GEOLOGY OF

THE BELUM – HALA TRANSECT AREA

ALONG THE MALAYSIA–THAILAND BORDER

by

The Malaysian - Thai

Working Group

A joint project carried out by

Minerals and Geoscience Department, Malaysia

and

Department of Mineral Resources, Thailand

The Malaysia-Thailand Border Joint Geological Survey Committee

(MT-JGSC)

2012

GEOLOGICAL PAPERS

VOLUME 9

GEOLOGY OF

THE BELUM-HALA TRANSECT AREA

ALONG THE MALAYSIA-THAILAND BORDER

by

The Malaysian-Thai Working Group

A joint project carried out by

Minerals and Geoscience Department, Malaysia

and

Department of Mineral Resources, Thailand

The Malaysia-Thailand Border Joint Geological Survey Committee

(MT-JGSC)

2012

i

PREFACE

This report together with the accompanying geological map on the scale 1:250,000 is the

result of close cooperation between the Minerals and Geoscience Department Malaysia, and the

Department of Mineral Resources Thailand in resolving problems related to cross border

geological correlation between Malaysia and Thailand. The Transect area covers about 2,020

square kilometres along the common Malaysia-Thailand border. Fieldwork was carried out in

October 2005, January 2010 and March 2010 in the Belum area, Malaysia. A joint field check

was carried out in the Belum area from 9th to 14th March 2010 by the geoscientists from both

Malaysia and Thailand. There was no fieldwork carried out in the Hala area, Thailand due to

security and accessibility reasons (very thick jungle). Thus, geological interpretation in the Hala

area was based on the remote sensing interpretation and correlation of the photogeological units

with the Belum area, Malaysia as well as previous works done in the Batu Melintang-Sungai

Kolok and Pengkalan Hulu-Betong Transects areas.

Problems on the discontinuity of time rock unit boundaries between the various rock units

found on both sides of the common border areas have been satisfactorily resolved. Potential

mineral deposits occur along the border areas but the present security situation, as well as

environmental issues does not encourage the exploitation of these mineral deposits. Future

increase in the price of minerals coupled with advances in mining technology may facilitate joint

exploitation of these mineral deposits.

Dato‟ Yunus Abdul Razak

Director General

Minerals and Geoscience Department

Malaysia

March 2012

Mr. Nitat Pootanakul

Director General

Department of Mineral Resources

Thailand

March 2012

ii

ACKNOWLEDGEMENTS

The Malaysian - Thai Working Group would like to express their gratitude to the Director

General, officers and staffs of the Minerals and Geoscience Department Malaysia (JMG) and

the Director General, officers and staffs of the Department of Mineral Resources, Thailand

(DMR) for their encouragement, support and funding of this project.

Thanks are extended to Mr. Alexander Unya Ambun, Director of Technical Services

Division, Minerals and Geoscience Department Malaysia and Dr. Tawsaporn Nuchanong,

Director of Bureau of Geological Survey, Department of Mineral Resources, Thailand, for

their encouragements during the study.

Thanks also due to all staffs of the Minerals and Geoscience Department Malaysia and

Department of Mineral Resources, Thailand for their involvement in this project either

directly or indirectly. The Malaysian and Thai military, provincials and border police officials

are duly thanked for their assistance in the security matters especially during the field trips in

the Royal Belum State Park and Temengor Lake areas. Last but not least to all local

residences for their support and assistance during the fieldworks.

iii

Geology of the Belum-Hala Transect along the Malaysia-Thailand Border

by

The Malaysian-Thai Working Group

EXECUTIVE SUMMARY

According to the Sixth Meeting of the Malaysia-Thailand Border Joint Geological

Survey Committee held in Kuala Lumpur on 11th

June 2009, both parties have agreed to carry

out the study on the Geology of the Belum-Hala Transect as proposed by the Malaysian-Thai

Working Group. Since then, the project has been carried out by the geoscientists from the

Minerals and Geoscience Department Malaysia and the Department of Mineral Resources

Thailand in 2010 and 2011.

On the Malaysian side, systematic geological mapping in the Belum, Gunung Hulu

Merah and Kerunai areas where the Belum-Hala Transect is located was carried out by the

Geological Survey Department during the year 1991-1993. During that time, the Malaysian

side of the Transect area was mapped on the scale of 1:63,360. For the purpose of this joint

geological mapping, the Malaysian Working Group has undertaken geological field checks

on the scale 1:50,000 at selected localities in October 2005 and January 2010. In the areas

where the ground data is not available, the remote sensing interpretation has been done. Then

the geological map on the scale 1:250,000 was produced and attached to this report.

On the Thai side, the geology mapping of the Belum-Hala Transect area was carried out

based on the remote sensing interpretation and previous works on the Batu Melintang-Sungai

Kolok and Pengkalan Hulu-Betong Transect areas. A geological map based on remote

sensing data has been prepared since January 2010. A joint field check had been carried out

on the Malaysian side of the Transect area close to the Malaysia-Thailand border in

conjuction with the Malaysia-Thailand Working Group Meeting on the Belum-Hala Transect

area that was held from 9th

to 14th

March, 2010 at the Belum Rainforest Resort, Malaysia.

Then the photo-geological map has been improved by using the data and information

collected from the joint field check. In addition, raw data from the field works in the Batu

Melintang-Sungai Kolok and the Pengkalan Hulu-Betong Transect areas were also included

in describing the characteristics of rock units.

The Transect area is covered by the Silurian-Devonian Betong Formation (SDbt),

Carboniferous Tiang schist (Cts), Carboniferous Kubang Pasu/Yaha Formation (Ckp/yh),

Carboniferous-Permian Mangga formation (CPmg) and Permian Gerik formation (Pgk). The

Betong Formation is only exposed on the Thai side, whereas the Mangga formation and the

Gerik formation are only exposed on the Malaysian side.

The photogeological ST1 unit is well exposed as the long, narrow roof pendant area in the

vicinity of the granite/shear zones in the upper central and northwestern parts of the area. The unit

iv

is represented mainly by schist and phyllite, which can be correlated to the metamorphic rocks of

the Silurian-Devonian Betong Formation (SDbt1).

The photogeological ST2 unit forms a long, narrow-shaped roof pendant in the vicinity of the

granite/shear zone in the northwestern part of the Transect area. The characteristic of this unit is

similar to the ST1 unit but has more resistance. The unit is interpreted to be schist, phyllite and

minor quartzite which can be correlated to the metamorphic rocks of the Silurian-Devonian

Betong Formation (SDbt2).

The Tiang schist (Cts) comprises purplish grey to dark grey quartz-mica schist, quartz

schist, quartz-mica-graphite schist and quartz-mica-garnet schist with minor hornfels. The

schist is strongly schistosed, well foliated, consisting essentially of medium-grained

elongated quartz and mica.

On the Malaysian side, the Kubang Pasu/Yaha Formation (Ckp/yh) occupies the Sungai

Kenerong valley in the western and central parts of the Transect area. The rocks in this area

are metamorphosed to hornfels, phyllite, schist, metasandstone and metaconglomerate. On

the Thai side, the Yaha Formation (Ckp/yh: S3) unit is distributed in the south-western part of

the Transect area adjacent to the Malaysia-Thailand border. The unit shows a wide roof pendant

on granite with prominent N-S bedding trace. The unit is characterized by well-bedded sandstone

and shale which can be correlated to the arenaceous and argillaceous facies within the

Carboniferous Kubang Pasu/Yaha Formation (Ckpar/yh1 and Ckpag/yh2).

Only arenaceous facies of the Mangga formation (CPmg) is exposed in the southeastern

part of the Transect area. The arenaceous facies consists of yellowish grey, light grey, thin- to

medium-bedded, fine- to medium-grained metasandstone and metagreywacke interbedded

with minor metasiltstone.

The Gerik formation (Pgk) is distributed in the southwestern part of the Transect area. It

comprises predominantly tuffs of rhyolitic to rhyodacitic composition. In addition, interbeds

of tuffs, limestone, calcareous shale, tuffaceous sandstone and chert as well as siliceous shale

also occur in places. Foliation can be seen in the groundmass of the tuffs as a result of

regional metamorphism.

On the Malaysian side, the igneous rock that is predominantly consists of granitic rock

and distributed as N-S linear masses in the middle part of the Transect area known as the

Main Range Granite. It comprises the Kabut granite (Trgrkt), Merah granite (Trgrmr) and Singor

granite (Trgrsg).

Based on remote sensing interpretation, four types of the granitic rocks are identified on the

Thai side of the Transect area and can be described as follows:

i. The G1 unit that is correlatable with the Merah granite/Bu Do granite (Trgrmr/bd) is widely

distributed as batholith in the eastern-central part of the Transect area and some stocks are

located in the central and western parts. It is also extented to the eastern part of the Belum

area in Malaysia

ii. The G2 unit that is correlatable with the Kabut Granite (Trgrkt) unit is exposed as the N-S

trending batholith in the western part of the Transect area. It is also extented to the Bang

v

Lang reservoir in Thailand and the upper reaches of Sungai Perak in Malaysia. Many roof

pendants are taken place in this granite type.

iii. The G3 unit or Chantharat Granite (Trgrch) is characterized by its medium- to coarse-

grained, sparsely megacrystic to good megacrystic, unfoliated to weakly foliated

biotite granite. It can be traced along the western flank of the Belum-Hala Transect

area.

iv. The G4 unit that is correlatable with the Singor Granite/Hala granite (Trgrsg/hl) is light

grey or leucocratic, fine- to medium-grained, equigranular to inequigranular biotite-

muscovite granite. Tourmaline is also present in significant amount. The Singor

Granite (Trgrsg) occurs as small isolated bodies within the Merah/Bu Do Granite

(Trgrmr/bd) and Kabut Granite/La Sa granite (Trgrkb/ls).

On the Malaysian side, the structural geology is generally corresponds to the regional

tectonic pattern of the Peninsular Malaysia with a slight variance as compared to the regional

pattern in places. The active period of tectonic activity, especially related the Bentong-Raub

Suture Zone during the Triassic might be responsible for the formation of major structures in

the Transect area during which the igneous intrusion and uplifting also occurred.

Structurally, the sedimentary and metamorphic successions of the Lower Paleozoic on the

Thai side are characterised by generally N-S trending strongly, close fold especially in the

Silurian-Devonian succession. The Upper Paleozoic rock sequence generally exhibits the N-S

trend, close and tight folds with fault-bounded units. The strike-slip, normal, reverse, and thrust

faults are trending in N-S, NW-SE and NE-SW directions.

On the Malaysian side, the Transect area was unknown for its economic deposits as there

were no records of prospecting and mining in the past. However, based on regional

geochemical survey carried out by the Minerals and Geoscience Department Malaysia during

1991 to 1993, seven multi-elements anomalous areas had been identified. Other than that,

rock aggregates and dimension stone showing a good potential to be exploited.

On the Thai side, mineral potential area in the Belum area has been studied by the

Department of Mineral Resources Thailand using airborne geophysic and magnetic anomalies

since 2003. The mineralization is found related to the contact metamorphism of granite intrusions

and country rocks, and subsequent hydrothermal activities. The Pb-Zn sulphide mineral potential

area, along the Hala stream, near the Malaysia-Thailand border and small Sn-W potential areas

were observed.

vi

Contents

PREFACE ................................................................................................................................... i

ACKNOWLEDGEMENTS ....................................................................................................... ii

EXECUTIVE SUMMARY ..................................................................................................... iii

1.0 INTRODUCTION ........................................................................................................... 1

2.0 PREVIOUS WORKS AND GEOLOGIC SETTING ................................................... 12

2.1 Previous works ..................................................................................................... 12

2.2 Geologic setting .................................................................................................... 13

3.0 LITHOSTRATIGRAPHY ............................................................................................. 17

3.1 Sedimentary and metamorphic rocks ................................................................... 17 3.1.1 The Betong Formation (SDbt1 and SDbt2).............................................................. 17 3.1.2 Tiang schist (Cts) .................................................................................................. 18

3.1.3 Kubang Pasu/Yaha Formation (Cyh) ..................................................................... 22

3.1.4 Mangga formation (CPmg) .................................................................................... 27 3.1.5 Gerik formation (Pgk) ............................................................................................ 29

3.2 Igneous Rocks ...................................................................................................... 35

3.2.1 Introduction .......................................................................................................... 35

3.2.2 Chantharat Granite (Trgrch) ................................................................................... 41 3.2.3 Kabut Granite/La Sa granite (Trgrkt/ls) ................................................................... 41 3.2.4 Merah Granite/Bu Do granite (Trgrmr/bd) ............................................................... 42

3.2.5 Singor Granite/Hala granite (Trgrsg/hl) ................................................................... 44 3.2.6 Age and correlation .............................................................................................. 46

4.0 STRUCTURAL GEOLOGY ........................................................................................ 47

4.1 Introduction .......................................................................................................... 47 4.2 Bedding ................................................................................................................ 48

4.3 Foliation ................................................................................................................ 48 4.4 Folding .................................................................................................................. 48

4.5 Faulting ................................................................................................................. 49 4.6 Jointing ................................................................................................................. 49

5.0 MINERALS AND OTHER NATURAL RESOURCES .............................................. 53

5.1 Introduction .......................................................................................................... 53

5.2 Geochemical Exploration ..................................................................................... 54 5.3 Other Geological Resources ................................................................................. 58

6.0 DISCUSSION AND CONCLUSION ........................................................................... 59

SELCTED BIBLIOGRAPHY ................................................................................................. 61

APPENDICES ......................................................................................................................... 64

vii

LIST OF FIGURES

Figure 1: Location map of the Belum-Hala Transect area .......................................................... 1 Figure 2: Location of the Pengkalan Hulu-Betong Transect as compared to the earlier

Transcet areas............................................................................................................... 2

Figure 3: The Transect area on the Malaysian side covered by topographic map sheets scale

1:50,000 ....................................................................................................................... 2 Figure 4: The Transect area on the Thai side covered by on the topographic map sheets

scale 1:50,000 .............................................................................................................. 3 Figure 5: Rafflesia azlanii ........................................................................................................... 4

Figure 6: Landsat TM satellite image of the Transect area. ........................................................ 5

Figure 7: Photogeological interpretation map of the Malaysian side of the Transect area ......... 7 Figure 8: Photogeological interpretation map of the Thai side of the Transect area .................. 9

Figure 9: Three dimensional surface view of Landsat 7 image of the Belum-Hala Transect

area. ............................................................................................................................ 11 Figure 10: Elevation map of the Belum-Hala Transect area ....................................................... 11 Figure 11: The three “Belts” of the Peninsular Malaysia and the northwestern domain within

the Western Belt. ........................................................................................................ 14

Figure 12: Generalised geologic sequence of the Belum-Hala Transect area (Malaysian side). 16

Figure 13: Schematic lithostratigraphic correlation for the Transect area. ................................. 17 Figure 14: Outcrop of the Tiang schist at Km 66.1 ..................................................................... 21

Figure 15: Close-up view of the Tiang schist. ............................................................................. 21 Figure 16: Exposures of quartz-mica-garnet schist at 5

o 45‟ N, 101

o 38‟ E, upper reaches of

Sungai Machang......................................................................................................... 21 Figure 17: The metaconglomerate exposures are limited within the vicinity of river mouth of

Sungai Tan Hain (05o 44.884‟ N, 101

o23.389‟ E) ..................................................... 26

Figure 18: Various size of quartz clasts within the conglomerate............................................... 26 Figure 19: Dark grey mudstone clasts that is up to 5 cm in diameter. ........................................ 26

Figure 20: Cross-bedding observed on the top part of the sandstone beds grading from the

conglomerate. ............................................................................................................. 26

Figure 21: Exposures of the psammitic unit of the Mangga formation near TM

Communication Tower at Km 173.2 of the East-West Highway. ............................. 28 Figure 22: Close up view of the psammitic unit of the Mangga formation near TM

Communication Tower at Km 173.2 of the East-West Highway. ............................. 28

Figure 23: Deformed metatuff of the Gerik Formation expose at river mouth of Sungai

Kenarong. ................................................................................................................... 32

Figure 24: Deformed metatuff of the Gerik Formation expose at river mouth of Sungai

Kenarong. ................................................................................................................... 32 Figure 25: Tuffaceous sandstone expose at Km 34 of the East-West Highway. ........................ 33 Figure 26: Close-up of the tuffaceous sandstone expose at Km 34 of the East-West Highway. 33 Figure 27: Bedded metasandstone at Sungai Ta Eng. ................................................................. 33

Figure 28: Cross-bedding in the metasandstone bed. .................................................................. 33 Figure 29: Calcareous facies expose at the river mouth of Sungai Gadong. ............................... 33 Figure 30: Calcareous facies expose at river mouth of Sungai Gadong...................................... 33 Figure 31: Subvertical to vertical strata of well-bedded light grey to grey radiolarian bearing

chert and silliceous shale interbedded with thin beds of shale at Km 18.6 East-

West Highway (5o 31.655‟ N, 101

o 14.790‟ E). ......................................................... 34

Figure 32: Thinly-bedded radiolarian bearing siliceous shale interbedded with thin beds of

shale located at the old stretch of the East-West Highway (5o 31.633‟ N,

101o 17.633‟ E). ......................................................................................................... 34

viii

Figure 33: Geological setting of the granites in Peninsular Malaysia. ........................................ 37 Figure 34: Distribution of granitic rocks exposed in the Transect area ...................................... 40 Figure 35: Photographs of the Kabut Granit/La Sa granite (Trgrkb/ls) in Malaysia at Km 56.6

of the East-West Highway. ........................................................................................ 42 Figure 36: Photographs of the Kabut Granit/La Sa granite (Trgrkb/ls) in Sungai Singor area on

the Malaysian side...................................................................................................... 42 Figure 37: Photographs of the Merah Granite/Bu Do granite (Trgrmr/bd) in Malaysia at Sungai

Kejar area. .................................................................................................................. 43 Figure 38: Photographs of the Merah Granite/Bu Do granite (Trgrmr/bd) in Malaysia at Km

56.6 of the East-West Highway.. ............................................................................... 43

Figure 39: Photographs of the Singor Granite/Hala granite (Trgrsg/hl) in Malaysia at the Sungai

Singor area. ................................................................................................................ 45

Figure 40: Photographs of the highly fractured Singor Granite/Hala granite (Trgrsg/hl) in

Malaysia at the Sungai Kejar area. ............................................................................ 45 Figure 41: Microphotograph of Singor Granite/Hala granite (Trgrsg/hl) shows euhedral to

subhedral tourmaline at Sungai Palai. ........................................................................ 46 Figure 42: Lineaments interpreted as the Ruok Fault Zone that almost parallel with the

Temengor Lake orientation ........................................................................................ 50 Figure 43: Location of the Ruok Fault Zone ............................................................................... 51

Figure 44: The Ruok Fault Zone crosses the East-West Highway at km 184 towards Kota

Baharu (208 km towards Ipoh) (05o 34.521‟ N, 101

o 24.289‟ E). ............................. 52

Figure 45: Numerous sigmoidal quartzs within the schist in the Ruok Fault Zone at km 184

towards Kota Baharu (05o 34.521‟ N, 101

o 24.289‟ E). ............................................ 52

Figure 46: Mining activities in the surrounding areas. ................................................................ 54 Figure 47: Anomaly map of the Transect area. ........................................................................... 56

Figure 48: Abandoned granite quarry at Km 61.6 of the East-West Highway. .......................... 58 Figure 49: Abandoned granite quarries at Km 63.3 of the East-West Highway. ........................ 58

LIST OF TABLES

Table 1: Photo-geological units of the Malaysian side (Belum) of the Transect area .................. 6

Table 2: Photo-characteristic and correlation unit on the Thai side of the Transect area ........... 10 Table 3: Simplified geological sequence of igneous rocks on the Malaysian side of the Transect

area. ............................................................................................................................... 38

Table 4: Correlation of igneous rocks on the Malaysian side of the Transect area .................... 38 Table 5: Summary of anomalies on the Malaysian side of the Transect area. ............................ 57

1

1.0 INTRODUCTION

During the Sixth Meeting of the Malaysia-Thailand Border Joint Geological Survey

Committee held in Kuala Lumpur on 11th

June 2009, both parties have agreed to carry out the

study on the Geology of the Belum-Hala Transect which was proposed by the Malaysian and

Thai Working Groups of the Malaysia-Thailand Border Joint Geological Survey Committee

(MT-JGSC) within the period 2010-2011. The Transect area is bounded by latitude 05o 30‟ N

to 06o 00‟ N and; by longitude 101

o 15‟ E to 101

o 35‟ E covering an area of 2,020 square

kilometers (Figure 1). It is located between the Pengkalan Hulu-Betong Transect on the west

and the Batu Melintang-Sungai Kolok Transect on the east (Malaysian-Thai Working Group,

2006 & 2010). Figure shows location of the Transect area as compared to the earlier

Transects.

Figure 1: Location map of the Belum-Hala Transect area

On the Malaysian side, the Transect area covers approximately 1,770 square kilometers

along the Malaysia-Thailand border. It is covered by four topographic map sheets on the

2

scale 1:50,000 i.e. nos. 3666 (Tasek Temengor), 3667 (Belum) as shown in Figure 3. The

Transect area lies to the northeast of Gerik Township, in the district of Upper Perak. The

access road to the Transect area is through the East-West Highway, the only road connecting

Gerik in Upper Perak with Jeli in west Malaysia.

Figure 2: Location of the Pengkalan Hulu-Betong Transect as compared to the earlier Transcet areas

Figure 3: The Transect area on the Malaysian side covered by topographic map sheets scale 1:50,000

3

On the Thai side, the Belum-Hala Transect area covers approximately 350 square

kilometres along the border (Figure 4) and is geographically covered by two topographic map

sheets (scale 1:50,000) of Khao Hun Kut (5220 I) and Ban To Mo (5320 IV) Quadrangles.

Figure 4: The Transect area on the Thai side covered by on the topographic map sheets scale 1:50,000

On the Malaysian side, the Transect area that stretches from the East-West Highway up

to the Malaysia-Thailand Border in the north is located within the Royal Belum State Park.

The state park is administered and managed by the Perak State Park Cooperation, an agency

under the State Government of Perak. Previously, the entire forest of the Royal Belum State

Park was considered as a „black area‟ and was placed under a state of emergency from 1948

until 1989 due to extremely active subversive of the Communist Party of Malaya (CPM).

According to sources, when the highway was under construction, the stretch constructed

crossing the Belum area was constantly under threat of being bombed and sabotaged by

renegades.

Most of the Transect area is mountainous terrain geomorphology covered by dense

forest; The Royal Belum State Park, mostly grown by Dipterocarpus sp. One of the

attractions to the Royal Belum State Park is the occurrence of Rafflesia, the biggest flower in

the world. Previously there were two species of Rafflesia found in this area, namely Rafflesia

cantleyi and R. hasselttii. In 2004, a new species of Rafflesia was discovered, known as

R. azlanii, named after the Sultan of Perak, His Royal Highness Sultan Azlan Shah

(Figure 5).

On the Thai side, the Transect area is situated in the Hala-Bala Wildlife Sanctuary.

Geomorphologically, the Belum-Hala Transect area on the Thai side covers mostly of

mountainous terrain (so-called the Hala mountainous terrain) with dense forest (90%).

Another 10% of the eastern part is covered by relatively undulating terrains with rubber and

oil palm plantation. In the western part, the mountainous area shows the high elevation (750-

950 m above MSL) at the Malaysia-Thailand border and decreases northwardly in elevation

4

to 200-300 m MSL at Bang Lang reservoir. The central-eastern part of the Transect area on

the Thai side is a plateau of high elevation mountainous terrain (1,000-1,400 m above MSL)

showing drop valley morphology around the plateau. The highest elevation of this mountain

is 1,490 m MSL. The eastern part of the Transect area consists of the N-S trending elongated

mountain and low-lying areas. General elevation of these terrains is about 200-600 m above

MSL. The main river of the Transect area on the Thai side is the Hala River originated from

the Hun Kut-Bu Lo mountainous area.

Figure 5: Rafflesia azlanii

The climate is Tropical Rainforest type (Koppen`s: „Af‟ climate). The mean annual

rainfall for 30 years (1951-1980) was 2,618.8 mm. The hottest month is May (28.4C in

average) and the coldest month is December (25.9C).

The geology of the Transect area on the Malaysian side was compiled based on the

geological maps on the scale of 1:63,360 covered by topographic map sheet nos. 19

(Kerunai), 20 (Belum) and 11 (Gunung Ulu Merah). Detailed geology and mineral resources

of those areas had been reported by Mohamad Hussein Jamaluddin et al. (in manuscript) and

Mohd Badzran et al. (in manuscript). The areas had been mapped systematically in the early

to middle nineties. Later, in early 2010, for the purpose of preparing this report, the

Malaysian Working Group has re-studied geology of the area briefly on the scale of 1:50,000.

Due to time and budget constrain, the Malaysian Working Group has only managed to re-

check the geology of the Transect area along the East-West Highway and at the selected

localities in the Temengor Lake area.

Besides field data, aerial photograph and Landsat TM satellite imageries have been used

in the interpretation of some of the geological boundaries and major geological structures in

the Transect area especially on the Thai side, which no accesiblity. Enhanced false colour

composites of satellite data were used. In Malaysia, the black-and-white aerial photographs

covering the Belum area on the scale 1:25,000 taken in 1966-1967 were also used. The main

objectives of the remote sensing study are to demarcate the regional geological structures

which are lacking in existing maps as well as the extensions and correlation of existing rock

units across the border.

Digital image processing was carried out with Landsat TM scene 127/56 (18.01.96) on

the ERDAS IMAGINE image processing system. The data covering the study area was

5

extracted from the geo-coded (rectified to RSO projection) full scene. Image of the study area

which is the subset of the full scene were generated for further processing (Figure 6 ).

Figure 6: Landsat TM satellite image of the Transect area.

The spectral bands corresponding to one visible red band (3) and two infrared bands

(4 and 5) were chosen for analysis. False colour composite (RGB 453) generated from these

bands was subjected to contrast stretches and selected filtering process to generate 1: 100,000

hard-copy imagery.

On the Malaysian side, sixteen major broadly generalized photolithological units were

identified to fall under four main categories: sediment/metasediment, volcanic/pyroclastic,

plutonic/granitoid and alluvium as shown in Figure 7. List of the photo characteristics are

given in Table 1. The rocks occur generally in almost parallel north-south aligned belts. The

6

photolithological units are described in the corresponding rock units which was interpreted

and confirmed by ground truthing.

Table 1: Photo-geological units of the Malaysian side (Belum) of the Transect area

Nos. Photo-

lithological Unit

Topography Drainage

Pattern And

Texture

Erosional Feature Photo Tone Of

Colour

Composite

Vegetation

And Land Use

1. Alluvium A1 Low and flat

area

Principal

stream flow

Principal stream Bluish light

green

Agriculture

and settlement

2. Tuffaceous shale

V6

Moderate relief

with a major

ridge

Trellis drainage

pattern with

fine texture

Small gullies

perpendicular to

the ridge

Yellowish

brown

Forest

3. Metatuff V5 High relief with

a major ridge

Trellis drainage

pattern with

coarse texture

Moderate gullies

perpendicular to

the ridge

Yellowish dark

brown

Forest

4. Tuffaceous

sandstone V4

High relief with

irregular hill

ridge

Dendritic and

trellis drainage

pattern with

coarse texture

Moderate gullies

with irregular

orientations

Brown Forest

5. Slaty tuff V3 Moderate relief

with parallel

ridges

Trellis drainage

pattern with

moderate

texture

Moderate gullies

perpendicular to

the ridge

Reddish

moderate brown

and disturbed

forest

6. Phyllitic tuff V2 Moderate relief

with parallel

ridges

Trellis drainage

pattern with

fine texture

Small gullies

perpendicular to

the ridge

Yellowish

moderate brown

, disturbed

forest and

settlement

7. Schistose tuff V1 Moderate to

high relief with

parallel ridges

Trellis drainage

pattern with

moderate

texture

Moderate gullies

perpendicular to

the ridge

Yellowish

moderate brown

, disturbed

forest and

settlement

8. Argillaceous

rocks S6

Moderate relief

with sharp

irregular ridges

Dendritic

drainage

pattern with

fine texture

Small gullies

with irregular

orientations

Dark brown Forest and

disturbed

forest

7

Figure 7: Photogeological interpretation map of the Malaysian side of the Transect area

In Thailand, the remote sensing work activities comprise image processing and

geological data interpretation from Landsat 7 imagery band 4, 5 and 7 as well as aerial

photograph. Geological interpretation including lineament mapping of the satellite data was

exclusively carried out on hard copy plots of the digitally enhanced satellite data for visual

interpretation. The visually extracted information can be annotated either onto a transparency

sheet overlaying the plotted-image or it can be digitized directly on the computer screen using

Geographic Information Systems (GIS). Accordingly, geological interpretation of the aerial

photography was done by visual interpretation.

Photogeological map interpretated from the Landsat 7 imagery is able to demarcate four

units of sedimentary and metamorphic rocks, and five units of igneous rocks (Figure 8). The

8

photogeological map interpreted from aerial photograph is able identify six units of

sedimentary and metamorphic rocks, and four units of igneous rocks, as shown in Table 2.

The final task, the geological map of the Belum-Hala Transect area on the Thai side was

compiled based on the remote sensing geological map and the geological data from

fieldworks in the Batu Melintang-Sungai Kolok Transect area and the Pengkalan Hulu-

Betong Transect area. Three dimensional surface view of Landsat 7 image and elevation map

of the Belum-Hala Transect area are shown in Figures 9 and 10.

9

Figure 8: Photogeological interpretation map of the Thai side of the Transect area

10

Table 2: Photo-characteristic and correlation unit on the Thai side of the Transect area

Unit Photo-characteristic Correlation unit

Unit

ST4

The S4 unit is interpreted as Schist, Phylite, Shale and sandstone.

This unit is distributed in the north-eastern corner of the study area,

low-relief. The unit has grey tone, granular texture, and

mountainous landform with moderate resistance, dense vegetation

and forest land use. Drainage pattern is persistent lines, moderate to

high density, dendritic type. Several joint directions and inferred

boundary are also remarked in this unit.

Tiang Schist (Cts)

Unit

ST3

The unit has dark grey tone, granular texture, and mountainous

landform with high resistance, dense vegetation and forest land use.

Drainage pattern is persistent lines, moderate to high density,

dendritic and trellis type. The good bedding trace, moderate

attitude, several joint directions and inferred boundary are also

remarked in this unit. This unit was interpreted as sandstone and

shale.

Kubang Pasu/Yaha

Formation (Ckb/yh)

Unit

ST2

The Unit S2 show dark grey tone and moderate to high resistant.

The unit has grey tone, granular texture, and mountainous landform

with moderate resistance, dense vegetation and forest land use. The

drainage pattern is persistent lines, moderate to high density,

dendritic type. Several joint directions and inferred boundary are

also remarked in this unit. This unit was interpreted as shale and

sandstone.

Kroh/Betong Formation

(SDkr/bt2)

Unit

ST1

The unit has grey tone, granular texture, and mountainous landform

with moderate resistance, dense vegetation and forest land use.

Drainage pattern is persistent lines, moderate to high density,

dendritic type. Several joint directions and inferred boundary are

also remarked in this unit. This unit was interpreted as schist and

phyllite.

Kroh/Betong Formation

(SDkr/bt1)

Unit

GT4

The unit has grey tone, granular texture, mountainous landform,

circular feature with moderate resistance, moderate to dense

vegetation and forest land use. This unit was interpreted as granite

Singor granite (Trgrsg)/

Hala granite (Trgrhl)

Unit

GT3

The unit has grey to dark grey tone, granular texture, mountainous

landform with high resistance, moderate to dense vegetation and

forest land use. Drainage pattern is persistent lines, moderate

density, and dendritic type. Several joint directions and sharp

boundary are also remarked in this unit. This unit was interpreted as

granite.

Chantrarat granite (Trgrch)

Unit

GT2

The unit has dark grey tone, granular texture, and mountainous

landform with moderate to high resistance, moderate to dense

vegetation and forest land use. Drainage pattern is persistent lines,

moderate density, and dendritic pattern. Several joint directions and

sharp boundary are also remarked in this unit. This unit was

interpreted as granite.

Kabut granite (Trgrkt)/

Lasa granite (Trgrls)

Unit

GT1

The photo-characteristic of this unit is grey to dark grey tone,

granular texture, mountainous landform with moderate resistance,

moderate to dense vegetation and forest land use. Drainage pattern

is persistent lines, moderate density, and dendritic pattern. Several

joint directions and sharp boundary are also remarked in this unit.

This unit was interpreted as shale and siltstone.

Merah granite/Bu Do

granite (Trgrmr/bd)

11

Figure 9: Three dimensional surface view of Landsat 7 image of the Belum-Hala Transect area.

Figure 10: Elevation map of the Belum-Hala Transect area

12

2.0 PREVIOUS WORKS AND GEOLOGIC SETTING

2.1 Previous works

The Malaysian side of the Transect area had been systematically mapped on the scale

1:63,360 by the Geological Survey Department Malaysia in 1991-1993. Most of the middle

part of the Transect area that covered by topographic map sheet no. 20 (Belum) and no. 11

(Gunung Ulu Merah) had been mapped by Mohamad Hussein et al. (in manuscript). The

western part of the Transect area covered by topographic map sheet no. 19 (Kerunai) was

mapped by Mohd Badzran et al. (in manuscript), and the eastern part that partly covered by

topographic map sheet no. 21 (Batu Melintang) and no. 12 (Belum) was mapped by

Mohamad Hussein et al. (in manuscript). Mohamad Sari et al. (in manuscript) mapped the

sheet no. 32 (Temengor) covering the area south of Belum.

The rock sequence consisting of quartz-muscovite schist, quartz-biotite schist, quartz-

biotite-muscovite schist, quartz-sericite schist and quartz schist in the Belum and Temengor

areas had been mapped as the Tiang schist by Mohamad Hussein et al. (in manuscript).

Quartz-mica-garnet schist and silimanite gneiss occur locally.

Mohamad Hussein et al. (in manuscript) introduced the term Mangga formation to

describe the sequence of chert, siliceous shale, phillite, greywacke and sandstone with tuff

lenses exposed on the eastern margin of Main Range Granite. Subsequently, Mohamad Sari

et al. (in manuscript) includes the sequence of metagreywacke and metasandstone exposed in

the vicinity of Temengor to the south of the Transect area as part of the Mangga formation.

MacDonald (1953) mentioned in his field record about an exposure composed of lenses

and bands of schist and hornfels occurred within the black limestone believed to be part of

the olistostrome unit. Wong (1974) reported the occurrence of sequence of upper greenschist

to lower amphibolites schist metamorphic grades in this area which are common in the suture

zone. The rocks are schists and gneisses containing muscovite, biotite, andalusite and garnet.

Hornblende amphibolite is conformable with the pellitic schist. Subsequently Tjia (1989a)

and Tajul Anuar (1989) proposed the zone as the extension of the Bentong-Raub Suture Zone

in the Transect area. In addition, Mohd Raji (1990) who studied in detail geology around

Batu Melintang area, reported the occurrence of muscovite-quartz schist, garnet-muscovite

schist, silimanite-muscovite schist, biotite-hornblend schist, hornblend-epidote schist and

biotite-hornblende gneiss.

Hutchison and Taylor (1978) proposed three geographical granite belts in the Malay

peninsula based on lithology and petrochemistry of the granite. The Eastern belt granitoids

are composed mostly of I-type, magnetite-series granitoids, which intruded the Palaeozoic

host rocks during Permo-Triassic period. The Main Range granitoids (in the central belt area)

are composed mainly of S-type, ilmenite-series granitoids with minor intrusions of I-type,

magnetite-series granitoids. They also intruded the Palaeozoic country rocks in the Permo-

13

Triassic age. The western belt granitoids on the Thai side consist of both I-type, magnetite-

series granitoids and S-type, ilmenite-series granitoids of Cretaceous age.

On the Thai side, the Belum-Hala Transect area was first mapped by the Geological

Survey Division, Department of Mineral Resources Thailand (Muenlek et al., 1979) on scale

1:250,000 of sheet NB 47-12 (Betong District; reprinted in 1985). Muenlek et al. (1979) also

introduced the Silurian-Devonian rocks as the Ban To and Betong Formations. The former

consists of recrystallised limestones to marble, quartzite, phyllite, phyllitic schist and mica-

schist, and the latter comprises shales with Tentaculites elegans, cherts, siliceous shales,

metatuff, carbonaceous shales, argillite, mudstones, sandstones, and bedded recrystallised

limestones.

Muenlek et al. (1982) published a regional geological map of the Narathiwat Sheet on

the scale 1:250,000. The individual granite pluton was preliminarily studied petrographically

and subsequently three granite phases were classified as gneissic granite, coarse-grained

porphyritic biotite granite and tourmaline-muscovite granite.

Cobbing et al. (1986) completed a Southeast Asian granite project including the

geological map of individual granite plutons, petrography, geochemistry and Rb/Sr age

determination studies. They suggested that the granites in the east coast of Malaysia-Thailand

peninsula are mainly of Triassic age.

Tonnayopas (1994) studied the geology and stratigraphy of the Bang Lang Dam area

situated in the northeastern part of the Transect area. He suggested that the Bang Lang dam

site could be mainly covered by the Kanchanaburi Formation which consists of sandstone,

shale, argillite and schist, with igneous intrusion to the west of the Dam site. The formation

could be separated into the Bang Lang Formation consisting mainly of clastic sedimentary

rocks and underlying the Hala Formation comprising metamorphic rocks with an angular

unconformity contact.

Utha-aroon et al. (2000) reviewed the mineral resources near the Malaysia-Thailand

border. They suggested that the mineralizations were related to granite intrusion and

subsequent hydrothermal activities.

Chanrungrot (2003) studied the economic geology and mineral potential on scale

1:250,000 of sheet NB 47-12. He proposed the potential of Pb-Zn and Sn-W in the Belum-

Hala Transect area.

2.2 Geologic setting

Based on differences of stratigraphy, mineralisation and structure, Peninsular Malaysia

had been divided into three north-south trending zones referred to as the Western, Central and

Eastern “Belts”. Some authors have recognized a Northwestern Domain within the Western

Belt that covers part of Kedah, Perlis and Langkawi Islands (Figure 11).

The Transect area lies in the western margin of the Central Belt. The major structural

geology features occurs in the Transect area is the Bentong-Raub Suture Zone that running

accross the eastern part of the Transect area in the north-south direction. The Bentong-Raub

14

Suture Zone represents a segment of the main Devonian to Middle Triassic Palaeo-Tethys

Ocean, and forms the boundary between the Gondwana-derived Sibumasu and Indochina

terranes (Metcalfe, 2000). It extends from Thailand where it is known as the Sra Kaeo and

Nan-Uttaradit Suture Zone, through the Transect area to Raub and Bentong, and then to the

east of Melaka, Peninsular Malaysia. The suture is exposed as an approximately 20 km wide

zone bordering the eastern limit of the Main Range granitoids and comprises melange,

oceanic ribbon-bedded cherts, schist, and discontinuous, narrow, elongate bodies of

serpentinised mafic-ultramafic rocks, interpreted as ophiolite (Hutchison, 1975, 1989; Tjia,

1987, 1989a,b).

Figure 11: The three “Belts” of the Peninsular Malaysia and the northwestern domain within the Western Belt

(after Lee, 2009).

100 EO

101 E 102 E 103 E 104 EO O O O

100 EO

101 E 102 E 103 EO O O

7O

6O

5O

4O

3O

2O

7O

5O

4O

3O

2O

THAILAN

D

LANGKAWI ISLANDS

NORTHWESTERNDOMAIN

PERLIS

KEDAH

PENANGKELANTAN

TER

EN

GG

AN

U

PA

HA

NG

PE

RA

K

SE

LA

NG

OR

NEGERISEMBILAN

MELAKA

JOHOR

S T R

A I T S

O F M

E L A

K A

S O

UT

H C

H I N

A S

E A

SUMATRA

W E

S T

E R

N B

E L

T

C E

N T

R A

L B

E L

T

E A

S T

E R

N B

E L

T

0 50 100 km

P. Tioman

SINGAPORE

15

The rock units on the Malaysian side of Transect area range from Carboniferous to

Quaternary in age. Upper Palaeozoic rock is represented by the Carboniferous Kubang Pasu

Formation (Ckp) and Middle Permian Gerik formation (Pgk). The oldest known rock unit is the

Carboniferous Tiang schist that is believed to be contemporaneous in age with the Kubang

Pasu Formation, which is widely exposed in southeastern part of the Transect area. It consists

of purplish grey, medium- to thick-bedded, medium-grained quartz-mica schist, quartz-mica-

chiastolite schist, amphibolites schist, silimanite gneiss and hornfels. The succession is

strongly deformed and metamorphosed due to the Main Range Granite intrusion as well as

tectonic activity along the Bentong-Raub Suture Zone that lies within this rock unit.

The Kubang Pasu Formation (Ckp) comprises essentially thick interbeds of psammitic

and subordinate pelitic rocks. The psammitic rock is composed of thick-bedded

metasandstones i.e., quartzite with minor metagreywacke interbedded with subordinate

metasiltstone. The pelitic rock consists of fine-grained quartz-mica schist, quartz-mica-

chiastolite schist and hornfels. Lithologically, the Kubang Pasu Formation in the Transect

area is slightly different from the succession exposed in the Pengkalan Hulu-Betong Transect

area due to the differences in degree of metamorphism. Fossils have not yet been found in

this rock unit in the Transect area. The rocks are commonly metamorphosed to

metasandstone, hornfels and fine-grained schist due to the Main Range Granite intrusion.

The Carboniferous-Permian Mangga formation (CPmg), located at the western margin of

the Bentong-Raub Suture Zone, overlies conformably the Carboniferous Tiang schist. It

comprises low- to medium-grade metamorphic sequences of psammitic, pelitic and

pyroclastic as well as schistose rocks.

Generally, the Permian Gerik formation (Pgk) overlies conformably the Carboniferous

Kubang Pasu Formation. However, a fault contact can be seen in the Transect area as a result

of uplifting of Carboniferous succession due to granite intrusion. The Gerik formation

consists of pyroclastic rocks, mainly tuffs of rhyolitic to rhyodacitic composition with

limestone and calcareous shale lenses, tuffaceous sandstone as well as chert and siliceous

shale that occur sporadically. The age of the Gerik formation is not older than Permian as

indicated by the presence of Phillipsia, Anisopyge (trilobite) and Chonetid (brachiopod)

within the calcareous shale at Kampung Batu 2, Gerik (Malaysian-Thai Working Group,

2010). Radiolarian bearing pelagic sediments crops out at Km 18.6 of the East-West

Highway and at an exposure (N 5o

31‟ 38”, E 101o 17‟38”) at the old stretch of the highway.

The samples yield Follicucullus sp., Gustefana sp., Latentifistula sp., Triplanospongos sp.

and Albaillella sp. Some radiolarian specimens resemble Follicucullus scholasticus and

Albaillella levis which are important faunas. The age of these fauna is interpreted as

Capitanian to Changhsingian stage of Middle to Late Permian (Saesaengseerung, pers.

comm.).

Quaternary alluvial deposits of appreciable extent and thickness are present along the

valley of the Sungai Perak, Sungai Pergau and their larger tributaries. The Recent deposits

have been accumulated through fluviatile accretion in the flood plains of the rivers.

Generalised succession of the rock units on the Malaysian side of the Transect area is

summarised in Figure 12.

16

Figure 12: Generalised geologic sequence of the Belum-Hala Transect area (Malaysian side).

17

3.0 LITHOSTRATIGRAPHY

The Transect area is covered by the Silurian-Devonian Betong Formation (SDbt),

Carboniferous Tiang schist (Cts), Carboniferous Kubang Pasu/Yaha Formation (Ckp/yh),

Carboniferous-Permian Mangga formation (CPmg) and Permian Gerik formation (Pgk). The

Betong Formation is only exposed on the Thai side, whereas the Mangga formation and the

Gerik formation are only exposed on the Malaysian side.

Schematic lithostratigraphic correlation for the Transect area is shown in Figure 13.

Geological map of the Transect area is included in the back pocket.

Figure 13: Schematic lithostratigraphic correlation for the Transect area.

3.1 Sedimentary and metamorphic rocks

3.1.1 The Betong Formation (SDbt1 and SDbt2)

The rock unit, exposed only on the Thai side, is well distributed as N-S trending, long

narrow, low relief terrain along the Hala River in the west-central part of the Transect area.

The Betong Formation is in contact with the granite (units G3, G2, and G1) to the east, north,

west and south. In some places, it forms the large roof pendant above the granite on the top of

mountainous terrains. Bodies of small roof pendant are also exposed near the low-lying

terrains in the western part of the Transect area near the Malaysia-Thailand border. Both units

SEDIMENTARY AND METASEDIMENTARY ROCKS

ERA

Kubang Pasu

Fm.(Ckpag)Yaha Fm.(Cyh2)

Kubang Pasu

Fm.(Ckpar)Yaha Fm.(Cyh1)

IGNEOUS ROCKS

Hala granite(Trgrhl)

CARBONIFEROUS

PERIOD/EPOCH

Singor granite (Trgrsg)

CARBONIFEROUS-

PERMIAN

Beto

ng

Form

ation (

SD

bt)

Singor granite (Trgrsg)

Tiang

schist(Cts)

Kubang P

asu

Form

ation(C

kp)

Mangga formation(CPmgar)

Merah Granite (Trgrmr)

Kabut granite (Trgrkt)

Tiang

schist(Cts)

Gerik

form

ation(P

gk)

Chantarat (Trgrch)

Budo Granite (Trgrbd)

Kabut granite (Trgrkt)

Chantarat Granite (Trgrch)

Merah Granite/Budo Granite (Trgrmr/bd)

Beto

ng

Form

ation (

SD

bt)

SILURIAN-DEVONIAN

Yaha F

orm

ation(C

yh)

Pyroclastic facies(Pgkpy)

Arenaceous facies(Pgkar)

MALAYSIA

Betong Formation(SDbt2)

Betong Formation(SDbt1)

Tiang schist(Cts)

ROCK UNITS

Gerik

form

ation(P

gk)

Argillaceous facies(Pgkag)

Arenaceous facies(Pgkar)

Pyroclastic facies(Pgkpy)

AGE/COUNTRY

MALAYSIA/THAILANDTHAILAND

PERMIAN

Argillaceous facies(Pgkag)

Betong Formation(SDbt2)

Betong Formation(SDbt1)

PA

LA

EO

ZO

IC

Hala granite(Trgrhl)

TRIASSIC

ME

SO

ZO

IC

Mangga formation(CPmgar)

Kubang Pasu/Yaha

Formation (Ckp/yh)

Kabut granite (Trgrkt)

18

can be correlated to the metamorphic rocks of the Silurian-Devonian Betong Formation

(SDbt) and Kroh Formation (SDkr) on the Malaysian side in the Pengkalan Hulu-Betong

Transect area. The term Betong Formation (SDbt) was proposed by Muenlek et al. (1979) to

describe a sequence of fossiliferous sedimentary rocks of Silurian-Devonian age in the Yala-

Betong area. The formation is named after the Betong District, where good outcrops are well

exposed on road-cuts. It is the oldest lithostratigraphic unit exposed in the Transect area

(Malaysian-Thai Working Group, 2006).

In the Pengkalan Hulu-Betong Transect area, fossil assemblages, i.e. Tentaculites

elegans and Tentaculites sp. occur in light pink shale strata and limestone lenses. Conodont

assemblage found in chert beds indicates the age of rock sequence is Devonian. However, the

discovery of graptolite in light pink shale leads to the possible age of the succession is

Silurian-Devonian. Therefore, the succession of the Betong Formation (SDbt) can be dated as

Silurian-Devonian age.

3.1.2 Tiang schist (Cts)

On the Malaysian side, the term Tiang schist had been introduced by Mohamad Hussein

et al. (in manuscript) to describe a sequence of metamorphic rocks cropping out on the east of

the Main Range Granite and to the west of the Bentong-Raub Suture Zone in the Belum and

Batu Melintang areas. It is named after Sungai Tiang in the central part of the Transect area

where good outcrops can be observed.

On the Malaysian side, based on remote sensing interpretation, the Tiang schist is named

as S4 Unit.

S4 Unit

This unit is interpreted as quartz-mica schist that could be correlated with the Tiang

schist. The S4 unit is distributed in the eastern part of the Transect area from the north at

Malaysia-Thailand border (Bt. Luat Lantai) to the south of the Transect area.

The remote sensing characteristic of this unit is very high to high topography (mountain

landform) with main ridges orientation in NS direction. The main ridges are curve, convex,

round and branches irregularly. The branch ridges are angular to the main ridges. It has

dendritic drainage pattern with coarse texture. V-shape valley/gully occurs between the

ridges. It has dark grey photo tone, dense vegetation and forest cover. Part of the unit shows

dome structure like granite intrusion. Based on the field observation, the lithology of the area

is quartz-mica schist, amphibolite schist and silimanite gneiss.

On the Thai side, the S1 unit referred to the S5 Unit from photo characteristic is

interpreted as Schist, Phylite, Shale and sandstone. This unit is distributed as two N-S

trending, low-relief elongated terrains on the Thai side and close to the Malaysia-Thailand

border. The unit boundary can be correlated to the Cts unit on the Malaysian side. Some parts

of this unit are intruded by Triassic granite showing the circular feature. The lithology is

composed of quartz-mica schist, quartz-graphite schist, quartz-mica garnet schist, and quartz-

19

mica-chiastolite schist. Amphibolite schist occurs locally. This unit can be correlated to Tiang

Schist/Ban Sa formation.

Ban Sa formation is correlate to Tiang Schist in Malaysia side. The term Tiang schist

was introduced by Mohamad Hussein et al. (in manuscript) to describe a sequence of

metamorphic rocks out cropping in the east of the Main Range Granite in the Belum area. It

is named after the Sungai Tiang River where good outcrops can be observed. The term Ban

Sa formation is proposed during the joint Malaysia-Thailand geological survey project to

describe the high-grade metamorphic rocks on the Thai side of the Batu Melintang-Sungai

Kolok Transect area (Malaysian-Thai Working Group, 2006). It is named after the Ban Sa

village, near the Mae Nam Kolok (Kolok River) where good outcrops are exposed.

Distribution

The Tiang schist occupies a north-south trending belt whose western margin is in contact

with the eastern margin of the Main Range Granite. It extends northeastwardly into the Batu

Melintang-Sungai Kolok Transect area, northwardly into Thailand and southwardly into the

Temengor area. The rock unit is highly faulted throughout the area; therefore it is difficult to

estimate its thickness (Mohamad Hussein et al., in manuscript).

In the Belum-Hala Transect area, this unit is distributed as two N-S trending, low-relief

elongated terrains on the Thai side at the boundary pillar No. 60, Khlong Kue Sa, close to the

Malaysia-Thailand border. The unit boundary can be correlated to the SDts unit on the

Malaysian side. Some parts of this unit are intruded by Triassic granite showing the circular

feature.

Lithology

The Tiang schist (Cts) consists of purplish grey to dark grey quartz-mica schist, quartz

schist, quartz-mica-graphite schist and quartz-mica-garnet schist with minor hornfels. The

quartz-mica schist is strongly schistosed, well foliated, consisting essentially of medium-

grained elongated quartz and mica, commonly muscovite with chlorite (Figures 14 & 15).

Hornblende, calcite, diopsite and pyrite occur as accessory minerals. Although biotite is

predominant, muscovite is fairly common. Lenses of amphibolite schist comprising quartz-

actinolite-tremolite schist and quartz-mica-hornblende schist occur at several localities along

Sungai Tiang. Rohayu (1994) reported the occurrences of sillimanite gneiss at the higher

terrain along the East-West Highway in the Transect area. The presence of quartz-mica-

chiastolite schist at Sungai Palai and Sungai Dadek, and quartz-mica-garnet schist (Figure 15)

at upper reaches of Sungai Machang indicates that it might be the result of both contact and

regional metamorphisms. Although granite is not exposed in the surrounding area of quartz-

mica-chiastolite schist and quartz-mica-garnet schist, it is believed that granite is sub-

cropping below the metamorphic rocks. Hornfels and hornfelsic rocks occur in the vicinity of

the granite body.

Tiang Schist (Cts) on the Malaysian side of the Transect area consists of quartz schist and

quartz-mica schist. The quartz-mica schist is typically strongly schistosed, well-foliated,

20

consisting essentially of quartz and mica (most commonly muscovite). Chlorite, calcite and

pyrite have also been recorded in the schist. Although muscovite is predominant, biotite is

fairly common. Lenses of amphibolite schist comprising of quartz-actinolite-tremolite schist

and quartz-hornblende schist occur at several localities along the Sungai Tiang. Rohayu

(1994) reported that sillimanite gneiss has been found in the higher terrain along the East-

West Highway in the Belum area, 10 km southwest of the Transect area. The presence of

quartz-mica-chiastolite schist indicates that it might be the result of both contact and regional

metamorphisms. Although granite is not exposed in the surrounding area of quartz-mica-

chiastolite schist, it is believed that the granite is sub-cropping below the metamorphic rocks.

According to the geology of the Batu Melintang-Sungai Kolok Transect area on the Thai

side, the Tiang schist/Ban Sa formation along the Mae Nam Kolok at Ban Sa and road-cut

succession at Ban Ba La consists mainly of thin- to thick-bedded, light grey, biotite-augen

gneiss (40-90%) intercalated with grey banded schistose biotite gneiss (10-60%). Augen

biotite gneiss has well-developed gneissocity, 1 cm per band. It has 40-50% phenocrysts in

volume. Phenocrysts are composed mainly of K-feldspar, porphyroblastic texture and are 0.5-

1X 2-4 cm in size. Groundmass is medium- to coarse-grained and shows well-developed

gneissic texture. Mineral composition consists of sheared quartz (30%), feldspar (40%) and

platy biotite (40%). The schistose biotite-gneiss outcrop at Ban Sa has a similar lithology to

the augen gneiss having fewer phenocryst than the former but has more mica. Quartz-

amphibolite schist has similar texture with the Ban Sa outcrop but has more silica and

probably calcareous composition. Thinly banded, dark brown biotite, hornblende and

actinolite are usually common.

The succession is strongly deformed and metamorphosed as a result of the intrusion by

the Main Range Granite as well as affected by the tectonic activity in the Betong-Raub Suture

Zone along its eastern margin. The rocks trend N-S, with the foliation dip gently to steeply

both eastwards and westwards, resulting from intensive folding and faulting. The rock

displays well developed N-S and NNE-SSW trending cleavages.

21

Figure 14: Outcrop of the Tiang schist at Km 66.1

of the East-West Highway.

Figure 15: Close-up view of the Tiang schist.

Figure 16: Exposures of quartz-mica-garnet schist at 5o 45‟ N, 101

o 38‟ E, upper reaches of Sungai Machang.

Age and correlation

No fossil assemblage is recorded and the thickness of the succession is indeterminable.

Previously, this rock unit was interpretated as Silurian-Devonian in age. However, owing to

the fact that the Tiang schist is conformably overlain by the Carboniferous-Permian Mangga

formation, therefore it is interpreted that possibly Carboniferous age. In addition, Metcalfe

(2000) discovered an Upper Devonian to Upper Permian radiolarian in some of collected

chert samples along the Bentong-Raub Suture Zone to the south of the Transect area, which‟s

also in contact with the eastern margin of the Main Range Granite. The Tiang schist is

located at the same geological setting and geographical belt with the other Upper Palaeozoic

rocks unit. Furthermore, the origin of the rock may be is same sequence with the

Carboniferous Kubang Pasu that expose at the west side of the Transect area but just

separated by the Main Range Granite intrusion, therefore it is believed that they are might be

of the same age. The different of lithology is due to the degree of metamorphism.

Lithologically, the schist interpreted as thick-bedded to massive arenaceous origin indicates

very stable and consistent environment during the Carboniferous. Structurally, Tiang schist

22

shows gently dipping which can be observed at Km 66.1 of the East-West Highway (Figure

8), so that it might be younger than Silurian-Devonian that expected before. Hence, the

succession of the Tiang schist can be dated as probably Carboniferous age.

3.1.3 Kubang Pasu/Yaha Formation (Cyh)

The Kubang Pasu Formation is conformably overlain by the Permian Gerik formation.

However, within the Transect area, it is interpreted as fault contact with strike NW-SE.

Originally, the term Kubang Pasu Formation was introduced by Jones (1981) for a sequence

of thick sandstone and thin shale in the Kedah and Perlis areas in northwest Peninsular

Malaysia. The stratigraphic name was taken after the Kubang Pasu District, Kedah where the

good outcrops of this rock unit can be observed. Lithologically, the Kubang Pasu Formation

in the Transect area is different from that exposed in Kedah and Perlis due to metamorphism.

The rocks in this area are locally metamorphosed to metasandstone, hornfels, phyllite and

schist.

On the Malaysian side, based on remote sensing interpretation, the Carboniferous

Kubang Pasu/Yaha Formation can be divided into S1, S2 and S3 units as described below:

S1 Unit

The unit is interpreted to be schist and metasandstone which can be correlated to the

arenaceous facies within the Carboniferous Kubang Pasu/Yaha Formation at Pengkalan Hulu-

Betong Transect area. The S1 unit is distributed in the northwest of the Transect area at

Malaysia-Thailand border in Ulu Titi Basah (5,030 m) and Gunung Angus (4,642 m)

mountainous terrain.

The remote sensing characteristic of this unit is very high topography (mountain

landform) and NS orientation. The main ridges are curve and linear, concave, sharp and

branches irregularly. The branch ridges are angular to the main ridge. It has dendritic

drainage pattern with fine to coarse texture. V-shape valley and gully occurs between the

ridges. It has grey to dark grey photo tone, dense vegetation and forest cover. Part of the unit

shows bedding plane with N-S strike and dipping gently to the east.

Based on the field observation, the lithology of the area are grey to greenish grey quartz-mica

schist and yellowish grey massive metaquartzarenite and minor of reddish mudstone and

siltstone.

S2 Unit

The unit is interpreted to be quartz-mica schist, metasandstone and metaconglomerate

which can be correlated to the arenaceous facies within the Carboniferous Kubang Pasu/Yaha

Formation at Pengkalan Hulu-Betong Transect area. The S2 unit is distributed in the

northwest of the Transect area near Malaysia-Thailand border.

The remote sensing characteristic of this unit is high topography having the N-S

direction. The main ridge is curve, irregular, convex, sharp and has more ridges branches.

23

The branch ridges are perpendicular and angular to the main ridge. It exhibits dendritic and

trellis drainage patterns with fine to coarse texture. More V-shape valley/gully occurs

between the ridges. It has light grey to grey photo tone covered with dense forest.

Based on field observation, the lithology of the area is grey to greenish grey quartz-mica

schist, light grey to grey metasandstone grading up to metaconglomerate. This meta-

conglomerate was interpreted as the upper part of this unit.

S3 Unit

This unit is interpreted to be arenaceous rock which can be correlated to the arenaceous

facies within the Carboniferous Kubang Pasu/Yaha Formation at Pengkalan Hulu-Betong

Transects area. The S3 unit is distributed in the central part of the Transect area.

The remote sensing characteristic of this unit is moderate high relief topography having

the N-S direction. The main ridge has curve, convex and sharp characteristics with irregular

branches pattern. These branches are angular and perpendicular to the main ridge. It exhibits

dendritic and trellis drainage pattern with fine texture. More V-shape gully occurs between

the ridges. It has light grey photo tone covered with dense forest. Based on the field

observation, the lithology of the area is quartz-mica schist.

On the Thai side, the Yaha Formation (Cyh) is conformably underlain by the Betong

Formation. The term Yaha was introduced by Nakapadungrat et al. (1988) to describe a

sequence of thick Carboniferous clastic rocks in the Sadao-Yala area. It is named after Yaha

District, where geological information was firstly studied and good outcrops are prevailed.

This unit can be correlated with the Kubang Pasu/Yaha Formation.

Distribution

In Malaysia, the Kubang Pasu Formation (Ckp) is well exposed in the western part of the

Transect area, covering the Sungai Kenarong valley. The rock exposures can be observed

along the streams of Sungai Kenarong which located in the remote and forested area. The

only access to that area is by boat via Temengor Lake, and then proceeds to continue the

traverse by foot. Metasandstone and metaconglomerate occurs in the river mouth of the

Sungai Tan Hain in the northern part of the Temengor Lake. The succession also occurs as

roof pendant within the Main Range Granite.

The Yaha Formation (Cyh) is well distributed in the western part of the Belum-Hala

Transect area. In the Transect area, the Yaha Formation can be subdivided into two facies,

namely, the argillaceous facies (Cyh1) of the Yaha Formation (Cyh) or the lower part, and the

arenaceous facies (Cyh2) of the Yaha Formation (Cyh) or the upper part of the complete

sequence.

24

Lithology

The whole succession of the Kubang Pasu Formation (Ckp) in the Transect area is

metamorphosed. Granite intrusion in the country rocks can be observed along Sungai Terosak

and its tributaries where the rocks are metamorphosed to phyllite, schist, hornfels,

metasiltstone and metasandstone.

In the Betong-Than To area, a complete sequence of the Yaha Formation (Cyh) is

characterized by the presence of sandstone, siltstone, shale and ribbon chert with subordinate

limestone lenses. The total thickness of this Carboniferous rock from the representative

section exceeds 800 m.

The succession consists of (in ascending order) thick sequence of pelitic rock comprising

hornfels, phyllite and schist intercalated with light grey, thick-bedded to massive, fine-

grained, well-sorted and graded metasandstone or metaquartzarenite and minor metasiltstones

overlain by metaconglomerate, grey, medium-grained grit and poorly sorted, graded and

cross bedded metasandstones.

The pelitic rocks consist of phyllite, schist, hornfels and a minor variety of thin-bedded,

poorly sorted pelitic-psammitic rocks of metamudstone, metasiltstone and metagreywacke.

The phyllite and schist consist of very fine- to fine-grained, elongated quartz grains with

bands of sericite, chlorite, muscovite, biotite and iron oxide. Hornblende presents as

accessory mineral. The phyllite is commonly laminated with the lamination parallel to the

original bedding plane and occasionally shows wavy cleavage. Schistosity in the schist is

made up of segregation of muscovite and biotite and other flaky and columnar minerals such

as hornblende as well as secondary minerals such as sericite and chlorite. Metasiltstone and

metagreywacke generally less than a few centimetres thick, occur commonly as interbeds and

intercalations within the phyllite or schist sequences. The presence of quartz-mica-chiastolite

schist at the right tributary of Sungai Kenarong indicates that it might be the result of both

contact and regional metamorphisms. Although granite is not exposed in the surrounding area

of quartz-mica-chiastolite schist, it is believed that granite is sub-cropping below the

metamorphic rocks.

On the Thai side, the S4 Unit referred to some parts of the S3 Unit, is interpreted to be

well-bedded sandstone and shale which can be correlated to argillaceous facies (western part

of S3) within the Carboniferous Kubang Pasu/Yaha Formation (Ckpag/yh) in the Pengkalan

Hulu-Betong Transect area. The unit is distributed in the western part of the Belum-Hala

Transect area (the Hun Kut mountainous terrain) close to the Malaysia-Thailand border. It

shows the wide patches of roof pendants on granite with distinct N-S bedding traces.

In the Transect area, the argillaceous facies of the Yaha Formation (Cyh) is well exposed

in the low relief terrain, near the eastern granite pluton in the western part of the area and

extends to the northwestern part of the Malaysian side.

The argillaceous rocks in the lower part (Cyh1) of the Yaha Formation (Cyh) are affected

by local deformation and low-grade metamorphism (or superimposed) in the shear and

contact zones. The rocks are metamorphosed to be thin- to medium-banded phyllite, phyllitic

25

schist, mica schist and quartz-schist with minor quartzite and calc-silicate. The thickness of

this unit is inconclusive due to strong folding.

The psammitic rocks of the Kubang Pasu Formation are made up of thick sequence of

thick-bedded to massive metasandstone, predominantly quartzite (metaquartzarenite) and

minor pelitic rocks such as metasiltstone. At the Gunung Hulu Titi Basah, in the vicinity of

Malaysia-Thailand border, the succession is composed predominantly of light grey- to

yellowish grey, fine- to medium-grained metaquartzarenite containing more than 95% quartz

grains. The rests are muscovite with minor tourmaline, feldspar and iron oxide. Thin

interbeds of metasiltstone occasionally occur within the metasandstone.

The Arenaceous facies (Cyh2) of the Yaha Formation (Cyh) are restricted as roof pendants

on granite in the mountainous area close to the boundary pillar No. 56 B. The unit is

distributed in the western part of the Belum-Hala Transect area (the Hun Kut mountainous

terrain) close to the Malaysia-Thailand border. It shows the wide patches of roof pendant on

granite with distinct N-S bedding traces. It is characterized by the presence of medium- to

thick-bedded sandstone, quartzite and minor argillite with indeterminable thickness.

The younger parts of the succession are composed of greywacke and subgreywacke. The

grains are poorly sorted and more often grading up from pebbly sandstone or grit to

conglomerate. The metaconglomerate exposures are limited within the vicinity of the river

mouth of Sungai Tan Hain (05o 44.884‟ N, 101

o23.389‟ E), in the northern part of the

Temengor Lake area (Figure 17). The metaconglomerates, grey to yellowish grey when

weathered, have medium- to thick-bedded (0.5-1.5 m thick) and coarsening upward sequence.

Their texture comprises 20% - 30% clasts of subangular to angular, low sphericity and poorly

sorted, various sizes from pebble to cobble; 1 to 5 cm in diameter of smoky, pinkish to white

vein quartz (95%) (Figure 18), and the rest is light grey sandstones, dark grey siltstone and

grey chert (5%) with occasional large mudstone clasts (Figure 19). Orientation of clasts

commonly follows the current direction. Matrix of rocks is fine- to medium-grained poorly

sorted grey dirty sandstones exhibiting well-developed graded and cross bedding. In places,

cross-bedding can be observed on the top part of the sandstone beds that graded to the

conglomerate (Figure 20).

The rocks cleavage strikes N-S and NNW-SSE, generally dipping both eastward and

westward. The total thickness of the Carboniferous rocks from the representative section is

more than 800 m.

26

Figure 17: The metaconglomerate exposures are

limited within the vicinity of river mouth

of Sungai Tan Hain (05o 44.884‟ N,

101o23.389‟ E)

Figure 18: Various size of quartz clasts within the

conglomerate.

Figure 19: Dark grey mudstone clasts that is up to 5

cm in diameter.

Figure 20: Cross-bedding observed on the top part of

the sandstone beds grading from the

conglomerate.

Age and Correlation

No fossil assemblage is recorded within the rocks unit in the Transect area. The

psammitic rock shows similar characteristics where thick-bedded to massive sandstone or

metasandstone indicates very stable and consistent environment during the Carboniferous. It

is correlatable with the Kubang Pasu Formation exposed in the Kubang Pasu area. The

difference is just due to the degree of metamorphism; however they are expected to be of the

same genesis. Furthermore, this rock unit is exposed at the upper reaches of Sungai

Kenarong, in the vicinity of Malaysia-Thailand border, just 6 km to the southeast of Ban Tai

Tong in Yala Province, Thailand where Carboniferous microfossils were found.

27

Depositional Environment

The sandstone is intercalated with the thick to very thick sequence of pelitic rocks,

followed by very thick sequence of thick-bedded to massive, well-sorted quartzitic

metasandstone with graded bedding and cross lamination. The rocks are interpreted to

represent a near shore environment of deposition, probably in either intertidal or upper

subtidal zones. The poorly sorted metaconglomerate is interpreted as reworked conglomerate

previously deposited in the shelf environment and then redeposited in the deeper

environment together with the arenaceous and argillaceous materials.

3.1.4 Mangga formation (CPmg)

The term Mangga formation was introduced by Mohamad Hussein et al. (in manuscript)

to describe the low- to medium-grade metamorphic sequences of psammitic, pellitic,

pyroclastic, hornfels and marble as well as schistose rocks in the eastern part of the Transect

area. It is named after the Sungai Mangga where this rock unit was first mapped and good

outcrops had been recorded. The formation exposed only on the Malaysian side. The Mangga

formation (CPmg), which is strongly deformed and metamorphosed, trends N-S and dips

moderately to steeply either westward or eastwardly.

On the Thai side, the unit S5 is pointed to some parts of the S5 unit which interpreted

from photo characteristics as shale and sandstone. The unit can be correlated with the

arenaceous facies of the Carboniferous-Permain Mangga formation/Ka Lu Bi formation

(CPmgkl) which comprises metasandstone, metagreywacke, tuffaceous sandstone, quartzite

and conglomerate. This unit extends as elongated N-S trending ridge in the eastern part of the

Transect area.

The S6 unit is referred to some parts of the S5 unit. From the photo characteristics this

unit is interpreted as shale and sandstone (S5 Unit). It is correlatable with the Carboniferous-

Permian Mangga formation/Ka Lu Bi formation (CPmgkl) on the Malaysian side. The Unit S6

is well exposed continuously along the elongated N-S trending ridge in the eastern part of the

Transect area. Some parts of this unit are intruded by the Cretaceous To Mo granite (Kgrtm)

and exhibit the aureole complex and circular feature.

The eastern margin of the Mangga formation is situated within the Bentong-Raub Suture

Zone. Structurally, the rocks within the suture zone are highly deformed due to the tectonic

activities during the collision of the Sibumasu and Indochina terranes.

Distribution

The Mangga formation (CPmg) is confined to the Sungai Mangga, located in the

southeastern part of the Transect area. It extends eastwardly into the Batu Melintang-Sungai

Kolok Transect area where the equivalent Ai Ka Po formation (CPak) and Ka Lu Bi formation

(CPkl) can be observed. The thickness of the succession is indeterminable due to its strongly

deformed nature.

28

Lithology

According to the Malaysian-Thai Working Group (2006), the Mangga formation/Ai Ka

Po formation/Ka Lu Bi formation (CPmg/ak and CPmg/kl) in the Batu Melintang-Sungai Kolok

Transect area, on the Malaysian side is represented by a low grade metamorphic sequence

that can be subdivided into four facies, namely, argillaceous (CPmgag), arenaceous (CPmgar),

pyroclastic (CPmgpy), and calcareous (CPmgcl) rocks. The argillaceous unit consists mainly of

metamorphosed siliceous shale, slate, phyllite, metasiltstone and hornfels. There are two

strata of argilliceous facies representative of the lower and upper parts of this formation. The

upper part consists of hornfelsic rocks such as calc-silicate hornfels. The best outcrop of

hornfels is located near the junction to Felda Tumbi Rapat. The rocks are light grey in colour,

very fine-grained, slightly foliated and recrystallized with both quartz and calcite veinlets.

Petrographically, the main minerals are quartz with minor muscovite, biotite, diopsite and

iron oxide. The chert is light grey to grey with some impure cherts forming ribbon cherts.

Only arenaceous facies is exposed in the Transect area. The arenaceous facies consists of

yellowish grey, light grey, thin- to medium-bedded, fine- to medium-grained metasandstone

and metagreywacke interbedded with minor metasiltstone. Due to deep weathering, no

suitable photograph of the outcrops exposed in the Transect area can be shown in this report.

Photographs of the arenaceous facies which is exposed in the Batu Melintang-Sungai Kolok

Transect area at Km 173.2 of the East-West Highway, about 2 km to the east of the Transect

area are selected as examples shown in Figures 21 and 22.

Figure 21: Exposures of the psammitic unit of the

Mangga formation near TM

Communication Tower at Km 173.2 of

the East-West Highway.

Figure 22: Close up view of the psammitic

unit of the Mangga formation near

TM Communication Tower at Km

173.2 of the East-West Highway.

Age and correlation

MacDonald (1955) reported on the occurrences of the poorly preserved fossils of

Palaeojera sp., brachiopod of Costiferina sp. and gastropod in the Mangga formation at

Kampung Belimbing, in the Batu Melintang area indicative of Permian age.

29

During the Malaysia-Thailand Working Group joint field check in March 2010, several

chert and siliceous shale samples were collected near the TM telecomunication tower at Km

173.2 of the East-West Highway (N 05o 35.883‟, E 101

o 36.002‟), 2 km to the east of the

Transect area. Radiolarians extracted from the chert and siliceous shale were poorly

preserved. However, the radiolarian can be identified as Follicuculus sp. and others, quite

similar with that found in the Gerik Formation at Km 18.6 of the East-West Highway, Upper

Perak. These fossils suggest that the age of the rock unit is possibly of Capitanian to

Wuchiapingian (Middle to Late Permian). However, based on lithological and stratigraphical

correlations, the age of the succession was assigned as Carboniferous-Permian (Malaysian

and Thailand Working Groups, 2010).

3.1.5 Gerik formation (Pgk)

The term Gerik formation was informally proposed to replace the term Grik tuff

introduced by Burton (1970, 1972, 1986) for the pyroclastic rocks consisting mainly of tuffs

of rhyolitic to rhyodacitic composition (The Malaysia-Thailand Working Group, 2010).

Limestone and calcareous shale lenses occur sporadically. The name of this formation is

taken after the Gerik town situated 10 km to the southwest of the Transect‟s area boundary.

The occurrence of interbedded tuff, limestone and fossiliferous calcareous shale on a road-

cut at Kampung Batu 2, Gerik indicates a Permian age for the formation. The tuffs of the

Gerik formation are occasionally metamorphosed (The Malaysia-Thailand Working Group,

2010).

In the Transect area, the tuff is underlain by the thick beds of fine-grained tuffaceous

sandstone. There are several small lenses of marble in the tuff at the river mouth of Sungai

Gadong (05o 36.759‟ N, 101

o 18.997‟ E) in northwestern part of the Temengor Lake. It is

also well exposed at Bukit Tali Kail, Temengor Lake, just 1 km outside of Transect‟s south

boundary. Lithologically, the sandstone resembles the Carboniferous Kubang Pasu

Formation‟s sandstone, but structurally, the sandstone lies on top of the tuff beds. Therefore

it is interpreted as belonging to the Permian Gerik formation. On the Malaysian side, based

on remote sensing interpretation, the Gerik Formation can be divided into six units, named as

V1 to V6 as described below:

V1 Unit

The unit is interpreted to be schistose tuff of the Gerik Formation. The V1 unit is

distributed in the south central part of the Transect area which is in contact with the Main

Range Granite. The remote sensing characteristic of this unit is moderate high relief

topography; parallel ridges and unit orientation are in nearly NS direction. Main ridge has

sharp characteristic, curve, convex and branches parallel/irregularly. The ridges branch not

too sharp and perpendicular/angular to the main ridge. The unit has trellis and dendritic

drainage pattern with moderate texture and many V-shape gullies. It has grey photo tone,

dense vegetation and forest/disturbed forest landuse. The rock is of greenish grey to dark

grey of quartz-mica schist.

30

V2 Unit

The unit is interpreted to be phyllitic tuff of the Gerik Formation. The V2 unit is

distributed in the south central part of the Transect area. The remote sensing characteristic of

this unit is low relief topography (hilly landform). Main ridges, oriented nearly N-S direction,

have not too sharp characteristic, curve, concave and many parallel branches. The branches

are perpendicular to the main ridge. The unit has trellis drainage pattern with fine texture and

V-shape gully. It has grey photo tone and dense forest. The rock is laminated to thin beds of

grey to greenish grey metatuff of rhyolitic composition.

V3 Unit

The unit is interpreted to be slaty tuff of the Gerik Formation. The V3 unit is distributed

in the southwestern part of the Transect area. The remote sensing characteristic of this unit is

moderate high relief topography (hilly landform Main ridges, oriented nearly N-S direction,

have not too sharp characteristic, curve, concave and many parallel branches. The branches

are pendicular to the main ridge. The unit has trellis drainage pattern with moderate texture

and V-shape gully. It has grey photo tone and dense forest. The rock is laminated to thin beds

of grey to greenish grey metatuff of rhyolitic composition.

V4 Unit

The unit is interpreted to be tuffaceous sandstone of the Gerik Formation. The V4 unit is

distributed in the southwestern part of the Transect area to the west of Temengor Lake. This

rock unit forms the Gunung Pilong (2344 m) and Gunung Tenok (1970 m).

The remote sensing characteristic of this unit is high to moderately high relief

topography with many main ridges in various, especially in the N-S direction, concave, not

too sharp, and curved. The branch ridges are angular to the main ridge. The unit has dendritic

and trellis drainage pattern with fine to moderate texture and V-shape gully between branch

ridges. It exhibits grey photo tone of dense vegetation. Part of the unit shows circular features

like volcanic cone. The rock is high grey to high yellowish grey of thin to thick beds of fined

grained tuffaceous sandstone.

V5 Unit

The unit is interpreted to be metatuf of Gerik Formation. The V1 unit is distributed in

the west of the Transect area near Malaysia-Thailand border in Gunung Guak Rimau (3713)

and Gunung Daungsang (3598) mountainous terrain. The remote sensing characteristic of

this unit is high relief topography (mountain landform). Main ridge and unit orientation are in

NS direction. Main ridge has sharp characteristic, curve, convex and branches irregularly.

The ridges branch angular to the main ridge. The unit has dendritic drainage pattern with

coarse/ moderate texture and V-shape gully. It has light grey photo tone, dense vegetation

and forest landuse. Part of the unit shows circular features like volcanic cone. Based on the

field observation, the lithology of the area is metatuff.

31

V6 Unit

The unit is interpreted to be tuffaceous shale and minor chert of the Gerik Formation.

The V6 unit is distributed in the southwestern part of the Transect area near the Malaysia-

Thailand border. The remote sensing characteristic of this unit is low relief topography

(narrow hilly landform). It has a N-S main ridge with sharp characteristic, curve, concave.

The branches are perpendicular to the main ridge. The unit has trellis drainage pattern with

fine/moderate texture and V-shape gully between the branches. It has light grey photo tone

and dense vegetation. Based on field observation, the lithology of the area is tuffaceous shale

and minor chert.

Distribution

The Gerik formation is widely exposed in the western part of the Transect area on the

Malaysian side but not exposed on the Thai side. It is fairly well exposed in the vicinity of

the Gerik town and Lawin area. This rock unit also crops out in the Temengor Dam site‟s

area. In the Transect area, the rock exposures can be observed along the East-West Highway

especially around the Banding Island area. The Gerik formation is also exposed in the

Kerunai area to the southwest of the Transect area. The eastern margin trends northward

from Temengor Dam area passing the East-West Highway and then Sungai Chachor to the

Main Range Granite mass at river mouth of Sungai Kejar in the central part of the Transect

area. Some good metasandstone outcrops can be observed at the river mouth of Sungai Ta

Eng.

Lithology

The Gerik formation consists of pyroclastic, calcareous, arenaceous and argillaceous

facieses. The pyroclastic facies consists mainly of tuffs of rhyolitic to rhyodacitic

composition. Interbeds of tuffs, limestone and calcareous shale also occur. These tuffaceous

rocks also contain variable amounts of clastic sediments of sandstone, limestone and lenses

of calcareous shale. In places, foliation can be seen in the groundmass of the tuffs as a result

of regional metamorphism. The most altered rocks show clearer schistose texture (Figures 23

& 24). Burton (1986) reported that no lava flows were recognised when he studied the Gerk

tuff. However a weak flow structure shown by the alignment of prismatic K-feldspar

phenocrysts was observed at a road-cut near the Kuala Rui Police station, to the west of

Gerik township in the Pengkalan Hulu-Betong Transect area. The flow direction is towards

330o (The Malaysia-Thailand Working Group, 2010).

The arenaceous facies comprises of tuffaceous sandstone and sandstone. The rock is

fine-grained and light grey to grey in colour. The tuffaceous sandstone can be observed along

the East-West Highway (Figures 25 & 26). This N-S trending formation which dips steeply

eastwards and westwards consists of greenish grey to light grey, thick-bedded to massive,

fine- to medium-grained tuffaceous sandstones. The rocks are generally metamorphosed to

metasandstones. The good outcrops of fine-grained grey sandstone can be observed at river

mouth of Sungai Ta Eng (Figure 27). Cross bedding structure can be observed in parts

(Figure 28).

32

Figure 23: Deformed metatuff of the Gerik Formation

expose at river mouth of Sungai Kenarong. Figure 24: Deformed metatuff of the Gerik Formation

expose at river mouth of Sungai Kenarong.

The N-S trending ridge from the river mouth of Sungai Semilian at northern part of the

Temengor Lake to Sungai Banun is represented by deformed sedimentary rocks of the Gerik

formation. Quartz-mica schist occupies an N-S trending belt whose eastern margin is in

contact with the western margin of the Main Range Granite. The rock is grey to dark grey

and greenish grey in colour which consists of elongated quartz, biotite and muscovite. Some

biotite altered to chlorite due to weathering process.

In the Transect area, the unmappable calcareous facies of the Gerik formation is well

exposed in the Temengor Lake as small lenses between arenaceous facies and pyroclastic

facies. One of the good outcrops can be observed at the river mouth of Sungai Gadong i.e at

5o 36.759‟ N, 101

o 18.977‟ E (Figures 29 and 30). Generally, limestone in the calcareous

facies is metamorphosed to light grey to grey marble.

The argillaceous facies of Gerik formation comprises of tuffaceous shale, shale,

carbonaceous shale, siliceous shale and ribbon chert. The N-S trending ridge from the upper

reach of Sungai Chinchong at westhern part of the Transect area to river mouth of Sungai

Kedah and road cut of East-West Highway. Radiolarian bearing pelagic sediments comprises

pelagic chert and siliceous shale occurred at several localities along the East-West Highway.

One of the good outcrop can be observed at Km 18.6 East-West Highway (5o 31.655‟ N,

101o 14.790‟ E) which comprises subvertical to vertical strata of well-bedded light grey to

grey chert and silliceous shale interbedded with thin beds of shale (Figure 31). At this

locality the bedding thickness ranges from 5 cm to 10 cm. The shale beds become prominent

and thicker towards the east. Another outcrop is at a locality along the old stretch of the

highway (5o 31.633‟ N, 101

o 17.633‟ E) where the rock sequence is made up of thinly-

bedded siliceous shale interbedded with thin beds of shale with bedding thickness of 2 cm to

10 cm; and strike and dip, 140o/30

o (Figure 32).

33

Figure 25: Tuffaceous sandstone expose at Km 34 of

the East-West Highway.

Figure 26: Close-up of the tuffaceous sandstone

expose at Km 34 of the East-West

Highway.

Figure 27: Bedded metasandstone at Sungai Ta Eng. Figure 28: Cross-bedding in the metasandstone bed.

Figure 29: Calcareous facies expose at the river

mouth of Sungai Gadong.

Figure 30: Calcareous facies expose at river mouth

of Sungai Gadong.

34

Figure 31: Subvertical to vertical strata of well-

bedded light grey to grey radiolarian

bearing chert and silliceous shale

interbedded with thin beds of shale at

Km 18.6 East-West Highway

(5o 31.655‟ N, 101

o 14.790‟ E).

Figure 32: Thinly-bedded radiolarian bearing

siliceous shale interbedded with thin beds

of shale located at the old stretch of the

East-West Highway (5o 31.633‟ N,

101o 17.633‟ E).

Age and Correlation

Jones (1970) suggested that the age of Grik tuff (now Gerik formation) might be Late

Ordovician. Burton (1986) interpreted the age of the Grik tuff as Middle Ordovician.

However, Middle Ordovician to Early Silurian age was thought to be more possibility for this

pyroclastic rock. The presence of Anisopyge sp. and Phillipsia sp. (trilobite) in the calcareous

shale interbeded with tuff and dark grey impure limestone at Batu 2, Gerik in the Pengkalan

Hulu-Betong Transect area strongly indicates Middle Permian age of the clastic sediments

(The Malaysia-Thailand Working Group, 2010).

During the joint field check of the Malaysia-Thailand Working Group along the East-

West Highway, Northeastern Perak in March 2010, several radiolarian bearing chert and

siliceous shale samples had been collected from two localities along the highway. The first

locality was at Km 18.6 East-West Highway (5o 31.655‟ N, 101

o 14.790‟ E); and the second

locality was at a locality along the old stretch of the highway (5o 31.633‟ N, 101

o 17.633‟ E).

The radiolarians yield from the samples had been examined by Dr. Duongrutai

Saesaengseerung of DMR, Thailand. Based on diagnostic features observed under the

microscope, the radiolarian specimens discovered from both localities were identified as

Follicucullus sp., Gustefana sp., Latentifistula sp., Triplanospongos sp. and Albaillella sp.

Some specimens resemble Follicucullus scholasticus and Albaillella levis which are

important fauna. The age of these fauna are estimated as Capitanian to Changhsingian of

Middle to Late Permian.

35

Depositional Environment

Based on the well-bedded characteristic of the tuff, together with the presence of

epiclastic materials as well as the fact that the tuff is interbedded with argillaceous, siliceous

and calcareous materials at some places, this formation is interpreted as pyroclastic origin.

The volcanism might occur subaerially but the deposition of the erupted materials was in

marine environment (Jones, 1970). Sia (1989) reported that the occurrence of fossil algae

within the calcareous rocks in the tuff might indicate that the deposition was probably

occurred in the shallow marine environment. The presence of sandstone with cross bedding,

grit and conglomerate indicate that this sequent was deposited as the submarine fan. The

fine-grained pelagic sediments comprised of chert and siliceous shale was deposited in the

deeper part i.e. at the outer (distal) submarine fan.

3.1.6 Surficial Deposits

Recent surficial deposits comprise unconsolidated gravel, sand, silt and clay of fluviatile

and colluvial origin deposited in the non-marine environment overlying the major river

valleys and low lying areas.

On the Malaysian side, based on remote sensing interpretation, the surficial deposit is

named as A1 Unit and described below:

A1 Unit

The unit is interpreted to be alluvium. The A1 unit is distributed in the east part of the

Transect area from Malaysia-Thailand border in the north and along Kalai and Pergau river

to the southwest. The remote sensing characteristic of this unit is low flat topography with

principal stream in U shape valley. The principal stream branches irregularly. It has light

grey poto tone, agriculture vegetation and settlement landuse. The unit occur along Kalai and

Pergau Kalai River contains gravel, sand and silt, underlying the floodplain even the

limestone from karst topography in Kg. Batu area.

3.2 Igneous Rocks

3.2.1 Introduction

The igneous rock in study area consists predominantly of granitic rock. The Indosinian

Orogeny is presumed to have been evolved by the subduction of a continental crustal plate

(the western part) and an oceanic crustal plate (the eastern part) which is accompanied by the

granite emplacements (Metcalfe, 2000). Geologically, the granitic rocks in Peninsular

Malaysia are distributed as linear masses parallel to the Bentong-Raub Suture Zone. Malayan

orogeny is presumed by the subduction of a continental crustal plate (the western part) and an

oceanic crustal plate (the eastern part) which is accompanied by the granite emplacements.

36

In Malaysia, the granites can be divided into three belts based on lithology and

petrochemistry of the granite, namely, the Main Range Belt, the Central Belt and the Eastern

Belt. The Main Range granite which consists of S-type, ilmenite series granitoids, intruded

into the Paleozoic host rocks during the Permo-Triassic period. The Central Belt granite

consists mainly of S-type, ilmenite series granitoids of Triassic age with minor intrusion of

Cretaceous I-type, magnetite series granitoids. The Eastern Belt granite consists mainly of I-

type, magnetite series granitoids and intruded into Palaeozoic host rocks during the Permo-

Triassic period. The country rocks of the Main Range Province are separated from those of

the Eastern Province by a structure designated the Raub-Bentong line (Hutchison, 1977).

Later, Cobbing et al. (1986) divided the granites into two provinces Main Range granite

and Eastern granite comprises of the Central belt plutons, the Eastern belt plutons and the

Cretaceous plutons. The Main Range granite has been regarded to be constituted exclusively

of S-type granites of mainly Triassic age (Bignell and Snelling, 1977 and Liew and Page,

1985; Hutchison, 1977; Cobbing et al., 1986; Hutchison, 1996). In contrast, the Eastern

province granite is dominated by I-type with subordinate compositional overlap S-type

granites of Permo-Triassic age (Bignell &Snelling, 1977; Hutchison, 1977). Small I-type

plutons of Cretaceous age are present in the central part of the Peninsular Malaysia (Bignell

& Snelling, 1977).

Muenlek et al. (1982) recorded three granite phases which were classified as gneissic

granite, coarse-grained porphyritic biotite granite and tourmaline-muscovite granite in

published a regional geological map of Narathiwat sheet on scale 1:250,000.

Finally, Cobbing et al. (1992) completed the Southeast Asian granite project including

geological map of individual granite plutons, petrography, geochemistry classification and

Rb/Sr age determination, and classified the granite in Southeast Asia into three granite

provinces. The eastern granite province is composed mainly of Triassic I-type, magnetite

series granitoids with minor compositional overlapping with S-type granitoids. The minor

intrusion of isolated Cretaceous I-type, magnetite series is also present in this province. The

western granite province consists of a mixture of S-type and I-type granites of Cretaceous

age. The Main Range granite province and Northern Thai migmatite province composed

mainly of Triassic S-type, ilmenite series granitoids. However, minor intrusions of isolated

Cretaceous I-type, magnetite series granite plutons can be found in the northern Thai

magmatite granite province.

In term of age, the Main Range Batholith had been radiometrically dated at 198-220 Ma

(Late Triassic to Early Jurassic) ages (Hutchison, 2007). The summary of the geological

setting of the granites in Peninsular Malaysia is shown in Figure 33.

37

Figure 33: Geological setting of the granites in Peninsular Malaysia (modified after, Bignell & Snelling,

1977; Hutchison, 1977; Cobbing et al., 1986; Cobbing et al., 1992).

On the Malaysian side, the granitic rocks cover approximately 903 square km (42%) of

the Transect area. The description of the granitic rocks in this report is mainly based on the

works of Mohamad Hussein et al., (in manuscript). During the present work in January 2010,

an attempt had been made to describe the selected outcrops and the surrounding geology in

the Transect area. Granitic rocks that are part of the Main Range Granite exposed in the

central part of the Transect area. The Main Range Granite comprises the Kabut granite

(Trgrkb), the Merah granite (Trgrmr) and Singor granite (Trgrsg). In this report, the granite in the

Km 50 50 Km0

SCALE

100 00O l

104 00O lO l

102 00O l

102 00O l

100 00 East of GreewichO l

104 00O lO l

102 00O l

102 00O l

SINGAPORE

06 00

O

l

04 00

O

l

02 00

O

l

06 00

O

l

04 00

O

l

02 00

O

l

Western provincegraniteEastern provincegranite

Cretaceous granite

66. Noring granite67. Kenerong granite68. Batang Melaka granite69. Gunung Ledang granite70. Pulai granite

LEGEND

S t r a

i t s o f M

a l a

c c a

S o

u t h

C h

i n a

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aTHAILAND

66

67

BE

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68

69

70

38

study area is classified into different salient sub-zones based on field geological setting,

structural and petrography supported by petrochemistry and petrogenesis analysis.

The simplified geological sequence of igneous rocks in the Transect area is shown in

Table 3. The distribution of granites in the Transect area is shown in Figure 34. Correlation

of the granites in the Transect area is summarised in Table 4.

Table 3: Simplified geological sequence of igneous rocks on the Malaysian side of the Transect area.

Granite body Description

Singor Granite Leucocratic, fine- to medium-grained biotit-muscivit-

tourmaline granite.

Merah Granite Grey, fine- to medium-grained foliated bioite granite

Kabut Granite Grey, fine- to medium-grained porphyrytic biotite granite.

Table 4: Correlation of igneous rocks on the Malaysian side of the Transect area

Malaysian side Thai side Malaysian/Thai side

TRIASSIC

Singor Granite

(Trgrsg) Hala granite(Trgrhl)

Singor Granite/Hala

granite (Trgrsghl)

Merah Granite

(Trgrmr)

Budo Granite

(Trgrbd)

Merah/Budo Granite

(Trgrmr/bd)

Kabut Granite

(Trgrkt) La Sa granite (Trgrls)

Kabut Granite/La Sa

granite (Trgrkt)

Chantarat Granite

(Trgrch)

Chantarat Granite

(Trgrch)

The N-S and NE-SW trending quartz dykes and some small igneous stocks or dykes

such as microgranite, aplite, pegmatite and lamprophyre usually intruded into the main

granite body and also into the country rocks, especially the Carboniferous-Permian

metasediments at the central and eastern parts of the Transect area. Contact metamorphism

and the associated late stage mineralization may be observed in the country rocks.

The Main Range Granite batholith is the main component of the Main Range Province

of Peninsular Malaysia (Cobbing et al., 1986). It is the most widely spread granite mass,

stretches from Melaka in the south to the Thailand frontier in the north. It forms the

mountainous country generally regarded as the backbone of Peninsular Malaysia and

emplaced mainly into the Silurian-Devonian and Carboniferous-Permian successions. This

granite is considered as the S-type granite (Bignell and Snelling, 1977; Liew and

39

Page, 1985). It composed mainly of ilmenite series with S-type affinity granitoids and is

typically related to cassiterite mineralisation. Late stage leucocratic granites are common

including aplite dykes, pegmatite dykes, and quartz-feldspar veins.

In the Transect area, the Main range granite can be classified into three textural types:

medium to coarse-grained porphyritic biotite granite, named as Kabut Granite, fine to

medium-grained foliated biotite granite, named as Merah granite and late phase fine to

medium-grained leucocratic biotite-muscovite granite, named as Singor Granite.

On its western margin, the Main Range Granite intruded the Upper Palaeozoic rocks

represented by the Carboniferous Kubang Pasu Formation (Ckp) and the Permian Gerik

formation (Pgk). On its eastern margin, the granite intruded the Carboniferous Tiang schist

(Cts).

On the Thai side, the study of granite geology in the Transect area was very limited due

to security reasons. However, there was an effort by the local DMR workers who were

assigned to carry out a geological mapping program in the southern part of the country.

40

Figure 34: Distribution of granitic rocks exposed in the Transect area

41

3.2.2 Chantharat Granite (Trgrch)

Distribution

The Chantharat Granite (Trgrch) is only exposed on the Thai side. It can be traced along

the western flank of the Belum-Hala Transect area. In the Pengkalan Hulu-Betong Transect

area, this unit covers approximately 20% of the Transect area that can be observed on the

road-cuts along the local road from Ban Chantharat to Ban Ai Yoe Quin, and Ban Chantharat

to Ban Chulaporn 10.

Petrography

The vast majority of the Chantharat Granite (Trgrch) is characterized by its medium- to

coarse-grained, sparsely megacrystic to good megacrystic, unfoliated to weakly foliated

biotite granite. K-feldspar can be seen as large megacrysts of light grey to chalky white

colour with elongate to tabular and euhedral to subhedral habits. Plagioclase presents in

groundmass as chalky white colour, euhedral to subhedral crystals with tabular habit. Quartz

can be observed as anhedral to subhedral crystals, single and clusters. Cognate and accidental

xenoliths are also present in these rock. Dykes and veins are locally found along the intrusive

margins.

3.2.3 Kabut Granite/La Sa granite (Trgrkt/ls)

On the Malaysian side, the Kabut Granite (Trgrkt) is named after Bukit Kabut (Mohamad

Hussein et al., in manuscript), which is located at the southern part of topographic map sheet

no. 20 (Belum). On the Thai side, the La Sa granite (Trgrls) is named after Khao La Sa which

is located in the central part of topographic map sheet no. 52201 Khao Han Kut Quadrangle.

Distribution

The Kabut Granite/La Sa granite (Trgrkt/ls) is distributed on the northwestern and

southeastern part of the Transect area. In the northwestern part, the granite is in contact with

the Merah/Budo Granite (Trgrmr/bd), Chantarat Granite (Trgrch), Kubang Pasu/Yaha Formation

(Ckp/yh) and Betong Formation (SDbt). Whilst in the southeastern part, it is in contact with the

Merah/Budo Granite (Trgrmr/bd) and Tiang schist (Cts).

Petrography

The granite is grey in colour, medium- to coarse-grained and contains K-feldspar

megacrysts of up to 15-30% of the rock composition (Figures 35 & 36). The K-feldspar

megacrysts is grey in coloured, euhedral in shapes, particularly of prismatic, stubby and an

equant in shape. Their size mostly ranges from 1 cm up to 3 cm, but in several localities they

can reach up to 5 cm long. In places, the granite exhibits foliated texture formed by the

arrangement of K-feldspar megacrysts especially in the area closed to the minor late-phase

magma such as dyke or veins of quartz or lamprophyre. The equigranular variety exposed in

the contact zone with the Merah granite (Trgrmr) body.

42

Microscopically, the rock is granite in composition. It exhibits holocrystalline texture

and its grains are hypidiomorphic granular in shape. The major mineral constituents consist

of quartz (25-45%), K-feldspar (25-45%), plagioclase (35-50%) and biotite (5% to 15%).

Apatite, zircon, sphene, allanite and opaque minerals present as accessory minerals.

Figure 35: Photographs of the Kabut Granit/La Sa

granite (Trgrkb/ls) in Malaysia at Km 56.6 of

the East-West Highway.

Figure 36: Photographs of the Kabut Granit/La Sa

granite (Trgrkb/ls) in Sungai Singor area on the

Malaysian side.

3.2.4 Merah Granite/Bu Do granite (Trgrmr/bd)

The Merah Granite (Trgrmr) is named after Gunung Hulu Merah, Upper Perak, Malaysia

whereas the Bu Do granite (Trgrbd) is named after Khao Bu Do located at Narathiwat

Province, Thailand.

Distribution

On the Malaysian side, the Merah Granite/Bu Do granite (Trgrmr/bd) is widely distributed

in the central part of the Transect area as a north-south trending mountainous belt. The Merah

Granite/Bu Do granite (Trgrmr/bd) was intruded into the Kabut granite (Trgrkb) in the northern

part of the Transect area indicating that the Merah Granite/Bu Do granite (Trgrmr/bd) is

younger than the Kabut Granite/La Sa granite (Trgrkb/ls). The contact of this granite can be

observed near Kg Belum Lama at the upper reaches of the Sg Perak. Photographs of the

Merah Granite/Bu Do granite (Trgrmr/bd) on the Malaysian side are shown in Figures 37 & 38.

On the Thai side, based on data from the Batu Melintang Sungai Kolok Transect area,

granite outcrops are widely exposed along the Ai So stream and the adjacent area. It forms a

N-S trending batholith from the Malaysia-Thailand border to Sisakhon District (Bu Do

mountain range), in the middle part of Sisakhon Quadrangle, northeast of the Transect area.

The Bu Do granite exposed northern part of the Transect area. The southern part of this unit

covers high terrain in the north of the Sungai Perak in Malaysia.

43

Petrography

The granite is characterised by grey, fine- to medium-grained showing a distinct

preferred orientation of biotite. It is moderate to strongly foliated striking from NNW to NNE

and dipping almost 60 to 80 degrees from the ENE to ESE. In places, the K-feldspar

phenocrysts are also observed as minor constituents.

Figure 37: Photographs of the Merah Granite/Bu

Do granite (Trgrmr/bd) in Malaysia at

Sungai Kejar area. The foliation is

formed by a distinct preferred

orientation of biotite.

Figure 38: Photographs of the Merah Granite/Bu Do

granite (Trgrmr/bd) in Malaysia at Km 56.6 of

the East-West Highway. Cognag xenoliths

made up of mafic minerals enrichment

particularly biotite can be seen at the East-

West Highway outcrop.

Microscopically, the rock shows holocrystalline texture and the grains are

hypidiomorphic granular. This rock consists of quartz (30-35%), K-feldspar (20-30%) and

oligoclase (20-30%). The mafic mineral is made up of biotite (5-10%). The accessory

minerals are sphene, apatite, zircon, and epidote. Flakes of biotite are mostly oriented,

kinked, deformed and interspaced between other minerals.

According to The Malaysian and Thai Working Groups (2006), on the Thai side, the Bu

Do granite (Trgrbd) forms an elongated north–south trending mountain range, starting from

Pattani Province in the east coast, extending southward to Yala and Narathiwat Provinces

north of the Malaysia–Thailand border. It is composed mainly of ilmenite series with S-type

affinity granitoids and is typically related to cassiterite mineralization. The major rock

forming minerals are quartz, K-feldspar, oligoclase and biotite, whereas subordinate

muscovite and tourmaline are locally present as accessory minerals. Late stage leucocratic

granites are abundant including aplite, pegmatite dykes, and quartz-feldspar veins. It is

44

noteworthy that the major granitic rocks in the Bu Do granite batholith are generally non-

foliated to slightly foliated. However, these rocks have been locally foliated along the margin

and are called the marginal facies.

Age

Bignell (1972) has done geochronological study for the Malaysian granites using both

K/Ar and Rb/Sr methods. He concluded that the Main Range Granite is 200 – 230 Ma in age

and the granite emplacement took place during the Triassic. Later on, Cobbing et al. (1992)

reported the Rb/Sr isochron age of 207 Ma for Songkhla granitoid and 221 Ma for Satun

granitoid. According to the field observation mentioned earlier by Cobbing et al. (1992), the

Bu Do granite batholith (in Thailand) is geographically located within the Main Range

granite province (in Thailand), which is represented by the Songkhla pluton. Therefore, the

age of the intrusion of the Bu Do granite is also Triassic. The Merah/Bu Do granite (Trgrmr/bd)

is, therefore, assigned by the Malaysia-Thailand Working Group to be of Triassic S-Type

granite.

3.2.5 Singor Granite/Hala granite (Trgrsg/hl)

The Singor granite (Trgrsg) is named after Sungai Singor a tributary of Sungai Perak that

is located in the south of the East-West Highway in the Temengor area (Mohamad Hussein et

al., in manuscript). Hala granite (Trgrhl) is named after Hala Forest Reserve located in Yala

and Narathiwat Provinces, Thailand.

Distribution

The Singor Granite (Trgrsg) occurs as small isolated bodies within the Merah/Bu Do

Granite (Trgrmr/bd) and Kabut Granite/La Sa granite (Trgrkb/ls) in the Sungai Perak area. This

granite also intruded into the country rocks, especially the Carboniferous Tiang schist (Cts),

within the fault zone and present as minor stocks in a few localities. However, this rock has

been locally foliated along its margin and is called the marginal facies. Figure 39 & 40 show

photographs of the Singor Granite (Trgrsg) on the Malaysian side.

45

Figure 39: Photographs of the Singor Granite/Hala

granite (Trgrsg/hl) in Malaysia at the Sungai

Singor area. Photograph shows the contact

of the Singor Granite/Hala granite (Trgrsg/hl)

with the Kabut Granite/La Sa granite

(Trgrkb/ls) (dark in colour).

Figure 40: Photographs of the highly fractured

Singor Granite/Hala granite (Trgrsg/hl) in Malaysia at the Sungai Kejar area.

Petrography

Singor Granite/Hala granite (Trgrsg/hl) is light grey or leucocratic, fine- to medium-

grained, equigranular to inequigranular biotite-muscovite granite. Tourmaline is also present

in significant amount.

Microscopically, it exhibits holocrystalline and alotriomorphic equigranular and

hypidiomorphic granular textures. The major mineral constituents consist of quartz (50%),

K-feldspar (30%) and plagioclase (15%). The mafic minerals (5% to 15%) are made up of

biotite and muscovite with occasional tourmaline (Figure 41). Apatite, zircon and opaque

minerals are present as accessory minerals.

Tourmaline and muscovite are characterised as detritus and deuteric minerals

respectively. These minerals indicate that the rock was formed at the late phase of the

magmatic differentiation. This granite also shows the characteristics and relics of the Merah

/Bu Do Granite (Trgrmr/bd) and Kabut Granite/La Sa granite (Trgrkb/ls) in parts, which suggests

that the Singor Granite/Hala granite (Trgrsg/hl) pluton was formed at the late stage of the

granitoid intrusion.

46

Figure 41: Microphotograph of Singor Granite/Hala granite (Trgrsg/hl) shows

euhedral to subhedral tourmaline at Sungai Palai.

3.2.6 Age and correlation

Bignell (1972) has conducted a geochronological study for the Malaysian granites using both

K/Ar and Rb/Sr methods. He concluded that the Main Range Granite is 200-230 Ma in age

and granite emplacement took place during the Triassic. Bignell and Snelling (1977) also

concluded that the age of the granite is Triassic. Liew and Page (1985), reported that the age

of the granite is 198 to 220 Ma (Late Triassic to Early Jurassic) based on U-Pb zircon dating

method.

47

4.0 STRUCTURAL GEOLOGY

4.1 Introduction

Based on remote sensing study, linear features are well developed in the all rock units

terrains. Bedding trends are well expressed in the sedimentary, volcanic and metamorphic

rock units but dips magnitudes are difficult to elucidate. The regional structural trend is

roughly N-S as expressed by the alignment of strike ridges and lithological boundaries.

Fracture lineaments are prominent and abundant in this area, particularly in the

granitoid, volcanic and metamorphic terrains with at least three main sets trending NE-SW,

NNW-SSE and E-W (see Figure 7). The major lineaments trending NE-SW are Selantan

Fault, Laho Fault, Cheng Fault, Jakal Fault and Belang Fault, whilst the NNW-SSW trends

are Ruok Fault and Makar Fault. The E-W trend is represented by Belum Fault, Tiang Fault,

Mendelum Fault and Banun Fault. Some circular features are also apparent in the volcanic

unit (crater?) and the granitoid unit (minor intrusion).

Pre-orogeny sedimentary successions in the Transect area are generally folded into a

series of synclines and anticlines. Folding is characterised by tight, asymmetric and open

folds, resulting in the repeated and overturn sequences in the older sedimentary rocks. The

NE-SW and N-S trending fold axes are sub-parallel to the long axis of the Malay Peninsula.

Historically, Malay Peninsula was formed as a result of the marine sedimentation took

place continuously throughout the Silurian-Devonian and Carboniferous-Permian periods,

then collision between Sinoburmalaya (Sibumasu/Shan Thai) block in the west and Eastmal-

Indosinia block in the east. The collision zone is represented by the Bentong-Raub Suture

which can be traced northward into Thailand and southward into the Banka and Biliton

Islands. This collision accompanied by the major tectonic event during Middle to Late

Triassic has resulted in rock deformation in the Malay-Thai Peninsula especially along and

adjacent to the suture zone. Tectonic activities have affected most of the rock units that form

various structures such as folding, faulting, jointing and fracturing. It was followed by major

igneous intrusion that forms the Main Range granite to the west of the suture zone. The large

breaks of sedimentation can be observed due to the uplift of granitic rocks during the

Triassic.

The continent-continent collision has caused uplifting and faulting along an N-S

direction. Uplifting resulted in the formation of N-S trending of the granite mountainous

range in the area. Pre-collisional rocks are fractured along the N-S direction as can be

observed in the Tiang schist and Mangga formation as well as in the Gerik Formation.

However, some major structures especially in the eastern part of the Transect area may have

been affected by the younger Cretaceous Noring granite intrusion and multi direction

fractures.

Tectonically, the Transect area was formed by the collision of two tectonic terranes: the

Sibumasu terrane in the west and Indochina terrane in the east which is separated by the N-S

trending former subduction zone known recently as the Bentong-Raub Suture Zone.

48

On the Malaysian side, the structural geology of the Transect area generally corresponds

to the regional tectonic pattern of the Peninsular Malaysia. However, detailed mapping has

revealed that, in some places, the local structures appear to have a slight variance as

compared to the regional pattern. It is believed that the active period of tectonic activity

during the Triassic. For example the Bentong-Raub Suture Zone was responsible for the

formation of major structures in the Transect area. The igneous intrusion and uplifting also

occurred during this time.

In Thailand, Khositanont (2004) have concluded that the Ka Toh-Buyong fault zone in

the Batu Melintang-Sungai Kolok Transect area is the northward extension of the Bentong-

Raub Suture Zone and represents a continent-continent suture on the Thai-Malay Peninsula.

The younger NE-SW and NW-SE fractures, which can be prominently observed in both

igneous and sedimentary host rocks, may have been resulted from the movement of the major

fault along the Malaysia–Thailand border.

4.2 Bedding

Bedding trends that roughly parallel with the foliation still can be observed in the

metasediments.

Graded bedding and cross bedding can be observed in some of the arenite beds

especially in the Kubang Pasu/Yaha Formation. No other sedimentary structures observed.

This might be due to the regional metamorphism that accompanying the folding and faulting

acted on the rock and destroyed all the sedimentary structures.

4.3 Foliation

The foliation is formed by subparallel to parallel alignment of the light and dark

coloured minerals in the rocks. This can be observed in the metasediments. In the Transect

area, foliation also can be observed in the granitic rock especially in the Merah/Bu Do

Granite (Trgrmr/bd). Foliation in the granite is believed to be formed as a result of crystal-

plastic process during the crystallization of the rock.

4.4 Folding

Pre-orogeny sedimentary successions in the Transect area are generally folded into a

series of synclines and anticlines that can be interpreted from the bedding‟s strike analysis.

Folding is characterised by tight, asymmetric and open folds, which cause the repeated and

overturn sequence in the older sedimentary rock. Generally folds are trending in the NE-SW

to N-S direction and the fold axes are sub-parallel to the long axis of the Malay Peninsula.

The synclinal and anticlinal axes can be recognised in the western side of the Transect area.

Other minor folds are present with small magnitude. Most of the bedding planes dip towards

the east with various dip angles.

49

4.5 Faulting

Faulting is widespread throughout the Transect area. Faults generally vary in width,

characterised by fractured, sheared or mylonitised rocks with the presence of slickensided

surfaces. However, in most cases it is very hard to observe traces of fault zones in the field

due to the thick soil cover and deep tropical weathering. Aerial photographs interpretation

and field evidences indicate that there are two prominent fault directions in the Transect area

i.e. NW and NE trending sets (see Figure 7). There are several faults, which are mainly of

strike-slip and normal faults, trending, NW-SE, NNW-SSE and NE-SW. Of these, the NW-

SE trending faults are the main fault of the Transect area. Among the major faults are Ruok

Fault (NNW-SSE), Jakal Fault (NNE-SSW), Laho Fault (NE-SW), Belang Fault (NE-SW),

Belum Fault, Tiang Fault, Mendelum Fault and Banun Fault (E-W).

Syed Sheikh Almashoor and Tjia (1987) reported the prominent fault in the Transect

area is named as the Ruok Fault. Based on Landsat image interpretation, the fault zone that

trends in the NNW-SSE direction covers a 4 km wide zone of tonal and topographic

lineaments that extend from Mae Nam Pattani in the north, in 165o direction, trends parallel

with Sungai Kenerong and than probably ends at Sungai Sara in the south (Figures 42 & 43).

The fault crosses the East-West Highway at Km 184 towards Kota Baharu (208 km towards

Ipoh, 05o 34.521‟ N, 101

o 24.289‟ E), where it can be observed within the quartz-mica schist

and phyllitic rocks with northerly strike and steeply dip foliation (Figure 44). Numerous

sigmoidal quartzs (Figure 45) within the schist and phyllite indicates left-lateral strike-slip

movement (Syed Sheikh Almashoor and Tjia, 1987).

In some places, faults formed the lithological contact between the granites and the

metasedimentary rocks. These can be observed along parts of the Laho Fault, Sungai Dadek

and Jakal Fault in the Transect area. Major faults might have been formed during the Late

Triassic because they cut the earlier Triassic igneous rocks.

4.6 Jointing

Joints can be observed in all rock types. Most of the joints are steeply dipping. There are

also minor subhorizontal joints. Joints system analysis on the granite around Sungai Singor

revealed the main deformation (P) in the 126o

- 306o direction. Whereas the joints in the

granite body in the central part of the Transect area lies in the 015o-195

o direction, the joints

in the metasedimentary rocks around the Sungai Tiang area is 023o - 203

o.

50

Figure 42: Lineaments interpreted as the Ruok Fault Zone that almost parallel with the Temengor Lake

orientation (after Syed Sheikh Almashoor and Tjia, 1987).

Khlong The Pho

Zo

ne

Fracture

Ridge

Strike valley andindistinct lineament

LINEAMENT

100 20

Kilometres

Nor

th

F a

u l t

S. Tiang

TEMENGGORRESERVOIR

R u

o k

S. Singor

Nor

th

Banding

Landsat 310 Jan 1979

S. Perak

East - West highway

North

51

Figure 43: Location of the Ruok Fault Zone (after Syed Sheikh Almashoor and Tjia, 1987)

Ban Nang Sata

Gerik

S. Singor

S. Tiang

S. PerakS

. Kenero

ng

S. P

atta

ni

Betong

Keroh

S. P

erg

au

S. S

ara

S. Perak

P E R A K

KEDAH

T H A I L A N D

K E

L

A N

T A

N

LEGEND

Fault

Road

River

International boundary

State boundary

F

F

F

0 10 20KILOMETERS

INDEX MAP

52

Figure 44: The Ruok Fault Zone crosses the East-

West Highway at km 184 towards Kota

Baharu (208 km towards Ipoh)

(05o 34.521‟ N, 101

o 24.289‟ E), where it

can be observed within the quartz-mica

schist with northerly strike and steeply

dip foliation.

Figure 45: Numerous sigmoidal quartzs within the

schist in the Ruok Fault Zone at km 184

towards Kota Baharu (05o 34.521‟ N,

101o 24.289‟ E).

53

5.0 MINERALS AND OTHER NATURAL RESOURCES

5.1 Introduction

The Transect area is not known for its economic deposits as there are no records

of prospecting and mining in the past. However, prospecting and mining activities

have been carried out in the Batu Melintang-Sungai Kolok and Pengkalan Hulu-

Betong Transect areas in the Kalai, Berusong and Kelian Intan in Malaysia, and Tham

Thalu and To Mo areas in Thailand (The Malaysian-Thai Working Group, 2006 &

2010).

On the Thai side, mineral potential area in the Belum-Hala Transect area has

been studied by DMR using airborne geophysic and magnetic anomaly since 2003.

The mineralization is related to the contact metamorphism of granite intrusions and

country rocks, and subsequent hydrothermal activities. The Pb-Zn sulphide mineral

potential area, along the Hala stream, near the Malaysia-Thailand border is observed.

Mineralization was interpreted to occur in the contact zone between the granite and

country rocks. High magnetic anomaly similar to those of the Pb-Zn sulphide model

of the Tham Ta Lu area in Bannang Sata District was identified. The other Sn-W

mineral potential area was proven in Ban Ai Yoe Quin, at the edge of the eastern part

of the Belum-Hala Transect area. Mining activities in the surrounding of the Transect

area is shown in Figure 46.

54

Figure 46: Mining activities in the surrounding areas.

5.2 Geochemical Exploration

On the Malaysian side, regional geochemical survey had been carried out by a

group of geologists of Minerals and Geoscience Department in 1991 to 1993 covering

Topographical Map Sheets 11 (Gunung Ulu Merah), 19 (Kerunai) and 20 (Belum)

areas. Stream sediment and rock samples were collected for geochemical study. As a

result, several multi-elements anomalous areas were identified; of which seven of

them are situated in the Belum-Hala Transect area (Figure 47). Pertinent information

on these anomalies including element associations, area extent, underlying geology,

the number of anomalous samples and the range of values is summarized in Table 5.

Anomalies are ranked from one to four in descending order of follow-up priority.

55

Follow-up work is not recommended for anomalies with a rating of four. Descriptions

of first-, second- and third-order anomalies are given below.

Anomaly 1901 [Sn, W, U (As, Ag, Zn, Pb)]

Anomaly 1901 is situated in the upper reaches of Sungai Kenarong, close to the

Malaysia-Thailand border. The area covers approximately 20 square km and is

underlain by arenaceous rocks of the Carboniferous Kubang Pasu Formation, intruded

by small granitic stock. Anomalous elements are Sn, W and U as well as As, Ag, Pb

and Zn. Sn value ranging from 40 ppm to 160 ppm whereas W ranging from 3 to

20 ppm and U ranges from 2 to 19.8 ppm. This anomaly is rated as Priority 3 which

requires possible follow-up for Sn, W and U.

Anomaly 1903 [Au, Cu, Co (Mn, Ni, Hg)]

Anomaly 1903 is situated on the western part of the Transect area. It covers

approximately 27 square km in the headwaters of Sungai Kedah and Sungai Cermin.

The area is underlain by arenaceous and argillaceous rocks of the Permian Gerik

formation, intruded by small dolerite dyke. This is essentially an Au-Cu-Co anomaly

with less extensive anomalies for Mn, Ni and Hg. Gold value in stream sediment is

0.05 to 10.049 ppm whereas in heavy mineral concentrate it gives maximum tenor

value 3.2 mg/m3. Anomalous Cu and Co are found in Sungai Cermin. Their values in

stream sediment are ranging from 60 to 300 ppm and 22 to 103 ppm respectively.

This anomaly was rated as Priority 2 that requires eventual follow-up for Au, Cu and

Co.

Anomaly 2001 [Sn, As, W (Zn, Au)]

This is predominantly Sn-As-W anomaly, located in the Sungai Palai drainage. It

covers an area of at least 43 square km. The rocks underlying this anomaly are

predominantly quartz-mica schist of the Tiang Schist that intruded by small stocks of

Singor Granite. The area is cut by NE-SW fault that runs parallel to the Laho Fault.

Tin and tungsten show high anomalous geochemical values in the stream sediment

where anomalous Sn values range from 20 to 40 ppm and W from 4 to 12 ppm.

Anomalous Sn values are randomly distributed over the area whereas As and W show

good association. This anomaly is given Priority 3 which requires possible follow-up.

Anomaly 2002 [Sn, Ag, W, As (Pb, Ni, U)]

This multi-element anomaly, located in the upper reaches of Sungai Dadek and

tributaries of Sungai Mangga with an areal extent of 51 square km. High geochemical

values are centred over the NE-SW Jakal Fault and unnamed NW-SE fault which

demarcates the contact between the Triassic Kabut Granite and the Carboniferous

Tiang schist. This anomaly is highlighted by Sn associated with Ag, W and As. It is

defined by thirteen anomalous stream sediment samples containing Sn values ranging

from 20 to 30 ppm and also anomalous values of Ag (39 samples), W (15 samples)

56

and As (19 samples). Anomalous values of Pb, Ni and U also occur. This anomaly is

given a Priority 2 and should be followed up to assess the tin and tungsten potential.

Figure 47: Anomaly map of the Transect area.

57

Table 5: Summary of anomalies on the Malaysian side of the Transect area.

Anomaly

No. Element(s)

Area

(km2)

Range in ppm

(No. of anomalous samples) Geology

Priority

Rating

1901 Sn, W, U

(As, Ag, Zn, Pb)

20 Sn 40-160 (11)

W 3-20 (10)

U 2-19 (10)

As 8-120 (4)

Ag 0.08-0.4 (12)

Zn 110-260 (10)

Pb 6-60 (4)

Arenaceous rocks of Carboniferous Kubang Pasu

Formation, intruded by small granitic stock

3

1903 Au, Cu, Co

(Mn, Ni, Hg)

27 Au 0.015-10.049 (9)

Cu 60-300 (5)

Co 22-103 (5)

Mn 5,000-6130 (2)

Ni 16-83 (3)

Hg 0.05-0.16 (2)

*Gold tenor: 3.2 mg/m3

Arenaceous and argillaceous rocks of Permian

Gerik formation, intruded by small dolerite dyke

2

2001 Sn, As, W

(Zn, Au)

43 Sn 20-40 (31)

As 10-200 (22)

W 4-12 (8)

Zn 127-142 (2)

Au 0.083-0.324 (2)

Predominantly quartz-mica schist of the Tiang

schist intruded by small stocks of Singor Granite,

microgranite, lamprophyre as well as quartz

veins.

3

2002 Sn, Ag, W, As

(Pb, Ni, U)

51 Sn 20-30 (13)

Ag 0.6-1.0 (39)

W 8-40 (15)

As 10-60 (19)

Pb 51-96 (5)

Ni 49-55 (3)

U 6.2-14.2 (8)

Contact aureole between the Kabut Granite and

Tiang schist. Fault zone striking NE-SW and

NW-SE

2

Note:

Priority 1 indicates high priority rating - warrants immediate follow-up

Priority 2 indicates moderate priority - requires follow-up

Priority 3 indicates low priority - possible follow-up

58

5.3 Other Geological Resources

Other potential geological resources in the Transect area are rock aggregates and

dimension stone. The reserves are sufficient enough to be quarried for construction materials.

The granite supplies are available mainly from the Merah and Kabut Granites. There are three

abandoned quarries, which previously supplied rocks aggregate for the construction of the

East-West Highway, such as at Km 61.6 (05o 36.057‟ N, 101

o 30.532‟ E) and at Km 63.3 (05

o

36.345‟ N, 101o 31.181‟ E) as shown in Figures 48 and 49 respectively.

Figure 48: Abandoned granite quarry at Km 61.6 of

the East-West Highway.

Figure 49: Abandoned granite quarries at Km 63.3 of

the East-West Highway.

59

6.0 DISCUSSION AND CONCLUSION

6.1 Discussion

i. Lithostratigraphically, the Betong Formation (SDbt) is the oldest rock unit exposed

in the Transect area. However this rock unit is not exposed on the Malaysian side

within the Transect area.

ii. Structurally, the Tiang schist (Cts) was affected by the tectonic activity along the

Bentong-Raub Suture Zone that can be observed along the eastern margin of the

rock unit and the intrusion of the Main Range Granite in its western margin.

iii. The Carboniferous Kubang Pasu/Yaha Formation (Ckp/yh) is distributed in the

central and western parts of the Transect area. The rocks are metamorphosed to

metasandstone, hornfels, phyllite and schist due to the Main Range Granite

intrusion. The Kubang Pasu/Yaha Formation (Ckp/yh) is conformably overlain by

the Permian Gerik formation.

iv. The Carboniferous-Permian Mangga formation (CPmg) was affected by the

tectonic activity along the Bentong-Raub Suture Zone. Pelagic sediments within

the Bentong Raub Suture Zone contain the radiolarian Follicuculus sp. suggesting

a Permian age.

v. The Permian rock unit in the Transect area is represented by the Gerik formation

(Pgk) comprising predominantly tuffaceous sediments. Radiolarian fauna

discovered in the siliceous sediments within this rock unit were identified as

Follicucullus sp., Gustefana sp., Latentifistula sp., Triplanospongos sp. and

Albaillella sp. Some specimens resemble the important fauna of Follicucullus

scholasticus and Albaillella levis. The age of these fauna are estimated as

Capitanian to Changhsingian of Middle to Late Permian (Saesaengseerung, pers.

comm., 2011).

vi. Surficial deposits comprise unconsolidated gravel, sand, silt and clay of fluviatile

and colluvial origin deposited in the non-marine environment overlying the major

river valleys and low lying areas.

vii. The granite in the Transect area can be divided into four units; namely, in

ascending order:

a. the Chantarat Granite (Trgrch) – medium- to coarse-grained, sparsely

megacrystic to good megacrystic, unfoliated to weakly foliated biotite granite.

b. the Kabut Granite/La Sa granite (Trgrkb/ls) – grey, fine- to medium-grained,

porphyrytic biotite granite

c. the Merah/Bu Do Granite (Trgrmr/bd) – grey, fine- to medium-grained, foliated

biotite granite

60

d. the Singor Granite/Hala granite (Trgrsghl) – Leucocratic, fine- to medium-

grained biotite-muscovite granite with occasional tourmaline.

viii The main structural feature in the Transect area is Ruok Fault. The fault zone

trends NNW-SSE extending from Mae Nam Pattani in the north, in 165o

direction, parallel with Sungai Kenerong and than probably ends at Sungai Sara in

the south.

6.2 Conclusion

i. The marine sedimentation in the Transect area took place continuously throughout the

Paleozoic Eras. Nevertheless, the large breaks can be observed due to the uplift of

granitic rocks during the Triassic.

ii. On the Thai side of the Transect area, the photogeological interpretation which have been

correlated with the previous geological data and information revealed the rock units in

the Transect area are as follows in ascending order:

a. ST1 and ST2 units correlatable with the Silurian-Devonian Kroh/Betong

Formation (SDkr/bt),

b. ST3 unit correlatable with the Carboniferous Kubang Pasu/Yaha Formation

(Ckp/yh),

c. ST4 unit correlatable with the Tiang schist

iii. The Silurian-Devonian Betong Formation (SDbt), Tiang schist (Cts), the Kubang

Pasu/Yaha Formation (Ckp/yh), the Mangga formation (CPmg) and the Gerik formation

(Pgk) were deposited on the Sibumasu terrane. All these Palaeozoic rocks in the Transect

area were subsequently intruded, faulted against, and metamorphosed by the Triassic

Main Range Granite.

iv. Based on regional geochemical survey carried out by the Minerals and Geoscience

Department Malaysia during 1991 to 1993, seven multi-elements anomalous areas had

been identified on the Malaysian side of the Transect area.

v. Rock aggregates and dimension stone have the potential to be exploited in the Transect

area.

61

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64

- 64 -

APPENDICES

65

- 65 -

APPENDIX 1

List of the Malaysian-Thai Working Group Member

Malaysian Working Group Member Thai Working Group Member

Name Name

1. Mr. Alexander Unya Ambun 1. Dr. Tawsaporn Nuchanong

2. Mr. Ibrahim bin Amnan 2. Dr Assanee Meesook

3. Mr. Noor Bakri bin Endut 3. Mr. Naramase Teerarungsigul

4. Mr. Mohd Badzran bin Mat Taib 4. Dr. Suree Teerarungsigul

5. Mr. Mohamad Hussein bin Jamaluddin 5. Mr. Terapon Wongprayon

6. Mr. Mohamad Sari bin Hasan 6. Mr.Suvapak Imsamut

7. Mr. Mat Niza bin Abdul Rahman 7. Ms. Piya-orn Assavapatchara

8. Mr. Muhammad Mustadza bin Mazni 8. Mr. Kitti Khaowiset

9. Mr. Mohd Anuar bin Ishak 9. Mr. Sutee Jongautchariyakul

10. Mr. Amir Mizwan bin Mohd Akhir 10 Ms. Pachara Sangoen

11. Mr. Azizan anak Juhin 11 Dr. Doungrutai Saesaengseerung