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]
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
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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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