (5) Cross bedded sandstone; (6) Hummocky

cross-stratified sandstone; (7) Structureless sandstone; (8) Bioturbated sandstone; (9) Coquinite;

(10) Monodiexodina sandstone, and (11) Limestone. The succession is divided into repeating cycles

or parasequences that coarsen upward from mudstone into hummocky cross stratified and cross

bedded sandstone, capped by coquinite or fossil lag deposit. The succession has been interpreted as

representing the distal expression of a wave- and storm-influence coast-shorface depositional

system (Meor et al., 2013).

Fig. 7: Geological map of the Bukit Chondong and Bukit Tungku Lembu outcrops, central Perlis (Meor

et al., 2013b).

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Fossils are common in the uppermost Kubang Pasu Formation, mainly comprising brachiopod valves

and crinoids ossicle concentrate as lag deposits at the base of sandstone beds. Or particular interest

is the presence of a c. 2 m thick Monodiexodina bed near the top of the section. The bed is a

grainstone made up of a dense monospecific concentration of the elongate tests of the foraminifera

Monodiexodina shiptoni. The coquinite and Monodiexodina bed are interpreted as winnowed storm

lag deposits and transgressive lag deposits. The presence of Monodiexodina shiptoni indicates a late

Early Permian (Kungurian-Rodian) age. Bryozoans are also found associated with Monodiexodina,

including Rhombopora. Limestone beds become more common upsection, until it culminated in the

overlying Chuping Limestone. The Chuping Limestone form the steep upper part of the hill and is not

accessible, but it shows general features of the unit, being white in colour and massive.

Fig. 8: Sedimentary logs of the Bukit Chondong and Bukit Tungku Lembu outcrops. Location in Fig. 7

(Meor et al., 2013b).

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Locality 5: Bukit Tungku Lembu, Perlis

Access: Bukit Tungku Lembu is a quarry just on the opposite side of the road from Bukit Chondong.

Geology: Bukit Tungku Lembu is the southern continuation of the Chuping Hill synclinorium

hingeline. The quarry on the western side of the hill again exposes beds of the uppermost Kubang

Pasu Formation. Again, the late Early Permian strata form several coarsening upward parasequences

capped by coquinite, interpreted as the distal expression of a shoreface depositional environment.

The Monodiexodina bed is also exposed at Bukit Tungku Lembu. The bedding plane is exposed and

interestingly, displays giant symmetrical ripples with straight tu undulating crestlines. This supports

the interpretation that the Monodiexodina Bed represents storm deposits, although giant

symmetrical waves formed, rather than the more typical hummocky beds, due to the

Monodiexodina tests acting as very coarse grains (Cummings et al., 2009). Fossils are abundant in

the upper sandstone beds, including gastropods, bivalves, the orthocerid Mooreoceras and the

brachiopod Cancrinella cf. cancrini. The uppermost Kubang Pasu Formation gradually becomes more

calcareous upsection, with the introduction of thin beds of limestone.

The Chuping Limestone overlies the uppermost Kubang Pasu Formation, forming the Bukit Tungku

Lembu hill. The base is well bedded and displays amalgamated beds of hummocky and swaley cross

stratification, indicative of shallow waters and strong wave and storm influence.

Fig. 9: (A) View of Bukit Tungku Lembu from the North. (B) Giant symmetrical ripples on bedding

plane of Monodiexodina bed.

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Locality 6: Bukit Tuntung, Pauh

Access: The Bukit Tuntung quarry is approximately 25 km east of Kangar, in the Arau district of

Perlis.From the Putra Palace Hotel roundabout, take the Persiaran Jubli Emas road towards the east,

until you pass the town of Arau. After Arau, turn left onto the Changlun-Kuala Perlis Highway. Drive

straight, pass Pauh town. Turn into quarry dirt road on the left before Kampung Ulu Pauh.

Geology: Bukit Tuntung forms a N-S trending hill in Pauh area. The strata are strongly deformed,

with beds oriented N-S and mainly dipping steeply towards the east. However, the beds display

strong and possibly isoclinal folding, with associated faulting. A small section on the western side of

the quarry exposes a relatively well preserved Early Carboniferous succession. The beds appear to be

overturned. The lowermost part of the section comprises black to reddish coloured mudstone

interpreted as the Mahang Formation by Basir et al. (2010). The Mahang is the eastern extension of

the Timah Tasoh Formation and probably represents deeper water facies (Lee, 2009). The Mahang

Formation is then overlain by folded, rhythmically interbedded chert and black mudstone of the

Tournaisian Telaga Jatoh Member, Kubang Pasu Formation. Basir et al. (2010) reported the

occurrence of Tournaisian age radiolarians from the beds. Overlying the Telaga Jatoh Formation are

mudstone and interbedded, m-thick sandstone of the Chepor Member, Kubang Pasu Formation. The

sandstone commonly displays normal grading and Bouma sequences, and are interpreted as

turbidites. A mudstone horizon near the base of the Chepor Member, contains abundant ammonoid

fossils. Specimens recently collected from the mudstone have been identified, with the help of Prof.

Thomas Becker, as Praedaraelites and Goniatites. These give an Early Carboniferous (Visean) age.

The occurrence of turbidites interbedded between the mudstone indicates a probable deeper water

depositional environment compared to the Chepor Member in Kampung Guar Jentik and Hutan Aji.

Fig. 10: Panorama of the Bukit Tuntung outcrop, Pauh, eastern Perlis.

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Outcrops of Langkawi

The trip also includes several well known outcrops of Palaeozoic rocks, including: (1) Cambrian

Geopark; (2) Pulau Langgun.

Fig. 11: Outcrop localities on Langkawi Island.

Locality 7: Machinchang Cambrian Geoforest Park

Access: Machinchang Mountain is located in the northwesten corner of the main Langkawi Island.

There is a cable car ride to the top. The topmost cable car platform, which is at the peak of Mount

Machinchang, is at an elevation of 708 m.

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Geology: Mount Machinchang is mainly composed of sandstone and quartzite of the Cambrian

Machinchang Formation. Prolonged erosion of the highly resistant rock has resulted in a unique

landscape, with narrow ridges with sharp crests on the mountain tops and narrow gorges dissecting

the moutntain. The sandstone displays abundant sedimentary structures, including cross-bedding,

ripple marks and load structures. Fossils are rare, mainly in the form of fragmentary saukiid trilobites

and otrhid brachiopods. However, the Machinchang Formation contains a diverse trace fossil

assemblage, including Dictyodora and Palaeodictyon.

Locality 8: Teluk Mempelam, Pulau Langgun, Langkawi

Access: Pulau Langgun is a small island off the northeastern coast of Langkawi main island. Teluk

Mempelam is a bay on the northwestern side of Pulau Langgun. You can rent a boat from Tanjung

Rhu for a day trip to Teluk Mempelam.

Geology: Pulau Langgun is an elongate island mainly composed of Palaeozoic Kaki Bukit and

Mempelam Limestone, which forms hilly karst terrain in the centre of the island and steep cliffs

along the coast. An eastward hading thrust fault runs through the middle of the island. There is also

a large, freshwater filled sinkhole in the middle of the island, which is also located along the fault

(Tasik Langgun). Teluk Mempelam on the northwestern side of the island is unique in that you can

walk through the whole Ordovician-Carboniferous geologic record, from older rocks in the south to

younger rocks in the north. Generally the strata moderately dip ENE.

The southernmost part of Teluk Mempelam is represented by faulted strata of the upper Kaki Bukit

Formation and overlying Tanjong Dendang Formation. The upper Kaki Bukit Limestone is

characterised by thickly bedded grey limestone. Fossils are abundant at certain horizons and include

rare orthocerids, Early Ordovician gastropods including Teiichispira, stromatoporoids, brachiopods

and crinoids. The topmost beds of the Kaki Bukit Limestone and less massive, more nodular and have

a reddish tinge. These beds contains a diverse trilobite fauna, containing 15 Late Ordovician taxa

(Kobayashi and Hamada, 1978). The Kaki Bukit Limestone is interpreted as representing peritidal

carbonates, possibly deepening to more subtidal conditions in the upper part (Wyatt et al., 1993).

The Tanjong Dendang Formation is exposed as two repeating bands, faulted between Kaki Bukit

Limestone, in the southern end of Teluk Mempelam. The lithology of the unit varies from quartzite

to dark shale and chert. Fossils are abundant in the flaggy shale, including graptolites and trilobites.

A Late Ordovician Hirnantian fauna is present, including the trilobite Mucronaspis. Jones (1973)

recorded graptolitesof the vesiculosus, cyphus, gregarious, convolutes and sedgwickii Zones from the

unit, indicating an age range from Ordovician Hirnantian to Silurian Llandovery for the Tanjong

Dendang Formation (Cocks et al., 2005).

North of the Tanjong Dendang Formation are outcrops and boulders of the overlying Mempelam

Limestone. The thickness of the type section onTeluk Mempelam is 198 m. It is mainly composed of

bedded stylolitic limestone, although the topmost beds are composed of nodular limestone

interbedded with thin black shale. A late Llandovery (Telchyian), celloni-amorphognathoides Zone

conodont fauna is known from the lower beds of the Kaki Bukit Limestone (Igo and Koike, 1966,

1968; Idris, 1989; Cocks et al., 2005). A trilobite fauna composed of 15 taxa is also found in the lower

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beds (the Prodontochile fauna of Kobayashi and Hamada ( 1971). Wenlock or early Ludlow have also

been reported from beds higher in the section (Igo and Koike, 1973). The topmost beds of the

Mempelam Limestone contains a Pridoli-Lochkovian conodont fauna. Also present in the uppermost

limestone beds are large globular shaped scyphocrinoid loboliths, which are either Camarocrinus or

Marhoumacrinus (Lee, 2001). These also indicate a latest Pridoli of earliest Lochkov age.

Beds of the uppermost Mempelam Limestone gradually pass upward into black shale of the Timah

Tasoh Formation. The black shales are rich in tentaculitids, including Nowakia (T.) acuaria acuaria

and Styliolina.

The Timah Tasoh Formation is overlain by folded and foliated flaggy rock and quartzite. The age of

the rocks are uncertain. They may either represent basal beds of the Kubang Pasu Formation, or

even possibly Late Devonian strata.

Overlying the folded strata are red mudstone and interbedded quartzite of the Langgun Red Beds,

Singa Formation. The Langgun Red Beds are age equivalent to the Chepor Member of the Kubang

Pasu Formation in mainland Perlis. Both units share the same facies characteristics and the same

fossil assemblage. Fossils include the trilobite Langgonbole vulgaris, the bivalve Posidonia and

brachiopods such as Tournquistia, Malayanoplia and Echinocoeliopsis. The fossils and correlation

with the Chepor Member indicate an Early Carboniferous age. The Teluk Mempelam exposure ends

in the north with a steep limestone cliff, which is upthrusted Kaki Bukit Limestone.

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Fig. 12: N-S transect of Teluk Mempelam, northwest Pulau Langgun, Langkawi. Modified from Jones

(1981).

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Basir, J., Zaiton, H., 2001. Some radiolarians from the bedded chert of the Kubang Pasu formation. Proceeding Annual Geological Conference, Pangkor Island, Perak, 2nd–3rd June, pp. 111–114. Basir, J., Zaiton, H., 2011. Lower Carboniferous (Tournaisian) radiolarians from Peninsular Malaysia and their significance. Geological Society of Malaysia Bulletin 57, 47-54.

Basir, J., Zaiton, H., 2011b. Radiolarian biostratigraphy of Peninsular Malaysia-An update. Geological Society of Malaysia Bulletin 57, 27-38.

Basir, J., Zaiton, H., Siti, N.H., 2003. Black siliceous deposits in Peninsular Malaysia: their occurrence and significance. Bulletin of the Geological Society of Malaysia 46, 149–154. Basir, J., Atilla, B., Nazariah, J., Norhifzan, I., 2010. Occurrence of slate in Perlis and its significance. Bulletin of the Geological Society of Malaysia 56, 75–78. Bradford, E.F., 1972. The geology and mineral resources of the Gunong Jerai area, Kedah. Geological

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Cocks, L.R.M., Fortey, R.A., Lee, C.P., 2005. A review of Lower and Middle Palaeozoic biostratigraphy in west peninsular Malaysia and southern Thailand in its context within the Sibumasu Terrane. Journal of Asian Earth Sciences 24, 703–717. Cummings, D.I., Dumas, S., Dalrymple, R.W. (2009) Fine-grained versus coarse-grained wave ripples generated experimentally under large-scale oscillatory flow. Journal of Sedimentary Research, 79, 83–93. Igo, H., Koike, T., 1966. Ordovician and Silurian conodonts from the Langkawi Islands, Malaya, Part I. Geology and Palaeontology of Southeast Asia 3, 1–29. Igo, H., Koike, T., 1968. Ordovician and Silurian conodonts from the Langkawi Islands, Malaya, Part II. Geology and Palaeontology of Southeast Asia 4, 1–21. Igo, H., Koike, T., 1973. Upper Silurian and Lower Devonian conodonts from the Langkawi Islands, Malaysia with note on conodont fauna of the Thung Song Limestone, southern Thailand and the Setul Limestone, Perlis, Malaysia. Geology and Palaeontology of Southeast Asia 13, 1–22. Ishii, K., Kato, M., Nakamura, K., Nogami, Y., 1972. Permian brachiopods from Bukit Tungku Lembu, Perlis. Journal of Geosciences, Osaka City University 15, 65-76. Jones, C.R., 1966. Geologic Map of Pulau Langkawi. Geological Survey of Malaysia, 1 sheet, scale 1:63,360.

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Jones, C.R., 1973. The Siluro-Devonian graptolite faunas of the Malay Peninsula. Overseas Geology and Mineral Resources 44, 25. Jones, C.R. 1981. The geology and mineral resources of Perlis, north Kedah and the Langkawi Islands. Geological Survey of Malaysia District Memoir 17, 1-257. Kobayashi, T., Hamada, T., 1971. Silurian trilobites from the Langkawi Islands, West Malaysia, with notes on the Dalmanitidae and Raphiophoridae. Geology and Palaeontology of Southeast Asia 9, 87–134. Kobayashi, T., Hamada, T., 1978. Upper Ordovician trilobites from the Langkawi Islands, Malaysia. Geology and Palaeontology of Southeast Asia 19, 1–27. Lee, C.P., 1983. Stratigraphy of the Tarutao and Machinchang Formations. In: Nutalaya, P. (Ed.), Stratigraphic correlation of Thailand and Malaysia. Geological Societies of Thailand and Malaysia, Bangkok, pp. 20–38. Lee, C.P., 2001. Occurrences of Scyphocrinites loboliths in the Upper Silurian Upper Setul limestone of Pulau Langgun, Langkawi, Kedah and Guar Sanai, Berseri, Perlis. Proceedings Geological Society of Malaysia Annual Geological Conference 2001, 99–104. Lee, C.P., 2009. Palaeozoic Stratigraphy. In: Hutchison, C,R., Tan, D.N.K. (Eds.), Geology of Peninsular Malaysia. University of Malaya and Geological Society of Malaysia, Kuala Lumpur, pp. 55–86. Meor, H.A.H., Erdtmann, B.D., Wang, X.F., Lee, C.P., 2013a. Early Devonian graptolites and tentaculitids in northwest Peninsular Malaysia and a revision of the Devonian Carboniferous stratigraphy of the region. Alcheringa: An Australasian Journal of Palaeontology 37(1), 49-63. Meor, H.A.H., Yeow, B.S., Lee, C.P., Abdul Rahman, A.H., 2013b. Facies analysis of the uppermost Kubang Pasu Formation, Perlis: A wave- and storm-influenced coastal depositional system. Sains Malaysiana 42(8), 1091-1100. Meor, H.H., Lee, C.P., 2003. The Sanai Limestone Member—A Devonian limestone unit in Perlis. Bulletin of the Geological Society of Malaysia 46, 137–141. Meor, H.H., Lee, C.P., 2005. The Devonian–Lower Carboniferous succession in Northwest Peninsular Malaysia. Journal of Asian Earth Sciences 24, 719–738. Mohd Shafeea Leman, 1996. The occurrence of brachiopods from pebbly mudstone near Kilim,

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Shi , G.R., Mohd Shafeea Leman, Tan, B.K., 1997. Early Permian brachiopods of Gondwanan affinity

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Stauffer, P.H., Lee, C.P., 1986. Late Paleozoic glacial marine facies in Southeast Asia and its implications. Bulletin of the Geological Society of Malaysia 20, 363–397. Ueno, K., 2006. The Permian a 1160 ntitropical fusulindoidean genus Monodiexodina: Dsitribution, taxonomy, paleobiogeography and paleoecology. Journal of Asian Earth Sciences 26, 380-404. Wyatt, D., Stait, B., Burrett, C., 1983. The Ordovician system in southern Thailand and northern Malaysia. In: Nutalaya, P. (Ed.), Stratigraphic correlation of Thailand and Malaysia. Geological Societies of Thailand and Malaysia, Bangkok, pp. 77-95.

Zaiton, H., Basir, J., 2000. The occurrence of thrusts in north Kedah and Perlis. Proceedings Annual Geological Conference, 17-20.