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Late Permian and Early to Middle Triassic radiolarians from the Hat Yai area,southern peninsular Thailand: Implications for the tectonic setting of theeastern margin of the Sibumasu Continental Block and closure timing of thePaleo-Tethys
Yoshihito Kamata, Akane Shirouzu, Katsumi Ueno, Apsorn Sardsud,Thasinee Chareontitirat, Punya Charusiri, Toshio Koike, Ken-ichiro Hisada
PII: S0377-8398(13)00101-1DOI: doi: 10.1016/j.marmicro.2013.07.006Reference: MARMIC 1489
To appear in: Marine Micropaleontology
Received date: 8 November 2012Revised date: 8 July 2013Accepted date: 18 July 2013
Please cite this article as: Kamata, Yoshihito, Shirouzu, Akane, Ueno, Katsumi, Sardsud,Apsorn, Chareontitirat, Thasinee, Charusiri, Punya, Koike, Toshio, Hisada, Ken-ichiro,Late Permian and Early to Middle Triassic radiolarians from the Hat Yai area, southernpeninsular Thailand: Implications for the tectonic setting of the eastern margin of theSibumasu Continental Block and closure timing of the Paleo-Tethys, Marine Micropale-ontology (2013), doi: 10.1016/j.marmicro.2013.07.006
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Late Permian and Early to Middle Triassic radiolarians from the Hat Yai area, southern peninsular
Thailand: Implications for the tectonic setting of the eastern margin of the Sibumasu Continental
Block and closure timing of the Paleo-Tethys.
Yoshihito Kamata1, Akane Shirouzu2, Katsumi Ueno3, Apsorn Sardsud4,
Thasinee Chareontitirat5, Punya Charusiri5, Toshio Koike6 and Ken-ichiro Hisada1
1. Graduate School of Life and Environmental Sciences, University of Tsukuba, Tennodai 1-1-1,
Tsukuba, Ibaraki 305-8572, Japan
2. Department of Earth Sciences, Graduate School of Science & Engineering, Yamaguchi University,
Yamaguchi, 753-8512, Japan
3. Department of Earth System Science, Fukuoka University, Fukuoka 814-0180, Japan
4. Bureau of Fossil Research and Geological Museum, Department of Mineral Resources, Bangkok
10400, Thailand
5. Department of Geology, Faculty of Science, Chulalongkorn University, Bangkok 10330, Thailand
6. Tokiwadai 36-6-606, Hodogaya-ku, Yokohama, Kanagawa Prefecture 240-0067, Japan.
Corresponding author
Yoshihito Kamata
Graduate School of Life and Environmental Sciences, University of Tsukuba, Tennodai 1-1-1,
Tsukuba, Ibaraki 305-8572, Japan
TEL:+81-29-853-4302, FAX:+81-29-853-7887
E-mail:[email protected]
Keywords
Radiolarian, Paleo-Tethys, Sibumasu, Indochina, Peninsular Thailand, Permian, Triassic.
Abstract
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The fine clastic and siliceous sedimentary successions distributed in the Hat Yai area, southeastern
peninsular Thailand, was examined using radiolarian biostratigraphy, lithology, and stratigraphy.
The studied succession was essentially divided into two kinds of fine-grained sedimentary rock
units: the lower shale unit and the upper chert unit. The lower shale unit and the upper chert unit
yielded late Middle to early Late Permian and Early to Middle Triassic radiolarians, respectively.
We clarified that the sedimentary rocks distributed in the study area are not entirely Carboniferous,
but contain some sediments from the Permian and Triassic. This age determination suggests that the
clastic-chert succession distributed in the study area should be distinguished from the Carboniferous
Yaha Formation and correlated with the Permian to Triassic Semanggol Formation. Lithological
change with increasing siliceous composition was observed in the uppermost part of the lower shale
unit, and the geological age based on the radiolarians indicates a nearly conformable stratigraphic
relationship for the lower shale unit and the upper chert unit. The stratigraphy and lithology of the
Permian to Triassic succession in the study area, together with geological correlation around
southernmost Thailand and northern Malaysia, suggest that the Triassic chert should be interpreted
as continental slope sediments overlying Permian clastic and/or calcareous facies, rather than typical
pelagic deep-water sediments formed on an abyssal plain. The depositional environment of the chert
in this area was likely restricted to the vicinity of a continental slope. Considering with the wide
distribution of Triassic platform carbonates over southeastern peninsular Thailand, the continental
margin of the Sibumasu along the Paleo-Tethys was represented by a stable passive margin during
the Middle-early Late Triassic time. On the basis of the sedimentary setting and stratigraphy in the
Permian and Triassic, it is suggested that the closure of the Paleo-Tethys between the Sibumasu and
Indochina continental blocks took place at least after the Middle Triassic in southeastern peninsular
Thailand.
1. Introduction
In order to understand the geotectonic history of Thailand, several models of tectonic subdivisions
have been proposed (e.g. Bunopas, 1981; Metcalfe, 1988, 1999; Barr and Macdonald, 1991; Ueno,
1999, 2002; Charusiri et al., 2002; Sone and Metcalfe, 2008; Ueno and Charoentitirat, 2011) based
on Paleozoic and Mesozoic stratigraphy and micropaleontology, represented by foraminiferal and
radiolarian biostratigraphy, paleobiogeography, the tectonic settings of granitoids, ultramafic rocks
indicative of suture lines, and paleomagnetic data (Fig. 1A). These geotectonic interpretations and
tectonic subdivisions in mainland Thailand have been refined by studies from northern Thailand,
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where Paleozoic to Mesozoic basement rocks of the Sibumasu Continental Block and oceanic rocks,
such as radiolarian bedded chert and seamount-type carbonate rocks, are widely distributed.
The geological map produced by the Department of Mineral Resources (DMR) of Thailand
indicates that peninsular Thailand, which is south of the Three Pagodas Fault Zone, is occupied by
Pre-Cambrian and Paleozoic to Mesozoic basement rocks. Furthermore, most of the peninsula lies
within the Sibumasu Continental Block, except for the southeastern tip east of the Benton-Raub
Suture that is the boundary between the Sibumasu and Indochina continental blocks (Fig. 1B).
Recently, Paleozoic strata in peninsular Thailand were well documented and summarized by Hansen
and Wemmer (2011), Ridd (2009, 2011), and Ueno and Charoentitirat (2011). According to these
studies, Carboniferous-Permian strata are widely distributed in the upper peninsula, which is north
and west of the Khlong Marui Fault, but are less widespread in the lower peninsula southeast of the
Khlong Marui Fault (Fig. 1B). The stratigraphy, lithology, and sedimentary environments of the
Carboniferous-Permian Khuan Klang Formation, Kaeng Krachan Group, and Permian Ratburi
Limestone were documented and discussed in these studies. These Carboniferous-Permian
successions possess gross tectono-stratigraphic and faunal similarities to the basins of NW Australia
and strongly suggest that the origin of the Sibumasu block was off the northwestern Australian
continental margin of Gondwanaland (e.g., Metcalfe, 1988; Ridd, 2009). They have also discussed
about the sedimentary environments of the Paleozoic sediments. For example, the Kaeng Krachan
Group represents rift-filling sediments under a developing extensional fault system during the
separation of Sibumasu from Gondwana (Ridd, 2009, 2011), and the Ratburi Limestone was
ubiquitously deposited on the Sibumasu block to form a wide carbonate platform in the late Early to
Late Permian (Ueno and Charoentitirat, 2011).
In contrast, geological information (e.g. stratigraphy and lithology) is scarce regarding the relatively
deeper fine clastic and siliceous rocks that are mainly distributed in the southeastern part of the
lower peninsula from Hat Yai in Changwat Songkhla to the Bentong-Raub Suture (Fig. 1B).
Carboniferous, Permian, and Triassic radiolarians were reported from bedded chert and siliceous
rocks (Sashida et al., 2000, 2002; Kamata et al., 2008, 2009); however, the stratigraphy and
depositional environment have not been fully established. In particular, the Triassic succession
distributed in this area is crucial for correlation with the Permo-Triassic Semanggol Formation,
which is widely distributed in northern peninsular Malaysia, and to understand the tectonic setting of
the eastern margin of the Sibumasu Continental Block and the collision and closure time of the
Sibumasu and Indochina continental blocks.
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In the course of mapping the 1:50,000 Hat Yai Quadrangle (Sardsud and Saengsrichan, 2002),
directed by the Geological Survey Division, Department of Mineral Resources (DMR), Thailand,
late Middle Permian and Early to Middle Triassic radiolarians were detected from the fine clastic
(shale) to chert facies distributed in the Hat Yai area, Changwat Songkhla, lower peninsular
Thailand (Fig. 1C). This paper describes the lithology of radiolaria-bearing sedimentary rocks and
age determination by radiolarian fauna. We also discusses the sedimentary environment of
radiolaria-bearing facies, the tectonics of these facies, the tectonic setting of the eastern margin of
the Sibumasu Continental Block, and the closure of the Paleo-Tethys in lower peninsular Thailand.
2. Geological outline of lower peninsular Thailand
According to the DMR geological map, lower peninsular Thailand is widely covered by Quaternary
sediments. Paleozoic-Mesozoic basement rocks in this area are generally concealed by these
younger sediments and crop out only in the form of scattered monadnocks. Carboniferous-Permian
siliciclastic facies of the Yaha Formation, Khuan Klang Formation, and Kaeng Krachan Group and
the Permian Ratburi limestone are broadly scattered in lower peninsular Thailand with Lower
Paleozoic to Devonian sedimentary rocks (Fig. 1B). Among these, the Kaeng Krachan Group (first
introduced as the Kaeng Krachan Formation by Javanaphet, 1969) represents a southeastern
extension of the upper peninsula, which contains rift-filling sediments of a fault system from the
separation of Sibumasu from Gondwana (Ridd, 2009, 2011). This group consists of various
siliciclastics and is characterized by common intervals of diamictite (pebbly mudstone) with
dropstones and dump structures in mudstone facies, indicating a glacially influenced environment.
The Ratburi Formation, which Bunopas (1981) restricted to Permian carbonates in western and
peninsular Thailand, was originally introduced by Brown et al. (1951) and consists mainly of
massive to bedded limestone. Limestone in this group is mainly distributed in the northwestern part
of lower peninsular Thailand around the Changwat Krabi and Surat Thai areas. In southeastern
lower peninsular Thailand, equivalents of the Ratburi Limestone only have a small distribution in
southern Changwat Yala (Fig. 1B). The Yaha Formation, introduced by Muenlek et al. (1985) for
the Carboniferous succession distributed in the easternmost area of the lower peninsula, consists
mainly of siliciclastic shale, medium- to coarse-grained sandstone, siliceous shale, chert, and
conglomerates. The depositional age of the formation is substantiated by the occurrence of a late
Tournaisian conodont from a chert and siliceous shale succession at Ko Yo in Songkhla Province
(Igo, 1973). Although Muenlek et al. (1985) correlated the Yaha Formation with the upper part of
the Kaeng Krachan Group, the lithostratigraphy and geological age of the formation are very
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controversial. According to the DMR map (1999), studied succession in this study is assigned to the
Yaha Formation (Fig. 1C).
As pointed out by Ridd (2009), the Carboniferous-Permian Kaeng Krachan Formation, partly
represented by a glacially influenced facies, is not recognized east of Hat Yai (study area in this
paper) in Songkhla Province. East of the Hat Yai area, some radiolarian occurrences were reported.
An Early Carboniferous (Tournaisian) fauna was reported from Na Thawi in Songkhla Province
(Sashida et al., 2000) and the Saba Yoi-Kabang area near the Songkhla-Yala provincial boundary
(Sashida et al., 2002). The exposed succession in the latter study was assigned to the Yala Formation
based on the DMR map (1999). Late Permian and Middle Triassic radiolarians have also been
reported from two areas that were mapped as the Yaha Formation by the DMR (1999): the Chana
area (Sashida et al. 2000) and the Rattaphum area (Sardsud and Saengsrichan, 2002; Kamata et al.
2008, 2009), both in Songkhla Province.
It should be noted that the Permo-Triassic calcareous and siliciclastic-siliceous succession is
distributed both in southeastern peninsular Thailand and northern peninsular Malaysia. The Permian
to Triassic platform-type limestone successions include the Chuping and Kodiang Limestones
(Perlis Province, northern Malaysia), the Khlong Kon Limestone (Saba Yoi, western Songkhla
Province), and the Chaiburi Formation (Rattaphun, northwest Songkhla Province). The Chuping and
Kodiang limestones have been studied using conodont biostratigraphy and found to range from the
Late Permian to Late Triassic in age (Koike, 1973, 1982; Metcalfe, 1981, 1990, 1992). Late Triassic
(late Carnian to middle Norian) radiolarians have also been obtained from the Kodiang limestone
(Basir et al., 1995). The Khlong Kon limestone yielded Middle to Late Triassic foraminiferous fauna
(Sashida et al., 1999). The Chaiburi Formation ranges from the Early to Late Triassic in age based
on conodonts (Ampornmaha, 1995) and radiolarians (Sashida and Igo, 1992). The Permian to
Triassic siliciclastic-siliceous succession is distributed across the border with the Semanggol
Formation in Kedah Province in northern Malaysia, the Na Thawi Formation in Saba Yoi in western
Songkhla Province, and a chert succession with fine clastics in Hat Yai in Songkhla Province (this
study). The Semanggol Formation is subdivided into three members: lower chert, middle rhythmite,
and upper conglomerate (Burton, 1973). Middle and Late Permian radiolarians were reported from
the lower member (Sashida et al., 1995). The middle member consists of rhythmically intercalated
beds of sandstone and shale and has been correlated with the Halobia-Daonella facies yielding
Triassic pelecypods (Kobayashi, 1963). The occurrence of late Early Permian to Middle Triassic
radiolarians from the lower chert member was also reported (Basir, 1997; Basir and Zaiton, 2007).
In the Na Thawi and Saba Yoi areas in western Songkhla Province, Early Triassic and Middle
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Triassic radiolarians were reported from siliceous shale and bedded chert (Sashida et al., 2002).
Sashida et al. (1999, 2000) summarized the sedimentary environments of the above-mentioned
limestone-clastic-siliceous rock association, which resulted from a change from shallow to deep
environments in the Sibumasu margin.
3. Lithology of the study sections
The study sections are located about 20 km west of Hat Yai town in Changwat Songkhla, lower
peninsular Thailand (Fig. 1C) and contain various kinds of clastic rocks consisting of sandstone,
shale, siltstone, well-bedded siliceous shale, and bedded chert. These sedimentary rocks have
broadly northward to northwestward strikes and dip to the east at various angles. The clastic and
siliceous sediments were assigned to the Yaha Formation of Carboniferous age without the
occurrence of good index fossils in previous geological maps (DMR, 1999).
The rocks of the six studied sections (HY-01, HY-02, HY-03, HY-04, HY-05, and HY-21) were
essentially divided into two fine-grained sedimentary rock units: the lower shale unit and upper
bedded-chert unit (Fig. 2).
The lower unit consists the alternation of yellowish-brown silty shale, brown shale, and black or
brown shale with calcareous nodules. The yellowish-brown, silty shale is about 10 cm to 30 cm in
thickness and shows several kinds of sedimentary structures, such as parallel and crossed lamination
(Fig. 3A). Some layers of the silty shale contain many calcareous bioclasts, such as foraminiferal
tests (Fig. 3B). The dark-colored and black shale with calcareous nodules is probably equivalent
stratigraphically to the Permian ammonoid-bearing shale reported by Fujikawa et al. (2005) from the
Phatthalung-Hat Yai area. It is important to note that the uppermost part of the shale succession
becomes more siliceous and often contains intercalated chert layers that are very similar in lithology
to those in the upper bedded chert unit (Fig. 2).
The bedded chert in the upper unit is composed of with generally 2–10-cm-thick chert beds
alternating with claystone a few millimeters thick (Fig. 3C). It is brown or milky white and is less
glassy and transparent than typical pelagic chert, such as the Paleo-Tethyan Fang Chert in northern
Thailand (Kamata et al., 2009). The polished surface of a chert slab shows distinct laminations (Fig.
3D). Petrographically, the matrix consists of clay minerals with microcrystalline quartz and contains
extremely fine, opaque organic matter (Figs. 3E and 3F). Radiolarians, which are scattered
throughout the matrix (Fig. 3E), are considerably less densely distributed than in typical pelagic
chert. The studied bedded chert contains not only siliceous organisms, such as radiolarians and
sponge spicules, but also calcareous biota, such as foraminifers, ostracods, and thin-shelled bivalves
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(Figs. 3G and 3H). This fossil content is also quite different from that of typical pelagic chert.
4. Radiolarians and age determination
Radiolarians of the late Middle Permian were obtained from one horizon (HY05-04 in Fig. 2, and
Table 1) of slightly silicified shale from the middle part of the lower shale unit. The upper chert unit
contains moderately to well-preserved Early to Middle Triassic radiolarians and these are divided
into five assemblages (Fig. 2, Plates 1–4, and Table 1).
Permian radiolarian zonations have been established by biostratigraphic examination of the
European Tethys (e.g. Kozur and Mostler, 1989), North America (Blome and Reed, 1992), China
(Wang et al. 1994), and SW Japan (Ishiga, 1986, 1990; Kuwahara et al., 1998, 1999). Additionally,
Triassic radiolarians had done the first systematic description by Nakaseko and Nishimura (1979),
and their zonation have been proposed by Yao (1982), Yoshida (1986), Carter (1993), Bragin (1991),
Kozur and Mostler (1994, 1996), and Sugiyama (1992, 1997). Recently, O’Dogherty et al. (2009)
reviewed Triassic radiolarian genera and later cataloged their stratigraphic ranges (O’Dogherty et al.,
2011). Early to Middle Triassic radiolarian biostratigraphy is well established by reports mainly
from SW Japan (e.g. Sashida, 1983, 1991; Kamata, 1995, 1999; Sugiyama, 1992, 1997; Kusunoki
and Imoto, 1996), Thailand (Sashida and Igo, 1992), Turkey (Kozur et al. 1996), and New Zealand
in the Southern Hemisphere (e.g. Takemura et al. 2007; Kamata et al. 2007; Yamakita et al. 2007).
The age determination of radiolarians from the study section referred to the above-mentioned
biostratigraphic studies.
4-1. Permian radiolarians
A monotonous radiolarian fauna was obtained from a horizon in the middle part of the lower shale
unit. This fauna consists of several specimens of Follicucullus scholasticus Ormiston and Babcock.
Follicucullus scholasticus was first described by Ormiston and Babcok (1979) from Guadalupian
rocks in west Texas, USA, and is well known as a species with worldwide occurrence. This species
is the representative species of the F. scholasticus zone (Ishiga, 1986, 1990) and ranges to the lower
part of the Neoalbaillella ornithoformis zone (upper Capitanian to Wuchiapingian) (Ishiga, 1990;
Kuwahara et al. 1998). In Thailand, the occurrence of F. scholasticus has been reported from eastern
Thailand (Sashida and Igo, 1999), northern Thailand (e.g. Caridroit, 1993; Kamata et al., 2012), and
northwestern Thailand (Wonganan and Caridroit, 2006). Sashida and Igo (1999) assigned the F.
scholasticus assemblage to the late Middle to earliest Late Permian (Capitanian to Wuchiapingian).
The present fauna is not directly correlated with the F. scholasticus zone (Ishiga, 1990) or F.
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scholasticus assemblage (Sashida and Igo, 1999) because of its monotonous faunal content.
However, the biostratigraphic range of this species suggests that the present fauna could correspond
to part of the late Middle to early Late Permian (Capitanian to Wuchiapingian).
4-2. Early to Middle Triassic radiolarians
The upper chert unit yielded Early to Middle Triassic radiolarians from 49 horizons (Plates 1–4,
Table 1). These radiolarians are divided into five assemblages (Fig. 2). Representative radiolarians
of the assemblages are as follows:
Assemblage 1: This assemblage is characterized by the occurrence of Follicucullus scholasticus
Ormiston and Babcock associated with poorly preserved bi-polar specimens of Spumellaria and
spherical radiolarians. Follicucullus is a representative genus of the Middle to Late Permian;
however, some occurrences in the Lower Triassic succession have been reported by Sugiyama (1992,
1997), Bragin (1991), and Takemura et al. (2007). Considering the coexistence of bi-polar
Spumellaria, which are similar to those of the Lower Triassic, particularly the late Olenekian
(Spathian) succession, as well as the absence of Permian-type Entactinarians and Latentifistularians
this fauna resembles that of TR0 and TR1 of the late Olenekian (Spathian) (Sugiyama, 1997). The
present fauna does not contain the common spicule-type genera Parentactinia and Archeosemantis
of TR0 and TR1, but it is here tentatively and roughly correlated to TR0 and TR1.
Assemblage 2: This assemblage is characterized by the common occurrence of Entactinia cf.
reticulata Sashida and Tonishi, Entactinosphaera chiakensis Sashida and Igo, Pantanellium sp.,
Acaeniospongus ? sp., Parasepsagon tetracanthus Dumitrica, Kozur and Mostler, Plafkerium sp.,
Tiborella sp., Eptingium nakasekoi Kozur and Mostler, and E. manfredi Dumitrica. This assemblage
also contains small amounts of the segmented Nassellaria, Hozmadia gifuensis Sugiyama, H.
reticulata Dumitrica, Kozur and Mostler, Anisicyrtis sp., and Spongosilicarmiger sp. Species
belonging to Entactinaria, Eptingium, Pantanellium, and Hozmadia are diagnostic of the upper part
of the Hozmadia gifuensis assemblage (Sugiyama, 1992) and TR2A (Sugiyama, 1997).
Entactinosphaera chakensis is reported from the latest Olenekian to early Anisian (latest Spathian to
early Anisian) bedded limestone at Phattalung, southern peninsular Thailand, which is 70 km
northwest of the study section (Sashida and Igo, 1992). The first occurrence of E. nakasekoi defines
the base of TR2A, and the present fauna is similar to that of TR2A. Considering the lack of
multisegmented nassellaria of the genus Triassocampe, this assemblage should be correlated to
TR2A.
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Assemblage 3: This assemblage is characterized by the abundant occurrence of Triassocampe and
collateral occurrence of Eptingium and Pseudostylosphaera. Triassocampe coronata Bragin,
Triassocampe sp., Eptingium manfredi Dumitrica, E. nakasekoi Kozur and Mostler,
Pseudostylosphaera japonica (Nakseko and Nishimura), Cryptostephanidium sp., Parasepsagon sp.,
and Pentactinocarpus sp. were also obtained and this faunal content resembles that of TR2B, of
which the base is defined by the first occurrence of T. coronata and Pseudostylosphaera japonica.
Assemblage 4: Diagnostic species in this assemblage are Pseudostylosphaera japonica (Nakaseko
and Nishimura), P. spinulosa (Nakaseko and Nishimura), Triassocampe deweveri (Nakaseko and
Nishimura), T. coronata Bragin, and Cryptostephanidium cornigerum Dumitrica et al. This fauna is
characterized by the occurrence of T. deweveri and the abundant and diverse genus
Pseudostylosphaera. This fauna resembles TR2C, of which the base is defined by the first
occurrence of T. deweveri.
Assemblage 5: This assemblage contains Triassocampe deweveri (Nakaseko and Nishimura), T.
campanilis (Kozur and Mostler), Pseudostylosphaera japonica (Nakaseko and Nishimura), P.
spinulosa (Nakaseko and Nishimura), Cryptostephanidium cornigerum Dumitrica, and Spine A2 of
Sugiyama (1997). This fauna resembles that of Assemblage 4 but is distinguished by the occurrence
of Spine A2. The first occurrence of Spine A2 defines the base of zone TR3A of Sugiyama (1997).
On the basis of the faunal similarity and the occurrence of Spine A2, the present fauna can be
correlated with TR3A.
In summary, five assemblages (1 to 5) from the upper chert unit in this study correspond to TR0 or
TR1, TR2A, TR2B, TR2C, and TR3 of Sugiyama (1997), respectively, indicating that the unit is
Early to Middle Triassic, late Olenekian (late Spathian) to Anisian in age.
5. Discussion
5.1 Stratigraphy
The sedimentary succession examined in this study had been assigned to the Carboniferous Yaha
Formation (DMR, 1999). However, radiolarian biostratigraphy has clarified that the age of the fine
clastic and siliceous sedimentary rocks distributed in the Hat Yai area are not entirely Carboniferous,
but some part is Permian and Triassic age. The geological age of the Yaha Formation was
substantiated by the occurrence of late Mississippian conodonts from a chert and siliceous
succession at Ko Yo in Songkhla Province (Igo, 1973). The occurrence of Permian and Triassic
radiolarians from study sections indicates that the siliceous succession in the Hat Yai area should be
distinguished from the Carboniferous Yaha Formation.
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According to Igo (1973), conodont-bearing Carboniferous chert overlies fissile shale and underlies
bedded coarse-grained quartzitic sandstone. In addition to conodonts, Carboniferous radiolarians
were reported from a similar succession from Songkhla (Sashida et al., 2002). The
radiolarian-bearing bedded chert conformably overlies thick-bedded sandstone layers in the Kabang
area, Songkhla (Sashida et al., 2002). The stratigraphic units of the Yaha Formation should be
restricted to the Carboniferous sequence consisting of chert (siliceous shale) and coarse-grained
quartzitic sandstone because the lithic features of the study sections are very different from these
Carboniferous successions. Sashida et al. (2000) reported the occurrence of Mississippian
radiolarians from siliceous shale blocks within strongly sheared alternating beds of sandstone and
shale in Na Thawi, Songkhla Province. As already pointed out by Sashida et al. (2000), the
radiolaria-bearing siliceous shale blocks were thought to be derived from an equivalent of the Yaha
Formation, and the texture of the blocks within the sheared beds could be due to sedimentary or
tectonic mélange-forming processes related to Paleo-Tethyan subduction and the following collision
of the continents.
As mentioned above in the lithologic section, the uppermost part of the shale succession becomes
more siliceous and often contains intercalated chert layers that are very similar in lithology to those
in the bedded chert unit (Fig. 2). Although fossil evidence for the uppermost Permian and lowest
Triassic ages has yet to be obtained from the study sections, this transitional lithological change in
the upper part of the lower shale unit and the geological age determined by radiolarians indicates
that the upper chert unit (Early to Middle Triassic) was conformably deposited on the lower shale
unit (late Middle Permian).
5.2 Geological correlation
In addition to the study (Hat Yai) area, the southeastern part of peninsular Thailand and northern
Malaysia also contain Permian to Triassic radiolaria-bearing siliceous rocks. The Semanggol
Formation is roughly divided into the lower chert, middle rhythmite, and upper conglomerate
members and is widely distributed in the Perlis and Kedah Provinces of northern Malaysia (Figs. 1B
and 4). The occurrence of Early Permian to Late Triassic radiolarians was reported from both
bedded chert and siliceous limestone (e.g. Sashida et al., 1995; Basir, 1994, 1995; Basir et al., 1995).
Basir (1995) reported the occurrence of Middle Triassic radiolarians from the bedded chert of the
middle member. On the basis of geological age and lithology, the upper chert unit in the study
sections can be correlated with the Middle Triassic chert of the middle member of the Semanggol
Formation (Fig. 4). The middle rhythmite member is represented by bedded chert and intercalated
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sandstone and shale yielding pelecypods. This succession containing pelecypods is equivalent to the
Daonella-Halobia facies (Kobayashi, 1963) and its extension is also recognized in Saba Yoi,
Songkhla between Hat Yai (study area) and Kedah Province, Malaysia (Figs. 2 and 4).
Recently, in Pattalung and Hat Yai northeast of the study area, some karst-forming carbonates were
biostratigraphically examined. These carbonates had been assigned to the Permian Rutburi
limestone (e.g. DMR, 1999). However, conodont, foraminifera, and radiolarian studies have
clarified that the carbonate is not entirely Permian but also partially Early to Late Triassic
(Ampornmaha, 1995; Sashida and Igo, 1992; Ueno et al., 2003). Lithofacies and foraminifera
content of these sediments are correlated with the Khlong Kon Limestone in Saba Yoi and the upper
part of the Chuping Limestone and Kodiang Limestone in peninsular Malaysia (Ueno et al., 2003).
These limestone lithofacies indicate that a large-scale carbonate platform developed in the Permian
to Triassic in this area (Fontaine et al., 1988, 1993; Sashida et al., 1999; Ueno et al., 2003).
The above-mentioned correlation of the facies indicates that three geological units such as a
carbonate platform of Permian to Triassic, a Daonella-Hallovia facies represented by intercalated
fine clastics, and a radiolaria-bearing bedded chert in southernmost Thailand extend to northern
Malaysia (Fig. 4).
6. Tectonic setting and closure time of the Paleo-Tethys in southern peninsular Thailand
In addition to the siliceous fossils of radiolarians and sponge spicules, the Triassic chert in the study
sections contains calcareous foraminiferal tests, ostracods, and planktonic bivalves (Figs. 3E-3H). It
is nearly conformable with the underlying Permian shale unit. This stratigraphic relationship,
together with its fossil contents, suggests that the Triassic chert is not pelagic deep-water sediment
formed on an abyssal plain underlain by oceanic crust consisting of basaltic rocks. Instead, it is
better interpreted as continental slope sediments overlying of Permian clastic and/or calcareous
facies (Fig. 5A). The depositional environment of the chert in this area was likely restricted to the
vicinity of a continental slope and rise (Kamata et al., 2008, 2009).
Taking the wide distributions of Triassic platform carbonates over southern peninsular Thailand
(Ampornmaha 1995; Sashida et al. 1999; Ueno et al. 2003) into account, the continental margin of
the Sibumasu Block along the Paleo-Tethys is represented by a stable passive margin without much
tectonic activity, at least during the Middle-Early Late Triassic (until the Carnian) (Fig. 5A). The
coeval Triassic chert and carbonates are now distributed rather closely in the same area of southern
peninsular Thailand, but their original depositional sites would have been considerably separated
horizontally (~several hundred kilometers). This fact further suggests that considerable crustal
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shortening took place after the deposition of these Triassic sediments (Fig. 5B). This event could be
related to the collision of the Sibumasu and East Malaya (Indochina) blocks and the closure of the
Paleo-Tethys.
On the basis of the sedimentary setting of the chert lithology, faunal content, and stratigraphy with
geological ages based on radiolarians, it is suggested that the closure of the Paleo-Tethys between
the Sibumasu and Indochina blocks took place at least after the Middle Triassic in southern
peninsular Thailand. This timing is very consistent with what has been concluded based on data
from mainland Thailand (e.g. Metcalfe, 2000; Ueno and Hisada, 1999).
7. Conclusion
(1) Fine clastic and siliceous sedimentary rocks distributed in the Hat Yai area, southeastern
peninsular Thailand, have been examined by radiolarian biostratigraphy, lithology, and stratigraphy.
They are divided into two kinds of fine-grained sedimentary rock units: the lower shale unit and the
upper chert unit.
(2) Late Middle to early Late Permian and Early to Middle Triassic radiolarians were identified from
the lower shale unit and the upper chert unit, respectively. This age determination suggests that the
clastic-chert succession in the Hat Yai area should be distinguished from the Carboniferous Yaha
Formation and correlated with the Permo-Triassic Semanggol Formation.
(3) Lithological changes of increasing siliceous composition were observed in the uppermost part of
the lower shale unit, and geological age based on radiolarians indicates a nearly conformable
stratigraphic relationship between the lower shale unit and the upper chert unit.
(4) The lithology and stratigraphy of the Permo-Triassic in the study area, together with geological
correlation around southernmost Thailand and northern Malaysia, suggest that the Triassic chert is
not typical pelagic deep-water sediment formed on an abyssal plain. Instead, it is better interpreted
as continental slope sediments overlying Permian clastic and/or calcareous facies. The depositional
environment of the chert in this area was likely restricted to the vicinity of a continental slope and
rise.
(5) Considering the wide distribution of the Triassic platform carbonates over southern peninsular
Thailand, the continental margin of the Sibumasu Continental Block along the Paleo-Tethys was
represented by a stable passive margin without much tectonic activity, at least during the Middle to
early Late Triassic.
(6) The sedimentary setting and stratigraphy of the Permo-Triassic suggest that the closure of the
Paleo-Tethys between the Sibumasu and Indochina blocks took place at least after the Middle
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Triassic in southern peninsular Thailand.
Acknowledgements
The first author (Y.K.) expresses thanks to the guest editor (Dr. Cortese) and two anonymous
reviewers for their critical review of the manuscript. This work was supported in part by
Grants-in-aid (No. 15403013 and 16740293) from the Japanese Ministry of Education, Culture,
Sports, Science and Technology. This research is part of the IGCP516 and 589 Projects.
References
Ampornmaha, A., 1995. Triassic carbonate rocks in the Phatthalung area, Peninsular Thailand.
Journal of Southeast Asian Earth Sciences, 11, 225-236.
Basir, J., 1994. Middle Triassic radiolaria from the Semanggol Formation, northwest Peninsular
Malaysia. Warta Geologi, 20, 279-283.
Basir, J., 1995. Occurrence of bedded chert radiolarian chert in the Kubang Pasu Formation, north
Kedah, Peninsular Malaysia. Warta, Geologi, 21, 73-79.
Basir, J., 1997. Permo-Triassic radiolaria from Semanggol Formation, NW Peninsular Malaysia.
Journal of Asian Earth Sciences, 15, 327-339.
Basir, J., Che, A. A., Kamal, R. M., 1995. Late Triassic Radiolaria from the Koding Limestoe,
northwest Peninsular Malaysia. Journal Southeast Asian Earth Sciences, 12, 31-39.
Basir, J., Zaiton, 2007. Stratigraphy and sedimentology of the chert unit of the Semanggol
Formation. Geological Society of Malaysia Bulletin, 53, 103-109.
Barr, S.M., Macdonald A. S., 1991. Toward a late Paleozoic-early Mesozoic tectonic model for
Thailand. Journal of Thai Geosciences 1, 11-22.
Blome, C. D., Reed, K. M., 1992. Permian and Early (?) Triassic radiolarian faunas from the
Grindstone terrane, central Oregon. Journal of Paleontology, 66, 351-383.
Bragin, N. J., 1991. Radiolaria and Lower Mosozoic units of USSR east regions. Academy of
Sciences of the USSR, 469, 122p.
Brown, G. F., Buravas, S., Charaljavanaphet, J., Jalichandra, N., Johnston, W. D. Jr., Sresthaputra,
V., Taylor, G. C. Jr. 1951. Geologic reconnaissance of the mineral deposits of Thailand.
United States Geological Survey, Bulletin, 984, 1–183.
Bunopas, S., 1981. Paleogeographic histry of western Thailand and adjacent parts of South-East
Asia. A plate tectonics interpretation. PHD. Thesis, pp. 810. Victoria University of Wellington,
Wellington.
ACC
EPTE
D M
ANU
SCR
IPT
ACCEPTED MANUSCRIPT
14
Burton, C. K., 1973. Mesozoic. In: Gobett, D. J., Hucchison, C. S., (Eds.), Geology of Malay
Peninsula, 97-141. Wiley-Interscience, New York.
Caridroit, M. 1993. Permian radiolaria from NW Thailand. In: Thanasuthipitak, T (ed.),
Proceedings of the International Symposium on Biostratigraphy of Mainland Southeast Asia.
Chiang Mai, 31 January -5 February 1993, Facies & Paleontology, 1, 83-96.
Carter, E. S., 1993. Biochronology and paleontology of uppermost Triassic (Rhetian) radiolarians,
Queen Charlotte Island, British Columbia, Canada. Memoires de Geologie (Lausanne), 11,
175p.
Charusiri, P., Daorerk, V., Archibald, D., Hisada, K., Ampaiwan, T. 2002. Geotectonic evolution of
Thailand: A new synthesis. Journal of the Geological Society of Thailand, 2002, 1–20.
Department of Mineral Resources (DMR). 1999. Geological Map of Thailand, Scale 1:1,000,000.
Geological Survey Division, Department of Mineral Resources, Bangkok.
Fontaine, H., Chonglakmani, C., Piyasin, S., Ibrahim, B., Khoo, H. P., 1993. Triassic limestone
within and around the Gulf of Thailand. Journal of Southeast Asian Earth Sciences, 8,
145-162.
Fontaine, H., Khoo, H. P., Vachard, D., 1988. Discovery of Triassic fossils at Bukit Chuping, in
Gunung Sinyum area, and at Kota Jin, Peninsular Malaysia. Journal of Southeast Asian Earth
Sciences, 2, 145-162.
Fujikawa, M., Ueno, K., Sardsud, A., Saengsrichan, W., Kamata, Y., Hisada, K., 2005. Early
Permian ammonoids from the Kaeng Krachang Group of the Phatthalung-Hat Yai area,
southern peninsular Thailand. Journal of Asian Earth Sciences, 24, 739-752.
Gradstein, F., Ogg, J. and Smith, A., 2004. A geological Time Scale 2004. Cambridge University
Press, Cambridge.
Hansen, B. T., Wemmer, K., 2011. Age and evolution of the basement rocks in Thailand. In: Ridd, M.
F., Barber, A. J., Crow, M.J. (Eds.), The Geology of Thailand, pp. 71-136-28. The Geological
Society of London.
Igo, H., 1973. Lower Carboniferous conodonts from Ko Yo, Songkhla, Peninsular Thailand. Geol.
Pal. Se. Asia, 12, 29-42.
Ishiga, H., 1986. Late Carboniferous and Permian radiolarian biostratigraphy of southwest Japan.
Journal of Geoscience, Osaka City University, 29, 89-100.
Ishiga, H., 1990. Paleozoic radiolarians. In : Ichikawa, K., Mizutani, S., Hara, I., Hada, S., Yao A.,
(Eds.), Pre-Cretaceous terrances of Japan. Nippon Insattsu Shuppan, Osaka. 285-295.
ACC
EPTE
D M
ANU
SCR
IPT
ACCEPTED MANUSCRIPT
15
Javanaphet, J. C. 1969. Geological Map of Thailand, Scale 1:1,000,000. Department of Mineral
Resources, Bangkok.
Kamata, Y., 1995. Early Triassic radiolarians from black siliceous shale and black chert in the Kuzu
area of the Ashio Terrane, central Japan. Paleontological Society of Japan, Kaseki (Fossils), 59,
23-31. (in Japanese with English abstract)
Kamata, Y., 1999. Lower Triassic (Spathian) radiolarians from Kuzu area in the Ashio Terrane.
Geodiversitas, 21, 657-673.
Kamata, Y., Maezawa, A., Hara, H., Ueno, K., Hisada, K., Sardsud, A., Charoentitirat, T., Charusiri,
P., 2012. Basaltic activity preserved in an Upper Permian radiolarian chert from the
Paleo-Tethys in the Inthanon Zone, northern Thailand. Journal of Asian Earth Sciences, 61,
51-61.
Kamata, Y., Matsuo, A., Takemura, A., Yamakita, S., Aita, Y., Sakai, T., Suzuki, N., Hori, R. S.,
2007. Late Induan (Dienerian) primitive nassellarians from Arrow Rocks, Northland, New
Zealand. In : Sporli, K.B., Takemura, A., Hori, R.S. (Eds.), Oceanic Permian/Triassic
boundary sequence at Arrow Rocks (Oruatemanu Island), Northland, New Zealand: Geology
and Paleontology. Institute of Geological and Nuclear Sciences Monograph. p. 109-116.
Kamata, Y., Ueno, K., Hara, H., Ichise, M., Charoentitirat, T., Charusiri, P., Sardsud, A., Hisada, K.,
2009. Classification of the Sibumasu and Paleo-Tethys tectonic division in Thailand using
chert lithfacies. Island Arc 18, 21-31.
Kamata, Y., Ueno, K., Saengsrichan, W., Sardsud, A., Charoentitirat, T., Charusiri, P., Hisada, K.
2008. Stratigraphy and geological ages of siliceous sedimentary rocks distributed in the Hat
Yai area, southern peninsular Thailand. In: Choowong, M., Thitimakorn, T. (Eds),
Proceedings of International Symposia on Geoscience Resources and Environments of Asian
Terranes (GREAT2008), 4th IGCP516, and 5th APSEG. Bangkok, 24–26 November 2008,
349–352.
Kobayashi, T., 1963. Halobia and some other fossils from Kedah, northwest Malaysia. Japanese
Geology and Geography Journal, 34, 113-128.
Koike, T., 1973. Triassic Conodonts from Kedah and Pahang, Malaysia. In: Kobayashi, T., Toriumi,
R., (Eds.), Geology and Paleontology of Southeast Asia, 12, 91-113.
Koike, T., 1982. Triassic Conodont biostratigraphy in Kedah, West Malaysia. I In: Kobayashi, T.,
Toriumi, R., (Eds.), Geology and Paleontology of Southeast Asia, 23, 9-51.
Kozur, H., Kaya, O., Mostler, H., 1996, First evidence of Lower to middle Scythian
(Dienerian-lower Olenekian) radiolarians from the Karakaya Zone of northwestern Turkey.
ACC
EPTE
D M
ANU
SCR
IPT
ACCEPTED MANUSCRIPT
16
Geologische-Palaeontologische Mittelungen Innsbruck, Sonderband, 4, 271-285.
Kozur, H., Mostler, H., 1989. Radiolarien und Schwammskelern aus dem Unterperm des Voruals.
Geologische-Palaeontologische Mittelungen Innsbruck, 21, 147-275.
Kozur, H., Mostler, H., 1994. Anisian to middle Carnian radiolarian zonation and description of
some stratigraphically important radiolarians. Geologische-Palaeontologische Mittelungen
Innsbruck, Sonderband, 3, 39-255.
Kozur, H., Mostler, H.,1996. Radiolarians and facies of the Middle Triassic Loibl Formation, South
Alpine Karawanken Mountains (Carinthia, Austria). Geologische-Palaeontologische
Mittelungen Innsbruck, Sonderband, 4, 195-269.
Kusunoki, T., Imoto, N., 1996. Early Triassic (Spathian) radiolarians in chert from Southern
Kameoka City, Kyoto Prefecture. Earth Science (Chikyu Kagaku), 50, 184-188. (In Japanese
with English Abstract)
Kuwahara, K., 1999. Phylogenetic Lineage of Late Permian Albaillella (Albaillellaria, Radiolaria).
Journal of Geosciences, Osaka City University, 42, 85-101.
Kuwahara, K., Sakamoto, M., 1992. Late Permian Albaillella (Radiolaria) from a bedded chert
section in the Gujo-hachiman area of the Mino Belt, Central Japan; Preliminary Report on
Morphometry and Cluster Anaysis. Journal of Geosciences Osaka City University, 35, 33-51.
Kuwahara, K., Yao, A., Yamakita, S., 1998. Reexamination of Upper Permian radiolarian
biostratigraphy. Earth Science (Chikyu Kagaku) , 52, 391-404.
Metcalfe, I., 1981. Permian and Early Triassic conodonts from Northwest Peninsular Malaysia.
Geological Society of Malaysia Bulletin, 14, 119-126.
Metcalfe, I., 1990. Stratigraphic and tectonic implications of Triassic conodonts from northwest
Peninsular Malaysia. Geological Magazine, 127, 567-578.
Metcalfe, I., 1992. Upper Triassic conodonts from the Kodiang Limestone, Kedaha, Peninsular
Malaysia. Journal of Southeast Asian Earth Sciences, 7, 131-138.
Metcalfe, I., 1988. Origin and assembly of Southeast Asian continental Terranes. In: Audley-Charles
M. G., Hallam, A., (Eds.), Gondwana and Tethys. Geological Society of London Special
Publication, 37, pp. 101-118, Oxford University Press, Oxford.
Metcalfe, I., 1999. Gondwana dispersion and Asian accretion, an overview. In: Metcalfe, I., (Eds.),
Gondwana Dispersion and Asian Accretion IGCP321 Final Results Volume, pp. 9-28. A. A.
Balkema, Rotterdam.
Metcalfe, I., 2000. The Bentong-Raub Suture Zone. Journal of Asian Earth Sciences, 18, 691-712.
ACC
EPTE
D M
ANU
SCR
IPT
ACCEPTED MANUSCRIPT
17
Muenlek, S., Meesook, A., Tongchit, P., Tipdhonsab, C., Skulkaew, P. 1985. Geologic Map of
Changwat Narathiwat and Amphoe Takbai (Sheet NB 47-8,5, Scale 1:250,000). Geological
Survey Division, Department of Mineral Resources, Bangkok.
Nakaseko, K., Nishimura, A. 1979. Upper Triassic Radiolaria from Southwest Japan. Science
Reports, College of General Education Osaka University, 28, 61-109.
Ormiston, A., Babcock, L., 1979. Follicucullus, New radiolarian genus from the Guadalupian
(Permian) Lamar Limestone of the Delaware Basin. Journal of Paleontology, 53, 328-334.
O’Dogherty, L., Cater, E. S., Dumitrica, P., Gorican, S., De Wever, P., Hungerbuhler, A., Bandini,
A.N., Takemura, A., 2009. Catalogue of Mesozoic radiolarian genera; part 1. Triassic.
Geodiversitas, 31, 213-270.
O’Dogherty, L., De Wever, P., Gorican, S., Cater, E. S., Dumitrica, P., 2011. Stratigraphic ranges of
Mesozoic radiolarian families. Palaeoworld, 20, 102-115.
Ridd, M. F. 2009. The Phuket Terrane: a Late Palaeozoic rift at the margin of Sibumasu. Journal of
Asian Earth Sciences, 36, 238–251.
Ridd, M. F., 2011. Lower Palaeozoic. In: Ridd, M. F., Barber, A. J., Crow, M.J. (Eds.), The Geology
of Thailand, pp. 71-136-28. The Geological Society of London.
Sardsud, A., Saengsrichan,W. 2002. Geologic Map of Amphoe Hat Yai Sheet (5023II). Department
of Mineral Resources, Technical Report, No. 16, 1–77 (in Thai with English summary).
Sashida, K., 1983. Lower Triassic Radiolaria from the Kanto mountains, central Japan. Part I:
Palaeoscenidiidae. Transaction and Proceedings of the Palaeological Society of Japan, New
Series, 131, 168-176.
Sashida, K., 1991. Early Triassic radiolarians from the Ogamata Formation, Kanto Mountains,
central Japan. Part 2. Transaction and Proceedings of the Palaeontological Society of Japan,
New Series, 161, 681-696.
Sashida, K. Adachi, S. Igo, H., Koike, T., Amnan. I. B., 1995. Middle Triassic and Late Permian
radiolarians from the Semanggol Formation, Northwest Peninsular Malaysia. Transaction and
Proceedings of the Palaeontological Society of Japan, New Series, 177, 43-58.
Sashida, K., Igo, H. 1992. Triassic radiolarians from a limestone exposed at Khao Chiak near
Phatthalung, southern Thailand. Transaction and Proceedings of the Palaeontological Society
of Japan, New Series, 168, 1296-1310.
Sashida, K., Igo, H. 1999. Occurrence and tectonic significance of Paleozoic and Mesozoic
Radiolaria in Thailand and Malaysia. In, Metcalfe, I. ed., Gondwana Dispersion and Asian
Accretion (IGCP 321 Final Results Volume). A. A. Balkema, Rotterdam, Brookfield, 175-196.
ACC
EPTE
D M
ANU
SCR
IPT
ACCEPTED MANUSCRIPT
18
Sashida, K., Nakornsri, N., Ueno, K., Sardsud, A. 2000. Carboniferous and Triassic radiolarian
faunas from the Saba Yoi area, southernmost part of peninsular Thailand and their
paleogeographic significance. Science Reports of the Institute of Geoscience, University of
Tsukuba, Section B, 21, 71–99.
Sashida, K., Salyapongse, S., Charusiri, P., 2002, Lower Carboniferous radiolarian fauna from the
Saba Yoi-Kabang area, southernmost part of peninsular Thailand. Micropaleontology, 48,
129-143.
Sashida, K., Ueno, K., Nakornsri N., Sarsud, A. 1999. Lithofacies and Biofacies of the Khlong Kon
Limestone, Southern Peninsular Thailand. In, Ratanasthien, B. and Rieb, S. L. eds.,
Proceedings of the International Symposium on Shallow Tethys (ST) 5 Chiang Mai, Thailand.
Department of Geological Science, Faculty of Science, Chiang Mai University, Chiang Mai,
228-241.
Sone, M., Metcalfe, I. 2008. Parallel Tethyan sutures in mainland Southeast Asia: New insights for
Palaeo-Tethys closure and implications for the Indosinian orogeny. Comptes Rendus
Geoscience, 340, 166–179.
Sugiyama, K., 1992. Lower and Middle Triassic radiolarians from Mt. Kinkazan, Gifu prefecture,
central Japan. Transanction and Proceedings of the Palaeontological Society of Japan, no.167,
1180-1223.
Sugiyama, K., 1997. Triassic and Jurassic radiolarian biostratigraphy in the siliceous claystone and
bedded chert units of the southeastern Mino Terrane, central Japan. Bulletin of the Mizunami
Fossil Museum, no. 24, 79-193.
Takemura, A., Sakai, M., Sakamoto, S., Aono, R., Takemura, S., Yamakita, S., 2007, Earliest
Triassic radiolarians from the ARH and ARF sections on Arrow Rocks, Waipapa Terrane,
Northland, New Zealand. In : Sporli, K.B., Takemura, A., Hori, R.S. (Eds.), Oceanic
Permian/Triassic boundary sequence at Arrow Rocks (Oruatemanu Island), Northland, New
Zealand: Geology and Paleontology. Institute of Geological and Nuclear Sciences Monograph.
p. 97-107.
Ueno, K., 1999. Gondwana/Tethys divide in east Asia: solution from Late Paleozoic foraminiferal
paleobiogeography. In: Ratanasthien, B., Rieb, S.L. (Eds.), Proceedings of the International
Symposium on Shallow Tethys 5, Chiang Mai, Thailand. Department of Geological Sciences,
Chiang Mai University, Chiang Mai, pp. 45–54.
Ueno, K., 2002. Geotectonic linkage between West Yunnan and mainland Thailand: toward the
unified geotectonic evolution model of East Asia. In: Fourth Symposium of IGCP Project no.
ACC
EPTE
D M
ANU
SCR
IPT
ACCEPTED MANUSCRIPT
19
411, Geodynamic Processes of Gondwanaland-derived terranes in East & Southeast Asia,
Phitsanulok, Thailand, pp. 35-42.
Ueno, K., Charoentitirat, T., 2011, Carboniferous and Permian. In: Ridd, M. F., Barber, A. J., Crow,
M.J. (Eds.), The Geology of Thailand, pp. 71-136-28. The Geological Society of London.
Ueno, K., Hisada, K., 1999. Ueno, K. & Hisada, K. 1999. Closure of the Paleo-Tethys caused by the
collision of Indochina and Sibumasu. Chikyu Monthly, 21, 832–839 (in Japanese).
Ueno, K., Meno, S., Arita, M., Sardsud, A., Saesaengseerung, D., Saengsrichan, W., 2003. Triassic
carbonates and foraminifers in southern peninsular Thailand. In : Proceedings of 1st.
International Conference on Palaeontology of Southeast Asia. Mahasarakham, 27-30 October
2003. Mahasarakham University Journal, 22, (Special Issue), 258-259.
Wang, Y., Cheng, Y., Yang, Q., 1994. Biostratigraphy and systematics of Permian radiolarians in
China. Palaeoworld, 4, 172-202.
Wonganan, N., Caridroit, M., 2006. Middle to Upper Permian radiolarian fauna from chert blocks in
Pai area, northwestern Thailand. Eclogae Geologicae Helvetiae, 99, 133-139.
Yao, A., 1982. Middle Triassic to Early Jurassic radioralians from the Inuyama area, central Japan.
Journal of Geoscience, Osaka City University, 25, 53-70.
Yamakita, S., Takemura, A., Kamata, Y., Aita, Y., Hori, R. S., Campbell, H. J., 2007. A conodont
biostratigraphic framework of a Permian/Triassic ocean-floor sequence in the Accretionary
waipapa Terrane at Arrow Rocks, Northland New Zealand. In : Sporli, K.B., Takemura, A.,
Hori, R.S. (Eds.), Oceanic Permian/Triassic boundary sequence at Arrow Rocks (Oruatemanu
Island), Northland, New Zealand: Geology and Paleontology. Institute of Geological and
Nuclear Sciences Monograph. 69-86.
Yoshida, H., 1986. Upper Triassic to Lower Jurassic radiolarian biostratigraphy in Kagamigahara
City, Gifu Prefecture, central Japan. Journal of Earth Sciences, Nagaya University, 34, 1-21.
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Captions of figures
Fig. 1. (A) Outline map showing the tectonic subdivision of mainland and peninsular Thailand, (B)
outline geological map of peninsular Thailand indicating the location of the study area, and (C)
index map of Hat Yai, Songkhla Province, showing the distribution of the Yaha and Kaeng Krachan
formations and the location of the study sections.
Fig. 2. Stratigraphic columns of the study sections in the Hat Yai area, Songkhla, peninsular
Thailand. Composite columns show the lithologic composition of the lower shale unit and the upper
chert unit and the horizons of radiolaria-bearing samples. The right-hand column presents a
summarized stratigraphy of the study sections. Radiolarian zonations are based on Ishiga, (1986,
1990), Kuwahara (1999), Kuwahara and Sakamoto (1992), Kuwahara et al. (1998), Yao (1982), and
Sugiyama (1992, 1997).
Fig. 3. Photographs showing the lithology of studied clastic and siliceous rocks. (A) Permian clastics
of the lower shale unit at section HY05 showing cross-lamination and parallel lamination. (B)
Photomicrograph of the Permian clastics of the lower shale unit at section HY05 (Note: silty shale
consists mainly of calcareous bioclasts, and a foraminiferal test is present in the center of the image).
(C) Photograph of the outcrops at section HY01 showing the occurrence of radiolaria-bearing
bedded chert. (D) Polished slab surface of radiolaria-bearing chert showing distinct lamination and a
lithology that is less glassy and transparent than typical pelagic chert. (E) Photomicrograph of the
chert showing scattered radiolarian tests within a clay-rich matrix. (F) Enlargement of the chert
matrix showing tiny opaque fragments (organic fragments) and radiolarian tests. (G)
Photomicrograph of the radiolaria-bearing chert shows the occurrence of thin bivalve shells and (H)
a foraminiferal test.
Fig. 4. Stratigraphic columns showing the ranges of depositional ages of the three Permo-Triassic
facies (platform carbonate, Daonella-Halobia facies of intercalated sandstone and shale and
radiolaria-bearing bedded chert) distributed in southernmost peninsular Thailand and northernmost
peninsular Malaysia.
Fig. 5. (A) Schematic reconstruction of the sedimentary environment showing the lateral lithological
distribution of platform carbonate, fine clastics, and chert or siliceous sediments in the eastern
Sibumasu Continental Block in the Middle Triassic. (B) Present coeval distribution of Triassic chert
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and carbonates suggests that crustal shortening took place after deposition and the event could be
related to the collision of the Sibumasu and East Malaya (Indochina) blocks.
Table 1. List of radiolarians from study sections in the Hat Yai area, Songkhla, peninsular Thailand.
Plate I.
1-6. Follicucullus schlasticus Ormiston and Babcock, HY05-04.
7. Follicucullus scholasticus Ormiston and Babcock, HY02-102.
8-11. Spumellaria gen. et sp. indet. 8. HY02-103: 9. HY02-103: 10. HY02-103: 11. HY02-103.
12-13,15-16 Entactinosphaera ? sp. 12. HY02-103: 13: HY02-103: 15. HY02-103: 16. HY02-106
14. Eptingiidae, HY02-103.
17. Copicyntra ? sp. HY02-106
18. Triassospongosphaera ? sp. HY02-106
19-20. Acaeniospongus ? sp. 19. HY02-113: 20. HY02-130.
21-22. Copiellintra cf. akikawaensis Sashida and Tonishi, 20. HY02-125: 21. HY02-126.
23-24. Copiellintra sp. A, 23. HY02-130: 24. HY02-100.
25. Copiellintra sp. B, HY02-100.
26-27. Entactinia ? sp. 26. HY02+100: 27. HY02-100.
28-29. Entactinia cf. reticulata Sadhida and Tonishi, 28. HY02-100: 29. HY02-130.
30-31. Entactinosphaera chiakensis Sashida and Igo, 30. HY02-118: 31. HY02-123.
32-33. Entactinosphaera sp. B. 32. HY02-118: 33. HY-02-127.
Plate II.
1-3. Entactinosphaera sp. C. 1. HY02-123: 2. HY02-125: 3. HY02-125.
4-5. Entactinosphaera ? crassispinosa Sashida and Tonishi. 4. HY02-133: 5. HY02-135.
6-8. Entactinosphaera sp. A. 6. HY02-133: 7. HY02-126: 8. HY02-133.
9-10. Pantanellium sp. A. 9. HY02-128: 10. HY02-130.
11-12. Parasepsagon sp. 11. HY02-118: 12. HY02-129.
13-14. Parasepsagon tetracanthus Dumitrica, Kozur and Mostler, 13. HY02-133: 14. HY02-123.
15, 20. Plafkerium sp. 15. HY02-119: 20. HY02-129.
16-17. Triassospongosphaera sp. 16. HY02-118: 17. HY02-125.
18-19. Tiborella sp. 18. HY02-123: 19. HY02-126.
21-23. Eptingium nakasekoi Kozur and Mostler, 21. HY02-129: 22. HY02-121: 23. HY02-125.
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24-25. Eptingium manfredi Dumitrica, 124. HY02-120: 25. HY02-119.
26. Hozmadia gifuensis Sugiyama, HY02-113.
27. Hozmadia reticulata, Dumitrica, Kozur and Mostler. HY02-130.
28. Hozmadia sp. HY02-130.
29. Anisicyrtis sp. HY02-129.
30. Spongosilicarmiger sp. HY02-127.
Plate III.
1-6, 13. Triassocampe coronata Bragin, 1. HY01-03: 2. HY01-03: 3. HY01-05: 4. HY21-01: 5.
HY01-05: 6. HY01-05: 13. HY01-05.
7-12, 14-16. Triassocampe sp. 7. HY21-01: 8. HY01-05: 9. HY01-05: 10. HY01-05: 11. HY01-03:
12. HY01-05: 14. HY01-01: 15. HY21-01: 16. HY01-03.
17. Pseudostylosphaera spinulosa (Nakaseko and Nishimura). HY21-01.
18, 20, 22. Eptingium sp. 18. HY21-01: 20. HY21-01, 22. HY21-01.
19, 21. Parasepsagon sp. 19. HY21-01: 21. HY01-05.
23. Eptingium nakasekoi Kozur and Mostler, HY21-01.
24. Pseudostylosphaera japonica, (Nakaseko and Nishimura) , 24. HY01-01.
25-28, 38. Pseudostylosphaera japonica (Nakaseko and Nishimura), 25. HY21-03: 26. HY21-03:
27. HY21-03: 28. HY04-03: 38. HY04-01.
29. Pseudostylosphaera sp. HY21-03.
30. Pseudostylosphaera ? sp. HY21-03.
31. Archaeospongoprunum bispinosum Kozur and Mostler, HY21-03.
32. Spongoxystris ? sp. HY04-02
33. Triassocampe coronata Bragin, HY21-03.
34. Triassocampe deweveri (Nakaseko and Nishimura), HY04-04
35-37. Triassocampe sp. 35. HY04-04: 36. HY04-04: 37. HY04-04.
39. Hozmadia sp. HY04-03.
40. Parasepsagon sp. HY21-03.
41. Tiborella cf. anisica Kozur and Mostler, HY21-03.
42. Entactinia ? sp., HY21-03.
Plate IV.
1. Triassocampe coronata Bragin, HY04-11.
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2. Triassocampe deweveri (Nakaseko and Nishimura) , HY21-03.
3-4. Triassocampe sp. 3. HY04-06: 4. HY04-06.
5-7. Pseudostylosphaera japonica (Nakaseko and Nishimura), 5. HY04-07: 6. HY04-11: 7.
HY04-07.
8. 16. Pseudostylosphaera sp. HY04-11.
9. 17 Pseudostylosphaera spinulosa (Nakaseko and Nishimura), HY04-06.
10-11. Spine A2 of Sugiyama (1997), 10. HY04-06: 11. HY04-06.
12. Spine A1 of Sugiyama (1997), 12. HY04-06.
13. Paroertlispongus sp. HY04-06.
14-15. Spongoxystris ? sp. 14. HY04-07: HY04-06.
18-20. Cryptostephnidium cornigerum 18. HY04-07: 19. HY04-11: 20. HY04-11.
21. Spongostylus ? sp.
22-23. Eptingium sp. HY04-07.
24. Hozmadia sp. HY04-06
25. Pentactinocarpus sp. HY04-11.
26-27. Triassospongosphaera ? sp. 26. HY04-06: 27. HY04-06.
28. Tiborella cf. anisica Kozur and Mostler, HY04-11
29. Parasepsagon sp. HY04-07.
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Figure 1
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Figure 2
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Figure 3
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Figure 4
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Figure 5
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Plate 1
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Plate 2
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Plate 3
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Plate 4
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Table 1
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Highlights 1. We revised depositional age a part of Paleozoic in Peninsular Thailand. 2. We proposed Paleo-environment of above re-interpreted sediments. 3. We clarify a tectonic setting of margin of the Sibumasu Block. 4. We provided constraints for oceanic closure time (collision time of continentals).
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