Geology of Thailand

7/27/2019 Geology of Thailand

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GEOLOGY OF THAILAND

Thailand is located in Southeast Asia between latitudes 5o 37 N and 20o 27 N

and longitudes 97o 22 E and 105o 37 E and cover area of 518,000 km2. It is bounded to the west byMyanmar, to the north by Myanmar and Laos, to the east by Laos and Cambodia, and to the south by

Malaysia. Physiographical, the country can be divided into four regions; the mountainous highland inthe north and northwest, the khorat plateau in the northeast, the central plain and the southern

peninsular, which are between Andaman Sea and the Gulf of Thailand.

STRATIGRAPHY

Geologically, Thailand consists of rocks range in age from Precambrian to Quaternary.

Precambrian

Precambrian rocks in Thailand were mentioned for the first time by the late Colonel Samak

Buravas from his pioneer studied of the high grade schistose rocks in the Pnom Sarakham area. Since

then, many geologists have assigned all the high grade metamorphic rocks under examined to be of

Precambrian sequence. Results and ideas from earlier investigations of the Precambrian and the

associated Lower Paleozoic rocks have reached the following general conclusions:


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A map of Thailand showing distribution of inferred Precambrian rocks

a. The Precambrian rocks in Thailand expose only in the North, Upper West, East, Lower and

Southern parts of the country.

b. The common lithologic associations of these rocks are mainly granitic to

granodioritic paragneisses, mica schist, hornblende schist or amphibolite, calc-silicate and marble of

the Almandine Amphibolite Facies with frequent collaboration of orthogneiss, migmatite, pegmatite,

aplite and granites.

c. They are usually associated with Lower Paleozoic rocks of the Greenschist Facies, which

grade into a mildly metamorphosed and unmetamorphosed rocks of the younger succession.

d. Due to the lack of outcrop continuation between the Amphibolite Precambrian rocks and

the Greenschist Lower Paleozoic rocks, an unconformity is usually proposed, however, this has neverbeen really observed.


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e. Except the unmetamorphosed Lower Paleozoic rocks at Tarutao island, elsewhere their

grades of metamorphism are rather constant within the Greenschist Facies range and more or less

parallel with the associated upper Amphibolite Facies of the Precambrian rocks. This is supported by

observations in most cases that, the original bedding and cleavage or schistosity are usually parallel.

f. Commonly rock types and age consistencies between the lower part of the Lower Paleozoic

and the upper part of the Precambrian rocks are usually observed in various places.

g. Very likely, the original rock types of the Precambrian before the regional metamorphism

were a thickly alternating sequence of impure arenaceous to argillaccous sediments with mainly

impure carbonate and rare siliciclastics. A rather mafic constituent may represent an involvement of

mafic volcaniclastics.

h. The Lower Paleozoic rocks have been thought to represent the siliciclastic carbonate facies

of the shelf deposit.

i. Structural analysis has been rarely investigated. The available studies reached the same

conclusion that there were at least two episodes of regional metamorphism and two periods of

cataclastic deformation. For the second regional metamorphism, only local overgrowths have been

quoted as the verified indication. Apparently there is no prevail cutting across among schistosity or

cleavage has been witnessed. Local evidence suggests against the second regional

metamorphism. More recent and specific studies on the Precambrian rocks from various parts of the

country have more or less confirmed the afore mentioned scenario as being summarized below.

j. Review of the mineral assemblages from various regions contradicted the earlier report ofthe type of metamorphism. They indicate the Cordierite Amphibolite Facies of the Abukuma Facies

Series (LP/HT) rather than the Almandine Amphibolite Facies (IP/IT).

k. Superimposed contact metamorphism was evidenced by its unique mineral

assemblages contradictory to those that are presented in the regional metamorphism.

Geochronological studies dated such contact metamorphism at Cretaceous time.

l. PT condition of the regional metamorphism has been evaluated from the observed

mineral assemblages relative to the relevant experimental results and came up with 3.5 - 4 Kb

pressure and 650-660o

c for the formation.

m. Geochronological studies gave two different ages of metamorphism at around

Triassic/Jurassic boundary and Cretaceous. However, the Precambrian rock pebbles being found in

the nearby Mesozoic red beds favors the metamorphism that took placed during the Triassic/Jurassic

boundary.

n. A singular metamorphism supports a transitional or gradational contact between the

Amphibolite Precambrian rocks and the Greenschist Lower Paleozoic rocks. Furthermore, there has

been no observation to verify that the older rocks of Precambrian have been served as a source for

the younger Lower Paleozoic rocks.


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o. Original sedimentary rocks before metamorphism were investigated by Rb/Sr small slab

technique and gave the depositional age of around 600 Ma.

Paleozoic

Lower Paleozoic

The Lower Paleozoic rocks of Thailand are subdivided into the lower Lower Paleozoic rocks

ranging in age from Cambrian to Ordovician and the upper Lower Paleozoic rocks ranging in age from

the Silurian to Devonian, and up to the early Carboniferous in some rock units. In Shan-Thai Terrane,

these rocks are widespread in western mountain area extending from Kanchanaburi Province in the

west to Chiang Mai, Mae Hong Son and Uttaradit Province in the North; and to Chon Buri in the east.

The rocks in the Peninsula are widely distributed in northsouth direction alongside of Khao Luang

mountain range, extending from Surat Thani Province through Nakhon Si Thammarat and Satun

Province to North Malaysia. In Indochina Terrane, only the upper Lower Paleozoic rocks are exposed

in northeastern part of Loei Province extending in north-south narrow belt across Thai-Laos border

to Western Laos.


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Map showing the distribution of the Lower Paleozoic rocks of Thailand

In general, most of the lower Lower Paleozoic rocks of Thailand have been subjected to low

grade regional metamorphism (greenschist facies) and contact metamorphism in the area close to

granite. The rocks are also strongly folded and faulted. These rocks are closely associated with and lie

unconformable above the Pre-Cambrian high-grade metamorphic rocks in Shan-Thai Terrane.

The lower Lower Paleozoic rocks of Thailand can be divided into two conformable rock units :

a lower siliciclastic, the Tarutao Group, and an upper carbonate, the Thung Song Group. The Tarutao

Group at the Tarutao Island, Satun Province, is a thick sequence of red sandstone, siltstone, shale

and conglomerate with the Late Cambrian trilobite on the upper part of the sequence. However, most

of the rocks on the mainland are quartzite. This group is a shallow shelf sequence periodically

subjected to storm. The overlying Ordovician Carbonates, the Thung Song Group, is a thick sequence

of tropical limestones, dolomites and calcareous shales. At least seven distinctive lithostratigraphic

units have been recognized in the South as the Malaka Formation, Talo Dang Formation, La NgaFormation, Pa Nan Formation Lae Tong Formation, Rung Nok Formation, and Pa Kae Formation. The


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Pa Kae Formation is the red stromatolitic limestone proposed for the uppermost Formation of the

Thung Song Group in the South. They were deposited in peritidal environment on a homoclinal ramp

during a long marine transgression in Early Ordovician, followed by shoaling, reefs, and a deeper

subtidal in a Middle, and a greater deepening during the Late Ordovician. Lithologically, the carbonate

rock of the Thung Song Group is very similar throughout Thailand. However, the age of the similar

rock unit in the east is still in controversy. The Cambrian-Ordovician boundary lies within the top most

part of the Tarutao Group whereas the OrdovicianSilurian boundary is placed in the black graptolitic

shale of the upper Lower Paleozoic rock, the Wang Tong Formation, about 25 meters above the Pa

Kae Formation.

The upper Lower Paleozoic rocks of Thailand which lies conformably above the Early

Paleozoic Rocks can be differentiated into 2 major north-south facial belts, the shelf-basin in the west

and the Peninsula, and the magmatic arc facies in the Sukhothai Fold Belt and Eastern part of the

Peninsula. The rocks in the west from Kanchanaburi to Mae Hong Son Province and the Peninsula are

black graptolitic and tentaculitic shale, chert, sandstone, siltstone and variegated stromatolitic nodular

limestone of shelf to back-arc basin facies. These rocks were formerly referred to as the Tanaosi

Group and Kanchanaburi Group but now they are defined as the Thong Pha Phum Group. In the

Peninsula from Surat Thani to Satun Province, this rock is represented by a continuous succession of

those deeper water siliciclastic and carbonate rocks. At least three conformably lithostratigraphic units

have been recognized in Satun Province. They are the Wang Tong Formation, Kuan Tung Formation

and Pa Samed Formation. Studies on the graptolite, trilobite, brachiopod, ammonite and conodont by

many paleontologists from Australia, England, Japan and USA. reveal that the upper Lower Paleozoic

rocks of this shelf-basin facial belt in the Peninsula are ranging in age from Late Ordovician to Early

Carboniferous. They seem to be conformably underlied the Upper Paleozoic rocks. However, recent

study on deeper water fossils from the Pa Samed Formation of Prof. Boucot and his colleaguesindicates the presence of a major disconformity between the Emsian dacryoconarid-rich beds and the

overlying siliciclastics that have yielded Carboniferous faunas. The upper Lower Paleozoic rocks in the

Sukhothai Fold belt of Shan Thai Terrane, in Eastern part of the Northern Highland, the Eastern Gulf

and Eastern part of the south can be separated into three facial belts including 1) back-arc-basin

facies in the west, 2) volcanic arc facies in the middle, and 3) inner trench stope facies of fore-arc in

the east.

Upper Paleozoic

The lithostratigraphic nomenclatures of the Upper Paleozoic strata in Thailand have beensummarized and correlated. The Mae Tha Group, Dan Lan Hoi Group, Doi Kong Mu Formation andFang Redbeds represent the Carboniferous strata, whereas the Phrae Group has been designated forthe Carboniferous-Permian succession in the Northern and Upper Western Region. The Nong DokBua, Wang Saphung, Dok Du and Huai Som Formation represent the Carboniferous strata in Loei-Petchabun Ranges region. The Kuan Klang Formation has been assigned for the Carboniferous rocks,whereas the Kaeng Krachan Group that contains pebbly mudstone and sandstone represent theCarboniferous-Permian strata in Lower Western and Southern region. The Ngao, Saraburi,Chanthaburi and Ratburi Groups represent the Permian strata in Northern and Upper Western, Loei-Petchabun Ranges, Eastern, and Lower Western and Southern regions respectively.

Mesozoic

Mesozoic rocks of Thailand consist of both marine and non-marine deposits. Whereas themarine rocks are well distributed in the northern, western and southern parts of the country, the non-


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marine rocks are widespread in the northeastern part (Khorat Plateau) and partly in the southern

peninsula. The marine rocks consist mainly of limestones, mudstones, sandstones, dolomites, and

conglomerates having been deposited in submarine fan and shallow water environments. These rocks

range in age from Lower Triassic to early Middle Jurassic on the basis of the ammonites, bivalves and

additional data from microfossils and stratigraphic correlations. The revised lithostratigraphic units

and correlations for the Triassic Lampang Group are summarised including other units in various parts

of Thailand. In the Jurassic Period, twelve new lithostratigraphic units have been established for the

marine Jurassic rocks in the Mae Hong Son, Mae Sot, Lamphang, Kanchanaburi, Chumphon, and

Nakhon Si Thammarat areas. The brackish facies of the Middle Jurassic Khlong Min Formation in

southern peninsula is also briefly reported. The Toarcian-early Bajocian age (upper Lower-lower

Middle Jurassic) is confirmed so far for the Thai marine Jurassic. The marine Cretaceous rocks have

not yet been reported elsewhere in Thailand.

The non-marine Mesozoic rocks in the Khorat Plateau belong to, in ascending order, the Huai

Hin Lat, Nam Phong, Phu Kradung, Phra Wihan, Sao Khua, Phu Phan, Khok Kruat, Maha Sarakham

and Phu Thok Formations of the Khorat Group. Reddish-brown to light-grey sandstones,

conglomeratic sandstones, siltstones, claystones and conglomeartes are the main lithologies of these

rocks; calcrete nodules and silcretes are also present in claystones but salts and gypsum are found

only in the Maha Sarakham Formation. The rocks are interpreted as having been deposited by the

meandering and braided rivers in semi-arid to arid conditions. Age determinations are based mainly

on vertebrates, bivalves and palynomorphs indicating that the rocks are reassigned to the late Upper

Triassic to Upper Cretaceous-Lower Tertiary. In the southern peninsula, the non-marine rocks consist

of reddished brown claystones, siltstones, sandstones, and conglomerates. These rocks are

interpreted to be deposited by both meandering rivers and alluvial fans. The small outcrops of the

non-marine rocks other than the northeastern and southern parts are also noted.

Cenozoic

Tertiary

Tertiary intermontane and rift basins in Thailand share some similarities in origin, timing,

sedimentary environments, and basin structural styles. These similarities corresponded with

northward movement of the India terrane. Those basins in the south formed relatively earlier than in

the north, and those in the west earlier than in the east. Alluvial environments dominated in the lower

and upper parts of the basin, while lacustrine, fluvio-lacustrine and swamp environments were

predominant in the middle part. They contain major deposits of petroleum, coal, oil shale, diatomite

and ball clay of the country.


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Tertiary map of Thailand

Tertiary sedimentary basins in Thailand occurred throughout the country as intermontane and

rift basins, except the Khorat plateau, with long axis of the basins normally oriented in N-S directionthat were related to the collision of India with Asia. Most of them show graben and half-graben

geometry. At present, at least 70 Tertiary basins have been named with most of large basins also

contain numbers of sub-basins. These Tertiary rocks are poorly exposed in natural outcrop and

covered by Quaternary sediments except in the margin of the basin where the rocks were often

brought to the surface by faults. As a result of post- as well as syndepositional faults, the present

Tertiary configuration is a remnant of an original larger basin that was uplifted and eroded.

Study of these rocks in the past was quite difficult due to scare published papers and most of

subsurface data are confidential. It is realized that these rocks are so important not only as source

rocks and reservoirs of oil and gas, but also accumulation of coal, oil shale, diatomite and ball clay.Mining activities were performed in several basins i.e. coal of mainly lignite and sub-bituminous ranks


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from Mae Moh, Mae Than, Chiang Muan, Bo Luang, Li, Nong Ya Plong, and Krabi basins with

prospective reserves in number of basins such as Wiang Haeng, Ngao, Wang Nua, Chae Khon,

Mae Ramat, Mae Lamao, Khian Sa, Saba Yoi; petroleum from Phitsanulok, Supan Buri, Fang, and

basins in the Gulf of Thailand; ball clay in association with coal from Mae Than basin; diatomite from

Mae Tha sub-basin of Lampang basin. Huge oil shale deposit was found in Mae Sot basin.

Quaternary

Quaternary geology is the study of all geological events that took place in Quaternary period.

This period subdivided into 2 epoches, Pleistocene (1.8 m.y.-10,000 yr.B.P) and Holocene (10,000

yr.B.P-present). Quaternary is a period concerning with climatic change, sea-level change, and

changing landforms. Migration of lives on the earth surface, and human evolution also taken in this

period.

Quaternary geologic sequences of Thailand cover one-third of the total area. They are

mainly semiconsolidated and unconsolidatd sediments, including some quick crystalline and lithified

volcanic rocks such as basalt. Formerly, Quaternary sediments were poorly understood because of

unexposures, thick accumulation of unconsolidated sediments and inaccessibility of subsurface data.

The classification of Quaternary sediments in Thailand is based on geomorphology, lithology,

depositional environments and fossils. Generally, Pleistocene deposits are related to neo-tectonics,

changing of alluvial and fluvial systems, weathering in-place of the bed rocks, and evidences of sea-

level change in restrictive areas. Appositionally, Holocene deposits are concern mainly with climatic

changes and marine sediments relating to the great fluctuation of sea level. The present coastal

area of Thailand was derived by inundation of Holocene sea- level. While in the upland area floodplain, levee, and young alluvial fan were developed.

Quaternary stratigraphy of Thailand is differed in each physiographic region. The result ofstudy is advantage in Holocene marine deposits and coastal zone studied while in the upland area,the Pliestocene deposits are almost concealed. The stratigraphic succession has been acquired fromsubsurface data, quarries, and road cut sections. Inaccessibility of data in many areas causeddifficulty in stratigraphic correlation among physioraphic regions, and it must be solved with therevealed data of future geological research.

IGNEOUS ROCKS

Igneous rocks are widespread in Thailand. Among them, granites are the most common

constituents whereas, intrusive rocks of intermediate, mafic, ultramafic composition and volcanic

rocks are subordinate. The Thai granites were lineated in three major belts, from east to west, the

Eastern Belt Granites (EBG), The Central Belt Granites (CBG) and the Western Belt Granites (WBG).

The EBG show strong correlation with the I-Type granites or Magnetite Series whereas, the CBG show

S-type or Ilmenite Series affinities. Majority of the WBG are S-Type with minor amounts of the I-Type

or Ilmenite Series granites. Emplacement ages of these granites, in a broad sense, appear to

decrease westward from Lower Triassic in the east to Late Cretaceous in the west. Widespread

discordant isotopic ages in these granites are observed and considered to be subjected to a number

of causes, such as metamorphism, tectonic deformation, hydrothermal activities and simple cooling

processes. Gold, copper, base metals, iron and barite are common economic minerals occurred in the


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EBG whereas, tin, tungsten, and fluorite are more common in the CBG and tin, tungsten, columbite,

tantalite and REE minerals are much more abundant in the WBG granites.

Igneous distribution pattern of the Thai Granites with a three

granites provinces in Thailand

Gabbro, peridotite, pyroxenite, hornblendite, and serpentinite are common intrusive mafic

and ultramafic assemblages and were interpreted as ophiolite suite. They expose as three

discontinuous narrow stripes from north to south, the Pha Som Ultramafic (Nan-Uttaradit), Sra Kaeo

Ultramafic and Narathiwat Ultramafic. The maficultramafic belt is considered to be a palaeo-suture,

separating the Shan Thai Block in the west from the Indochina Block in the east part of the country.

Age of the Pha Som Ultramafic have been reported as Early Permian (269_12 Ma) and Carboniferous

to Early Permian (356-256 Ma).


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Volcanic rock assemblages are widely distributed in most parts of Thailand and can be

broadly grouped into the Permo-Triassic, Chiang Mai-Chiang Rai Volcanic Belt, the Permo-Triassic to

Jurassic with some minor Late Tertiary Ko Chang-Tak-Chiang Khong Volcanic Belt, and the Late

Cenozoic Basalt.

Economic mineral deposits within the early two volcanic groups comprise gold, copper,

manganese, iron and barite, bentonite, dickite, Kaolinite and perlite. In contrast, some Late Cenozoic

Basalt carried gemstone in particular, ruby and sapphires.

METAMORPHIC ROCKS

Metamorphic rocks in Thailand have been provisionally subdivided into four belts, arcuatedly

elongated in a north-south direction, and roughly corresponded with the known litho tectonostratigraphic

belts. Starting from west to east, the western most belt-A, where, the metamorphic rocks of the belt

possess a continuous sequence, in terms of both stratigraphy and grades of metamorphism, from

inferred Precambrian to probably Middle or Upper Paleozoic rocks. They were metamorphosed in the

Abukuma Facies Series, producing Amphibolite in the inferred Precambrian rocks and graded to Upper

Greenschist the Lower Paleozoic rocks. It is still debatable to how and when this metamorphism was

generated.


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Belts of metamorphic rocks in Thailand

The second and third metamorphic belts (B and C) are more geochronologically diverse,however, either of them tends to be restricted more or less in a similar lithologic provinces. The

second belt-B represents the first eastward appearing of the volcanogenic metamorphic rocks. They

are calc-alkali and apparently were metamorphosed in the high temperature-low pressure regime.

Their distributions are rather patchy and localized, forming a longitudinally disconnected or

terminated volcanogenic chains. Transition sideward across the stratigraphic column seems

gradational to unmetamorphosed rocks. The rock sequences vary in ages from Silurian/Devonian,

Carboniferous, Permian and Triassic and are younging eastward to the margin of the belt, the Nan

Suture. These metavolcanogenic rocks indicate eastward reappearance during their formations and is

related to the westward accretion along the Nan Suture.


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The third belt -C lies roughly coincide with the Nan palaeo-suture zone. The metamorphic

rocks in this belt are probably subduction related and consist of metamafic to acid volcanic rocks

characterizing by a lesser evolved material. Imprint of the IP/IT Greenschist Faciess over the HP/LT

Blueschist Facies in Nan may connote other unknown tectonic movement rather than ordinary

adjustment of the PT regime by uplifting. The IP/IT Greenschist to Ampholite Facies in eastern part of

Thailand reflects a different PT condition. Age differences between the Early Carboniferous in Nan

and the Devonian-Carboniferous in east Thailand may suggest their differences in subduction

regimes.

The fourth metamorphic belt-D is isolated and limited in extense lying in a north-south

elongation in the northern end of the Khorat Plateau. The rocks were weakly metamorphosed and are

the only metamorphic chain in this region. They represent a unit in a thick and continuous sequence

ranging in age from Silurian to Upper Devonian and probably related to the western subduction

regime under the Indochina block.

TECTONIC EVOLUTION

Thailand, tectonically consists of two major Gondwana derived terranes, namely Shan-Thai

to the west, and Indochina to the east, that were amalgamated along Nan-Uttaradit suture during

Late Triassic, although opinions on moving history vary. Different in their stratigraphies, particularly

during Carboniferous to Triassic, strongly supported this interpretation. Indochina terrane drifted

away from the Gondwana in Late Devonian, as suggested by radiolarian assemblages from chert in

the suture zone. These were continuously followed by Carboniferous clastics and Permian platform

carbonates exhibited Cathaysian affinity. While Shan-Thai terrane was adjacent to NW Australian part

of the Gondwana till Early Permian, as evidenced by not only stratigraphic similarity from Cambrian toEarly Permian but also close faunal affinities in particular during Cambrian to Devonian. Discovery of

Devonian to Middle Triassic deep sea thin-bedded chert, and Cathaysian fauna in Carboniferous to

Permian limestones in northern Thailand where formerly mapped as part of the Shan-Thai terrane,

led to interpretation of major Paleotethys ocean with occurrence of seamount limestones in low

latitude area. Occurrences of Lower Paleozoic clastics and fauna in the northern Thailand similar to

those of Shan-Thai terrane suggest they were also derived-fragments of the Gondwana.

Subsequently, new suture zones of the Paleotethys have also been proposed in Chiang Mai and Mae

Sariang areas. However, westward subduction of the Indochina terrane beneath the Shan-Thai

terrane along the Nan-Uttaradit suture is preferred. This interpretation is strongly supported not only

by the presence of magmatic arc, Permian to Middle Triassic deep sea thin-bedded chert, Triassicforearc sediments and ophiolite rocks but also occurrences of syn- and post-subduction related

plutonics.


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Map showing distribution of continental terranes in Thailand and adjacent areas

Precambrian rocks have been mapped with regard to their degree of high grade

metamorphism. Sedimentary protolith from paragneiss was dated as around 600 ma. This was

challenged by metamorphic core complex model that indicated the protoliths of orthogneiss were Late

Triassic-Early Jurassic granites, experienced low pressure metamorphism and migmatitization in Late

Cretaceous and Early Miocene. In the Shan-Thai, Upper Cambrian shallow marine siliciclastics with

Trilobite cropped out only at Tarutao island, next to Malaysian border, whereas on the mainland

consists mainly of quartzite. They were conformably overlain by Ordovician shallow marine

carbonates and Silurian-Devonian fine-grained sediments with graptolite and tentaculite. Only in the


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southern peninsula, there were overlain conformably by Lower Carboniferous fine-grained sediments

containing Posidonomya sp. Stratigraphic break or hiatus occurred widely on the Shan-Thai terrane

during Late Carboniferous. Lower Permian glacial marine sediments cropped out mainly in the

Peninsula, particularly the western part that could be traced northward to Burma and southwestern

China, and southward to Malaysia and Sumatra. Depositional environment gradually changed to

carbonate platform during Middle to Upper Permian. Faunal evidences indicated that during Middle

Permian, the Shan-Thai terrane moved northward to a warm-temperate area between Gondwana and

Cathaysia. During Late Permian, it still remained at a distance from the Indochina terrane, as

suggested by faunal differences such as Shanita and fusulinadean. In the northeastern Thailand,

hiatus occurred extensively during Early to Middle Triassic. By the Late Triassic, extensional basins

were formed, and followed by a thermal subsidence that resulted in the continental deposition of

Jurassic-Cretaceous red beds.

Effect of continental collision between the Shan-Thai, then as a part of the Eurasia, and

Western Burma terrane along the Shan Boundary during Cretaceous, and later during Tertiary from

India and Eurasia that created huge Himalayan mountain belt, had greatly enhanced the complexity

of geological structures in this region, in particular northern Thailand. As a result, oroclinal Sshaped

structural trends and clockwise rotation of NE Thailand caused by crustal movement was created prior

to wide development of extensional Tertiary basins in the region.

Granites in Thailand occurred in three north-south belts. The Eastern belt contains small

batholiths of I-type Triassic granites. The Central belt consists of major batholiths showing S-type

Triassic granites. The Western belt contained mixed population of S-type and I-type Cretaceous

granites.

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Geology of Thailand