Petrography and Geochemistry of Metasedimentary Rocks from the Taku Schist in Kelantan, North-East Peninsular Malaysia

Journal of Applied Geology, vol. 5(2), 2020, pp. 124–140 DOI: http://dx.doi.org/10.22146/jag.61183

Muhammad Irman Khalif Ahmad Aminuddin1,2, Nugroho Imam Setiawan*1, I Wayan Warmada1, Kamar Shah Arifﬁn2, and Kotaro Yonezu3

1Department of Geological Engineering, Faculty of Engineering, Universitas Gadjah Mada, Yogyakarta, Indonesia 2School of Materials and Mineral Resources Engineering, Universiti Sains Malaysia, Nibong Tebal, Penang 14300, Malaysia 3Department of Earth Resources Engineering, Kyushu University, 819-0395, Fukuoka, Japan

ABSTRACT. The Taku Schist, located in north-east Peninsular Malaysia, is characterized by its North-South oriented elongated body. It forms part of the Indosinian orogenic build-up generated by the convergence of the Sibumasu continental block and Sukhothai Arc. Pet- rographic analyses of the metasedimentary rocks sourced from the Taku Schist revealed that the formation was attributable to greenschist’s metamorphism into amphibolite facies, which could be observed near the Triassic and Cretaceous intrusions of the Kema- hang Granite. The evolution process of the rocks could be linked with the interactions between a contact and regional metamorphisms. The resulting of XRF and ICP-MS geochemical analyses upon the assessment disclosed that the metasedimentary rocks of Taku Schist were made up of greywacke and shale, grouped into the quartzose sedimentary protolith, and belonged to the Continental Island Arc (CIA). It reﬂects the Taku Schist’s episodic contractions, wherein they would lead to the Sibumasu sedimentary cover along with both an accretionary wedge and the genetically-correlated Bentong-Raub mélange to different greenschist. Otherwise associated with amphibolite facies, the facies’ conditions and depths were determined according to their position with the Sukhothai Arc’s upper plate. Keywords: Peninsular Malaysia · Taku Schist · South-East Asia · Indosinian orogen.

1I NTRODUCTION tary rocks will be beneficial in evaluating the The metasedimentary rocks of Taku Schist in crucial determinants of both pre-metamorphic the north-east region of Peninsular Malaysia sedimentary and orogenic evolutions, as well formulate a percentage of the Indosinian oro- as their path. Furthermore, research efforts genic and post-orogenic structures found in on protolith analysis will also yield novel in- Southeast Asia. These rocks’ formation re- sight regarding the compositional differences sulted from subduction and collision experi- of a depositional environment, protolith, trans- enced by the Sibumasu continental block and port, and the source and sink’s geotectonic loca- Sukhothai Arc during the Permo-Triassic pe- tion. Accordingly, a metamorphosed sediment riod (Metcalfe, 2002; Ferrari et al., 2008; Ridd, and its composition represent its history and 2012; Morley, 2012). An assessment of the petro- initial evolution, whereas its mineral composi- logical and geochemical properties of sedimen- tion reveals the subsequent development. Re- gardless, geochemical research efforts encom- passing the significant elements and immobile *Corresponding author: N.I. SETIAWAN, Depart- ment of Geological Engineering, Universitas Gadjah trace elements, including rare earth elements, Mada. Jl. Grafika 2 Yogyakarta, Indonesia. E-mail: are likely to be beneficial as reactive indicators [email protected]

2502-2822/© 2020 The Authors. Open Access and published under the CC-BY license. PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN of source rocks and tectonic setting. Hence- Moreover, they experienced intrusions due to forth, this work aims to differentiate newly- no small pluton (Kemahang granite) and re- obtained data from protolith studies on South- main in the proximity of non-metamorphosed east Asia basins, specifically the Taku Schist to sub-greenschist facies Permo–Triassic sed- in North-East Peninsular Malaysia. This study iments (Ali et al., 2016; Hutchison, 2009 and will undoubtedly contribute towards the body Khoo and Lim, 1983). Meanwhile, the Taku of knowledge on the regional geodynamic en- Schist itself presents a north-south elongated vironment and tectonic setting. body characterized by 80 km-long and 8 to 22 km-wide dimensions. In general, the non- 2R EGIONAL GEOLOGY fossiliferous Taku schist’s age could not be The formation of the Indosinian orogeny in accurately determined but is presumed to be Peninsular Malaysia was dated back to the of the Permo-Triassic period (Khoo and Lim, Devonian–Permian subduction and Paleo– 1983). Tethys Ocean closure due to the Triassic collision between the East Malaya Block and 3M ETHODOLOGY Sibumasu continental unit (Metcalfe, 2000). Taku Schist belongs to north-east Peninsular Figure 1a shown the sequel of the subduction Malaysia and reveals a vast exposure of meta- and collision events, which have separated the morphic rocks originated from the sediments Peninsular Malaysia into three parallel belts and subordinate magmatic rocks that will meta- according to their variations of magmatism, morphose into greenschist-amphibolite facies stratigraphy, mineralization, structure, and in the later stages. The approximate sampling metamorphism (Hutchison, 1975 and Metcalfe, locations of metasedimentary rocks are marked 2013). Furthermore, in-depth geochemical and in Figure 2 accordingly. absolute age-dating works have concluded In total, 13 metasedimentary rock samples that the primarily sedimentary Central Belt were collected from the research area. The sub- separates the Permian–Lower Triassic I-type sequent thin section sample preparation pro- Eastern Belt and Late Triassic S-type Western cesses and petrographic analyses were carried Belt (Ghani et al., 2013; Ng et al., 2015 and out at Economic Geology Laboratory, Depart- Searle et al., 2012). The intrusion of plutons ment of Earth Resources Engineering, Kyushu into a well-documented sedimentary succes- University, Fukuoka, Japan. Petrographic thin sion depicts the measured shift from shallow sections were prepared to identify the textu- to deep marine environments, thereby impact- ral characteristics and the secondary minerals ing the regionally metamorphosed rocks to of rocks through observation using a Nikon different degrees. Such effect includes the ac- Eclipse E600 POL microscope equipped with an cretionary mélange housing the mafic rocks of AdvanCam-U3II camera. the Bentong–Raub suture zone (Ali et al., 2016). Geochemistry analyses for 13 samples of Accordingly, the area has been positioned as metasedimentary rocks from Taku Schist were the suture connecting the Sibumasu and East analyzed using X-ray fluorescence (XRF) and Malaya Block/Sukhothai Arc (Metcalfe, 2000; Inductively Coupled Plasma-Mass Spectrom- Metcalfe, 2013 and Hutchison, 2009). In partic- etry (ICP-MS) methods. For XRF, before the ular, the Taku Schist of North-East Peninsular analysis, one 1 gram of each sample was com- Malaysia as depicted in Figure 1b is notable busted in an electric furnace at 1000°C for 2 due to the varying grades of metamorphic hours to determine the LOI value. Pressed rocks lying close to the Late Cretaceous mag- powdered samples were prepared by pressing matic intrusions (Searle et al., 2012; Hutchison, at 20 MPa for about 2 minutes in vinyl chloride 2009; Khoo and Lim, 1983 and Ghani, 2000). rings. A Rigaku RIX 3100 XRF spectrometer Therefore, this region’s metasediments was utilized in the analysis to determine the have displayed several properties, including bulk major, minor, and trace elemental compo- greenschist-amphibolite facies metamorphism, sitions of the pressed powdered samples. The an extensive deformation fabric, and resid- research’s measurement conditions considered ual metamorphosed mafic or acid intrusive. were 30 kV, and 70 mA, and the JA-3 andesite

Journal of Applied Geology 125 AMINUDDIN et al.

100OE 105OE 110OE

1a Paleo-Tethys Suture Zone Myanmar Sukhothai Island-arc System West 0 500km Burma Block Laos

O Figure 2 20 N 1b T H A I L A N D Lebir Fault N Thailand Indochina Tanah Terrane Merah Machang Baling Jeli K E D A H RESEARCH Cambodia

Bentong-Raub Suture Zone Suture Bentong-Raub AREA Bok Bak Fault Chanthaburi Terrane Kuala Krai Lebir Fault

ANDAMAN Sukhothai and SEA Gerik K E L A N T A N 10ON

Sibumasu Bok Bak Fault Terrane P E R A K Lebir Fault

Bok Bak Fault Gua Musang Kuala Kangsar 05ON Fig.1b Malaysia West Sumatra Block East P A H A N G Malaya

Block Tanah Rata

LEGENDS Quaternary clay, silt, sand with minor gravel Acid intrusive rock Jurassic-Cretaceous cross-bedded sandstone with Major Fault subordinate conglomerate and shale/mudstone Triassic interbedded sandstone, siltstone and shale; widespread volcanics mainly tuff Minor Fault Permian-Triassic bedded limestone Thailand Permian phyllite, slate and shale with subordinate sandstone and schist Carboniferous-Permian schist, phyllite, slate, metasandstone, sandstone, shale and chert with minor limestone Carboniferous phyllite, slate, shale and sandstone Silurian-Devonian argillaceous; slate, phyllite, schist and pelitic hornfels, calc- sillicate facies; calc-sillicate hornfels, and impure limestone; and sandstone Ordovician-Silurian schist, phyllite, slate and limestone

FFigureIGURE 1. 1: (a) Simplified (a) Simplified tectonic map tectonic of Peninsular map Malaysia of Peninsular in terms of Malaysia Asia continental in terms units and of suture Asia zonescontinental (modified units after Metcalfe, and suture 2013); (b)zones Simplified (modified geological after map Metcalfe, of Taku Schist 2013); in North-East (b) Simplified Peninsular Malaysia.geological Note map the Sibumasu of Taku continental Schist unit’sin the demarcation North-East and East Peninsular Malaya Block Malaysia. via the Bentong-Raub Note the suturedemarcation zone (modified of the after Sibumasu Ali et al., 2016). continental The rectangle unit in Figure and 1a East denotes Malaya the map’s Block location via in theFig- ureBentong-Raub 1b.. suture zone (modified after Ali et al., 2016). The rectangle in Figure 1(a) denotes the location for the map in Figure 1(b).

126 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

102,0° 102,2° LITHOLOGY

Lebir Shale, slate, phyllite

O O O O O O O O O O O O O O O Sandstone O O O O

O O Fault Limestone/marble

Schist

V V V V V V V V V V V

V V V V V V Acid to intermediate volcanic

V V V V V

V V V V V V

V V V V V

V V V V V V Intermediate to basic volcanic

+ + + + + Tanah Merah 5,8° + + + + + + + + + Acid intrusive Boundary Range + + + + Kemahang Granite Serpentinite Granite

2105B AGE 2107A Late Cretaceous 2101A Jurassic-Early Creataceous 2001A 2102A Temangan Middle-Late Triassic 2003A 2104A Late Permian-Middle Triassic

Carboniferous-Permian

Silurian-Devonian 5,6° LEGEND

Unconformity Kuala Krai Thrust Fault

Anticline Fold

Normal Fault

Strike-slip Fault Taku Schist Sampling Point Location

SAMPLE NO & ROCK TYPE 2001A Chl-Bt-Ms schist 2107A Chl-Bt-Ms schist 1901A 5,4° 2105B Chl-Bt-Ms schist 2003E 2103A Chl-Bt-Ms schist Dabong 2105A Chl-Bt-Ms schist Kenerong 2103A 2106A Chl-Bt-Ms schist Leucogranite 2106A 2106B Chl-Bt-Ms schist 2105A 2101A Metasandstone 2106B 2102A Graphitic Slate 0 2 4 6 8 10km 2003E Mica schist 2003A Ab-Chl-Bt-Ms schist 2104A Ep-Ab-Chl-Bt-Ms schist 1901A St-Chl-Bt-Ms schist

FFigureIGURE 2. 2: Detailed Detailed geological geological and structural andmap structural of the metasedimentary map of the rock metasedimentary sampling locationsfor rock this studysampling (Modiﬁed locations after Ali et for al., 2016). this studyThe red circles (Modified represent after the sampling Ali et al., locations 2016). plotted The on the sampling map with theirlocations representative are represented sample codes (white by boxes). the red Abbreviations: circles Chl plotted = Chlorite, on Bt the = Biotite, map Ms with = Muscovite, their Strepresentative = Staurolite, Ab = Albite, sample Ep = Epidote. codes (white boxes). Abbreviations: Chl=Chlorite, Bt=Biotite, Ms=Muscovite, St=Staurolite, Ab=Albite, Ep=Epidote.

Journal of Applied Geology 127 AMINUDDIN et al.

(Imai et al., 1995) standard was used to monitor ern margin. Recent U-Pb dating of the Kema- the result precision, with an error of less than hang granite yielded an age estimation of 226.7 5% was yielded. These XRF analyses were car- ± 2.2 Ma (Ng et al., 2015). As the metamor- ried out at the Economic Geology Laboratory, phism fans outwards away from the granite Department of Earth Resources Engineering, margins and to the south of the Taku Schist, the Kyushu University, Japan. subsequent compaction of the rocks and pres- ICP-MS determined the concentrations of sure cause plate movements, thus resulting in rare earth elements (REE) at the Centre of Ad- the formation of low-grade mica schist (2003E) vanced Instrument Analysis, Kyushu Univer- (Figure 3d) and Chl–Bt–Ms schist (2106A) (Fig- sity, Japan. The ICP-MS sample preparation ure 3e). In particular, the presence of mylonitic procedure commenced with the digestion of and augen textures outcrops (2106B) in this area the sample containing REEs with diluted HCl is a reflection of the complex history behind solution. The digested sample was added a brittle-ductile deformation (Figure 3f). As to aluminum sec-butoxide (Al(O-sec-Bu)3, such, the metamorphism of coarse-grained sed- TBA0) at room temperature before agitation imentary rocks such as metasandstone outcrop for 2 hours. Subsequently, the solvents of (2101A) can be found in certain localities (Fig- tetraethyl orthosilicate (Si(OEt)4, TEOS) and ure 3g), whereas a highly folded graphitic slate N, N-dimethylformamide were added. The sol (2102A) may be identified in some other loca- solution was heated to 160°C at a rate of 1 °C/h tions (Figures3h and3i). to produce dry gel before further heating to 1000 °C for 2 hours using a heating rate of 10 4.2 Petrography °C/h. ICP-MS analyzed the concentrations of A summary of results is mentioned in the fol- REEs after the acid decomposition of the glass. lowing passages to delineate the representative samples’ petrographic attributes. At the same 4R ESULTS time, Table 1 lists the estimated modal abun- 4.1 Field Occurence and Sample Description dances of minerals for each sample. In general, The Chl-Bt-Ms pelitic schist outcrops are the the sample petrographic analysis indicates that common type of rock identified in the study the metasedimentary rocks from the Taku Schist area. Figure 3a shows one of the Chl–Bt–Ms can be grouped into greenschist and amphibo- schist (2001A) samples sourced near the Taku lite facies accordingly. Schist’s northern part (Figure 2). Several bar- Seven samples of Chl–Bt–Ms schist were an- ren quartz veins have intruded into the Chl- alyzed in this study, wherein mica minerals pri- Bt-Ms schist in this location, which may occur marily made up of biotite and muscovite were either following the foliation or cross-cutting abundantly present in the rock. Meanwhile, into the outcrop foliation for contact with the other minerals present were predominantly of brecciated appearance along with the outcrop the quartz and opaque types. In particular, (Figure 3b). Generally, the northern part of the Chl-Bt-Ms schist sourced from the northern the Taku Schist is associated with the metamor- part of the Taku Schist (i.e., 2001A, 2107A, and phism of argillaceous rocks close to the granite 2105B) displayed a decussated texture consist- margin (Kemahang Granite), thereby resulting ing of a muscovite-rich layer made up of ran- in the non-schistose appearance of Ep–Ab–Chl– domly oriented interlocking platy, prismatic, Bt–Ms schist (2104A) in some localities within or elongated minerals (4a). The texture above the area (Figure 3c). According to MacDonald was a reflection of the contact metamorphism (1968) in Ali et al. (2016), the Kemahang gran- present in the northern part of the study area, ite, specifically in this region, is foliated, cata- whereby the Triassic Kemahang granite played clastically sheared, and made up of numerous a role in interconnecting the structures of the schist xenoliths of 107 ± 3 Ma age. Bignell and Stong Complex and Taku Schist specifically Snelling (1977) reported the K-Ar biotite dat- via the intruded dome-shaped structures (Mac- ing of the Taku Schist as Late Triassic (212 ± 8 Donald, 1968 and Francois et al., 2017). Towards Ma) with metamorphism near the dome’s west- the south of the Taku Schist, the same rock type of Chl-Bt-Ms schist (i.e., 2103A, 2105A,

128 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

a b Chl-Bt-Ms schist c

Ep-Ab-Chl-Bt-Ms schist Chl-Bt-Ms schist

Brecciated Quartz Vein Quartz Quartz Veins

2001A 2005B 2104A d e f Chl-Bt-Ms schist

Chl-Bt-Ms schist Mica schist

2003E 2106A 2106B g h i Metasandstone

Graphi�c slate Graphi�c slate

2101A 2102A 2102A

FFigureIGURE 3. 3: Field Field views views of the samplingof the sampling stations for thestations metasedimentary for the rocksmetasedimentary sourced from Taku rocks Schist, north-eastsourced Peninsular from Taku Malaysia. Schist, (a) An north-east exposed outcrop Peninsular of Chl–Bt–Ms Malaysia. schist in the (a) northern An exposed part of the Takuoutcrop Schist. of (b) Chl-Bt-Ms Greenschist facies schist and brecciated in the quartz northern vein contact. part of (c) The the non-schistose Taku Schist. appearance (b) ofGreenschist Ep–Ab–Chl–Bt–Ms facies schist. and (d) A brecciated boulder of mica quartz schist rock. vein (e) contact. Greenish Chl–Bt–Ms (c) Non-schistose schist outcrop. (f) An outcrop of highly foliated Chl–Bt–Ms schist in the southern part of the Taku Schist. (g) Exposed metasandstoneappearance with of several Ep-Ab-Chl-Bt-Ms structural joints. schist. (h) A closed (d) dark A plate boulder of graphitic of mica slate. (i) schist Folding rock. of graphitic (e) slate.Greenish Abbreviations: Chl-Bt-Ms Chl = Chlorite,schist outcrop. Bt = Biotite, Ms(f) =An Muscovite, outcrop Ep =of Epidote, highly Ab foliated = Albite. Chl-Bt-Ms schist in the southern part of the Taku Schist. (g) Exposed metasandstone with several structural joints. (h) A closed dark plate of graphitic slate. (i) Folding of graphitic slate. Abbreviations: Chl=Chlorite, Bt=Biotite, Ms=Muscovite, Ep=Epidote, Ab=Albite.

Journal of Applied Geology 129 AMINUDDIN et al. oe l lgols;A:Abt;Ks oasu edpr z urz t itt;M:Msoie h:Clrt;G:Gaht;E:Eioe t Staurolite; St: Epidote; Ep: Graphite; Gr: Chlorite; Chl: Muscovite; microscope. Amphibolite; under Ms: Amp: – Absent/Unidentiﬁed Biotite; Greenschist; –: Bt: Grs: and Quartz; minerals; Opaque Qz: Feldspar; Op: Potassium Sericite; Kfs: Grs Ser: Albite; Ab: Plagioclase; Pl: Grs Note: schist Ep-Ab-Chl-Bt-Ms 13 2104A Grs 12 schist Mica Grs 11 2003E 10 Metasandstone 2101A Grs 9 schist Chl-Bt-Ms 8 2106A 7 Grs 6 schist Chl-Bt-Ms 5 2103A 4 schist Chl-Bt-Ms 2107A 3 Facies 2 1 Type Rock Sample No. 1901A 2003A 2102A 2106B 2105A 2105B 2001A tClB-sschist St-Chl-Bt-Ms schist Ab-Chl-Bt-Ms slate Graphitic schist Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms T Amp ABLE Grs Grs Grs Grs Grs Grs .Mdlaayi ftercsdlbrtdi h urn work. current the in deliberated rocks the of analysis Modal 1. ♦ # # – ♦ ♦ ♦ ♦ ♦ Op ♦ ♦ Ser St ♦ Ep ♦ Gr Chl Ms ♦ Bt Qz Kfs Pl/Ab

♦ ♦ ♦ ♦ ♦ ♦ ♦ ♦

# # # # ao iea te Mineral Other Mineral Major

# # # # # # # # #

bnat(>40%); Abundant :

# ♦

# – – – – – –

– – – – – – – – – – – – – – – – – – – – – – – # ♦ – – – – – – – ih(20–40%); Rich :

– – – – – – – – –

– – – – – – –

♦ ♦ ♦ ♦ ♦ ♦ – – – – oeae(10–20%); Moderate : tuoieminerals staurolite of texture Poikiloblasts metamorphism. appearance.Contact hornfelsic Non-schistose, Metapsammite. mica. of essentially consisting schistose well-foliated Strong, cleavage.Metapelites. slaty Pervasive Metapelites. metamorphism.Metapelites. feldspar.Regional and quartz of texture fabrics.Augen Crenulation greenschist.Metapelites. indurated metamorphism.Spotted layer.Contact rich mica of texture Decussate Remark ♦ or(<10%) Poor :

130 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

2106A, and 2106B) depicted the crenulation fab- (4f), while chlorite (10%) and muscovite (5%) rics (4b) as schistosity. Such crenulation cleav- minerals could be observed as a matrix in the age was generated following the alignment of samples. The dark- coloration of the specimen platy minerals, which were mostly muscovite for this type of rock indicates a history of inter- minerals in nature. mediate metamorphism with concomitant in- Furthermore, the texture indicated the im- terbedding between basic volcanic rocks and pact afflicted on the southern part of the Taku the original sedimentary rocks. Schist due to extensive metamorphic foliation, Moreover, one particular sample of St–Chl– namely the varying types of planar and lin- Bt–Ms schist (i.e., 1901A) contained poikilo- ear structures. These include foliations and blasts of high-relief staurolite (10%) and dis- stretching lineations, folds, faults and stria- played yellow pleochroism (4g), thereby fre- tions, and shear zones described by Ali et al. quently consisting of fine-grained quartz and (2016). Almost all Chl–Bt–Ms schist samples opaque minerals. Meanwhile, the other min- consisted of more than 40% muscovite minerals that concurrently present in the sample eral, followed by biotite (20–30%), quartz (10– included muscovite (20%), biotite (20%), and 20%), chlorite (10%), plagioclase (>10%), and quartz (15%), with a minor presence of opaque K-feldspar (>10%). Meanwhile, other compo- minerals (>5%). Besides, one might define sitions were of opaque minerals. this rock’s schistosity using mica minerals and In particular, the metasandstone rock sam- opaque grains (4h). The Ep–Ab–Chl schist rock ple (i.e., 2101A) yielded minerals such as quartz sample (i.e., 2104A), in particular, consisted of (30%) and feldspar (10%), which were typically epidote (>10%), albite (30%), biotite (10%), mus- present in polycrystalline phaneritic clasts dis- covite (10%), chlorite (20%), and quartz (10%) playing a porphyroblastic texture (4c). Simi- (4i). The occurrence of epidote minerals is larly, the lithic grains of metamorphic metap- due to the contamination of felsic igneous rock sammite were composed of quartz, muscovite, in this region. Additionally, specific places and sericite fragments (50%), thereby proving and those nearby the contact location between the occurrences of solid-state deformation and Taku Schist and Kemahang granite at the north- recrystallization under the greenschist facies ern part might reveal amphibolite schist. It conditions (Palin and Dyck, 2020). In brief, was suggested that its formation is attributable the lowest metamorphism grade was repre- to metamorphism and direct association with sented by a very fine-grained rock of graphitic granite intrusion. However, its appearance is slate (2102A), consisting of the detrital grains of not schistose to mica-schist; instead, it is often quartz (20%), minor alkali feldspar (10%), and hornfelsic in nature. a fine matrix consisting of mica (20%), graphite (20%), and chlorite (20%) (4d). Besides, the in- 4.3 Whole-rock Geochemistry tensely deformed shape of rock produced a per- The compositions of major oxides (wt.%), trace vasive slaty cleavage, wherein the original fine- elements (ppm), and rare earth elements (ppm) scale bedding was concurrently disrupted via in all metasedimentary rock samples from the folding. Additionally, one specific rock sam- Taku Schist of north-east Peninsular Malaysia ple of mica schist (2003E) yielded good schistos- are presented in Table 2. The concentrations of ity. The majority of the minerals demonstrated major oxides and trace elements were obtained crystalloblastic, nematoblastic, and xenoblastic from the XRF analysis, while the rare earth el- textures with crystal sizes ranging from 0.5 mm ements concentrations have resulted from the to 4.0 mm. In particular, its composition was ICP-MS analysis. primarily made up of quartz (30%), muscovite 4.3.1 Major element geochemistry (30%), biotite (20%), and K-feldspar (10%) (4e). The Ab–Chl–Bt–Ms rock sample (2003A) pre- Figure 5 displays the distribution of all samples dominantly consisted of colorless minerals such understudy in a SiO2/Al2O3 versus K2O/Na2O as twinned albite (40%) and quartz (20%) ap- diagram according to the grid proposed by pearing as porphyroclasts. Some of the biotite Wimmenauer (1984). The grid design was cre- (20%) samples were marked by brown color ated to clarify clastic sedimentary protoliths,

Journal of Applied Geology 131 AMINUDDIN et al.

a Chl-Bt-Ms schist b Chl-Bt-Ms schist c Metasandstone bt pl

2001A 5mm 2106B 5mm 2101A 5mm d Graphi�c slate e Mica schist f Ab-Chl-Bt-Ms schist bt

chl

2102A 5mm 2003E 5mm 2003A 5mm g St-Chl-Bt-Ms schist h St-Chl-Bt-Ms schist i Ep Ab Chl Bt Ms schist ms bt

st ep

st 1901A 5mm 1901A 5mm 2104A 5mm

FFigureIGURE 4. 4: Photomicrographs Photomicrographs of the rock of samples the rock from Takusamples Schist, north-eastfrom Taku Peninsular Schist, Malaysia. north-east (a) De- cussatedPeninsular texture of Malaysia. Chl–Bt–Ms schist. (a) (b) Decussated Crenulation fabric texture of Chl–Bt–Ms of schist. Chl-Bt-Ms (c) Polycrystalline schist. phaner- (b) iticCrenulation clasts of quartz fabric and plagioclase of Chl-Bt-Ms in the quartz-muscovite-sericite schist. (c) Polycrystalline fragments of a phaneritic metasandstone clasts rock sam- of ple. (d) Detrital grains of quartz and minor alkali feldspar with a ﬁne matrix of mica, graphite, and some chloritequartz of a and graphitic plagioclase slate rock sample. in (e) the Schistosity quartz-muscovite-sericite of mica schist. (f) Porphyroclasts fragments of twin albite offor themetasandstone Ab–Chl–Bt–Ms schist. rock (g) A sample. close-up of (d) staurolite Detrital mineral. grains (h) Poikiloblasts of quartz of high-relief and minor staurolite alkali in St– Chl–Bt–Msfeldspar schist. with (i) a Bright fine and matrix ﬂuorescent of mica, color of epidote graphite, minerals and in Ep–Ab–Bt–Ms some chlorite schist. of Abbreviations: graphitic Chlslate = Chlorite, rock Btsample. = Biotite, Ms(e) = Muscovite,Schistosity Pl = ofPlagioclase, mica schist. Ab = Albite, (f) St Porphyroclasts = Staurolite, Ep = Epidote. of twin albite for the Ab-Chl-Bt-Ms schist. (g) A close-up of staurolite mineral. (h) Poikiloblasts of high-relief staurolite in St-Chl-Bt-Ms schist. (i) Bright and fluorescent color of epidote minerals in Ep-Ab-Bt-Ms schist. Abbreviations: Chl=Chlorite, Bt=Biotite, Ms=Muscovite, Pl=Plagioclase, Ab=Albite, St=Staurolite, Ep=Epidote.

132 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

TABLE 2. Major (wt.%) and trace elements (ppm) compositions of representative samples in this study.

Facies Grs Grs Grs Grs Grs Grs Grs Grs Grs Grs Grs Grs Amp Sample 2001A 2107A 2105B 2103A 2105A 2106A 2106B 2101A 2102A 2003E 2003A 2104A 1901A Rock Type Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms schist Chl-Bt-Ms schist Meta-sandstone Graphitic Slate Mica schist Ab-Chl-Bt-Ms schist Ep-Ab-Chl-Bt-Ms schist St-Chl-Bt-Ms schist Major Elements (wt.%) SiO2 72.47 72.38 77.15 63.86 66.31 62.17 65.11 61.7 54.28 68.44 78.83 59.31 67.33 TiO2 0.17 0.63 0.29 0.44 0.64 0.8 0.62 0.59 0.82 0.57 0.37 0.65 0.68 Al2O3 14.09 12.82 11.29 11.05 14.99 16.37 13.3 17.59 19.67 13.57 9.06 23.49 13.59 FeO 2.02 4.0 3.02 3.62 3.88 4.6 3.15 4.54 6.99 4.12 3.55 5.02 4.83 MgO 1.0 2.36 1.42 1.83 2.26 2.48 2.59 1.94 3.54 2.19 1.6 0.61 2.57 MnO 0.02 0.07 0.06 0.18 0.09 0.1 0.12 0.19 0.04 0.08 0.04 0.01 0.19 CaO 4.69 0.41 1.35 7.73 2.2 2.31 5.05 4.25 2.99 1.64 0.62 0.04 1.88 Na2O 0.56 1.41 0.49 0.58 0.6 0.82 1.34 2.49 0.85 0.64 0.92 0.48 1.16 K2O 3.0 3.46 3.13 2.54 3.8 4.06 2.45 3.73 3.97 3.13 2.09 4.09 3.13 P2O5 0.07 0.12 0.11 0.13 0.18 0.17 0.12 0.07 0.13 0.17 0.22 0.01 0.15 LOI 1.7 2.18 1.21 7.58 4.67 5.68 5.63 2.64 6.51 5.16 2.11 6.14 4.08 Total 99.77 99.84 99.52 99.54 99.62 99.56 99.48 99.73 99.79 99.71 99.41 99.85 99.59 Trace Elements (ppm) V 28 92 20 132 20 185 92 85 185 114 98 114 182 Cr 50 46 60 54 64 38 46 70 117 19 38 109 140 Ni 73 32 13 50 13 24 32 60 96 13 40 13 39 Rb 52 172 145 24 36 15 172 57 190 177 148 177 456 Sr 185 47 40 166 40 100 47 161 186 51 68 51 686 Zr 160 337 260 133 298 340 143 265 211 187 109 342 110 Nb 3 14 15 7 15 23 14 10 15 14 9 14 12 Ba 173 679 470 308 288 197 679 908 636 698 438 698 478 Th 12 4 15 10 6 15 11 7 6 4 12 10 13 U 2 n.d. 2 1 4 2 n.d. n.d. n.d. n.d. 2 n.d. 1 Rare Earth Elements (ppm) Sc 12. 4. 10. 8.1 10.9 10.3 10.4 5. 6.1 9.4 10.1 8. 12.4 Y 8.7 9.5 13.2 12.2 7.6 7.9 4.4 9.7 3.9 4.4 5.4 8.7 4.4 La 20.5 20.7 10.3 50.3 2.5 7.4 15.1 9.2 15.2 13.6 10.6 19.7 25.4 Ce 24.8 38.9 21.1 22.2 27.7 29. 20.6 19. 30.9 24.2 19.5 25.3 23.9 Pr 5.4 4.6 2.7 2.6 3. 3.4 2.4 2.4 3.7 2.8 2.3 4.9 2.8 Nd 19.1 15.5 10.8 9.5 11.1 12.5 8.3 8.9 12.9 10. 8.1 16.4 9.5 Sm 3.7 2.9 2.6 1.9 2. 2.3 1.6 1.7 2.3 1.9 1.4 3.1 1.5 Eu 0.7 0.5 0.4 0.4 0.4 0.5 0.3 0.5 0.5 0.3 0.3 0.6 0.3 Gd 2.9 2.7 2.5 1.8 2.2 1.9 1.3 1.9 1.8 1.6 1.4 2.7 1.5 Tb 0.4 0.4 0.4 0.3 0.3 0.3 0.2 0.3 0.2 0.2 0.2 0.3 0.2 Dy 2. 2.2 2.6 2. 1.7 1.7 1. 2.2 1.1 1. 1.1 2. 1.1 Ho 0.3 0.4 0.5 0.4 0.3 0.3 0.1 0.4 0.2 0.2 0.2 0.4 0.7 Er 1.1 1.2 1.7 1.4 0.9 1. 0.6 1.4 0.6 0.6 0.5 1.3 0.5 Tm 0.1 0.1 0.2 0.2 0.1 0.1 0.1 0.1 0.1 0.1 0.1 0.2 0.1 Yb 0.7 1.2 1.5 1.1 0.7 0.8 0.6 1.1 0.7 0.6 0.4 1.4 0.6 Lu 0.1 0.2 0.2 0.2 0.1 0.1 0.1 0.2 0.1 0.1 0.1 0.2 0.1 ∑REE 102.5 105 80.7 114.6 71.5 79.5 67.1 64. 80.3 71. 61.7 95.2 85. Note: LOI: Loss on ignition; n.d.: not determined

Journal of Applied Geology 133 AMINUDDIN et al. wherein the resulting ratios primarily reflect the 5D ISCUSSION relative contents of feldspar, quartz, and clay 5.1 Metamorphism type and metamorphic mineral present. It would further help define facies the samples’ schematic variation fields as either Within the research area, various metasedi- graywackes, pelites, arkoses, or others. How- mentary rocks are present, including products ever, the overall variation of the SiO /Al O 2 2 3 of contact and regional metamorphisms. The (2.5–8.7) and K O/Na O (1.4–8.5) ratios was 2 2 contact metamorphism is believed to be re- limited. In particular, most of the samples could lated to the contact between Kemahang gran- be categorized into the graywacke field, while ite and rocks that are hornfelsic in texture. four samples were of the pelitic graywacke The contact is typically permeated with the field. Meanwhile, only one sample was plotted development of quartzo-feldspathic minerals on the quartz-rich greywacke field. (Hutchison, 2009 and Khoo, 1980). The re- The SiO /Al O vs. Fe O /K O diagram 2 2 3 2 3 2 gional type of metamorphism is a part of oro- (Herron, 1988) in Figure 6 depicts the rocks un- genic metamorphism, which typically produces der the study’s protoliths to be wacke deriva- rock texture with good foliation. The contact tives shale, litharenite, and arkose. In par- and regional metamorphisms can be grouped ticular, the schists with litharenitic protoliths into high and medium dT/dP metamorphism yielded higher concentrations of SiO (>77%), 2 realms, respectively, according to Palin et al. Na O, and CaO. This outcome is in line with 2 (2020) on their work of apparent peak metamor- the high metamorphic plagioclase content and phic temperature/pressure (dT/dP) gradients would possibly depict the detrital plagioclase through time. Therefore, the contact metamor- present in the sedimentary protolith (Lopez et phism (high dT/dP) in this region is related to al., 2018). Moreover, the high SiO concen- 2 the island and continental arcs at the conver- trations observed in the samples plotted near gent plate margins, continental rifts, hot spots, the litharenites indicated the significant impact and large margins, deep-seated batholiths. In of quartz debris in the sedimentary environ- contrast, the regional metamorphism (medium ment. The schists containing shale and wacke dT/dP) is related to over thickened continental protoliths revealed lower SiO concentrations 2 crust due to accretional or collisional orogeny (<72%), but high Al O ,K O, FeO, and MgO 2 3 2 tectonic regime. contents were in line the higher mica and chlo- Most of the metasedimentary rocks found rite concentrations. within the Taku Schist region were grouped 4.3.2 Rare earth element geochemistry into greenschist facies due to the major pres- The chondrite-normalized rare earth elements ence of chlorite, muscovite, and biotite miner- (REE) patterns of the rock samples under study als in the rock samples. According to Winter are portrayed in Figure 7. Similar chondrite- (2001), this greenschist facies formed at depths normalized REE patterns were observed for all of 5–35 km with a pressure condition of 0.1– samples about the Post Archaean Australian 1 GPa and temperatures of 280–500°C. Mean- Shales (PAAS). However, all samples initially while, the amphibolite facies are characterized have lower REE contents and exhibit lower than by the presence of staurolite minerals in the PASS REE normalized values. This could be rock samples. These amphibolite facies rocks characterized by LREE enrichment and a slight are suggested to form at depths of 8–40 km with negative Eu anomaly in the samples, suggest- a pressure condition of 0.2–1.2 GPa and temper- ing the primary sedimentary source was con- atures of 500–700°C (Winter, 2001). tinental crustal rocks in nature (Tang et al., 5.2 Protolith 2012). The Tm negative anomaly indicates Roser and Korsch’s (1988) work has evolved the non-carbonaceous sedimentary rock (Jean- the available discriminant functions to involve Alix, 2016). Three samples (2102A, 2003E, and major elements in distinguishing the sedi- 2003A) with the lower normalized REE values ments as a derivative of felsic, intermediate, showed a steeper slope from LREE to HREE and mafic igneous quartzose sedimentary pro- (red shaded) compared to other samples.

134 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

10 2001A (Grs) 2107A (Grs) 8 Quartz-rich graywacke Quartz-rich arkose 2105B (Grs) 2103A (Grs)

3 Graywacke 2105A (Grs)

O 6 2 2106A (Grs) Arkose

/Al 2106B (Grs) 2 4 2101A (Grs) SiO 2102A (Grs) 2003E (Grs) 2 Peli�c graywacke Pelite 2003A (Grs) 2104A (Grs) 0 1901A (Amp) 1 10 100 K2O/Na2O

Figure 5: Sample distribution on the SiO2/Al2O3 – K2O/Na2O diagram. The FIGURE 5. Sample distribution on the SiO /Al O –K O/Na O diagram. The subdivision of the composition subdivision of the composition2 field2 3into2 pelitic2 graywackes, graywacke, quartz- field into pelitic graywackes, graywacke, quartz-rich graywacke, pelite, arkose, and quartz-rich arkose is rich graywacke, pelite, arkose and quartz-rich arkose is after Wimmenauer after Wimmenauer (1984). Most of the samples belong to the graywackes field, only four samples belong to (1984). Most of the samples belong to the graywackes field, only four samples the pelitic graywackes field, and only one was plotted on quartz-rich graywacke. belong to pelitic graywackes field and only one was plotted on quartz-rich graywacke. 1.0 2001A (Grs) 0.8 Fe-shale Fe-sand 2107A (Grs) 2105B (Grs) 0.6

O) 2103A (Grs) 2 0.4 2105A (Grs) /K 3 Shale Wacke Litharenite Sublitharenite 2106A (Grs) O 2 0.2 2106B (Grs) 0.0 2101A (Grs) 2102A (Grs)

Log (Fe -0.2 2003E (Grs) Arkose Subarkose -0.4 2003A (Grs) 2104A (Grs) -0.6 1901A (Amp) 0.2 0.4 0.6 0.8 1.0 1.2 1.4 1.6 Log (SiO2/Al2O3)

Figure 6: Plot of Log (Fe O /K O) versus Log (SiO /Al O ) of the analyzed FIGURE 6. Plot of log (Fe O /K O) versus2 log3 (SiO2 /Al O ) of the analyzed2 2 samples3 within the composition samples within2 composition3 2 fields proposed2 2 3by Herron (1988). Almost all of the fields proposed by Herron (1988). Almost all of the studied rock samples were plotted on the wacke field. Three samplesstudied were rock plotted samples on the were shale field, plotted while on two the other wacke samples field. were Three plotted samples on the litharenite were field. plotted on the shale field while two other samples were plotted on the litharenite field. 1000 2001A (Grs) 2107A (Grs) 2105B (Grs) 100 2103A (Grs) 2105A (Grs) PAAS 2106A (Grs) 10 2106B (Grs) 2101A (Grs) 2102A (Grs) Sample/Chondrite 1 2003E (Grs) 2003A (Grs) 2104A (Grs) 1901A (Amp) 0.1 PAAS La Ce Pr Nd Sm Eu Gd Tb Dy Ho Er Tm Yb Lu

Figure 7: Chondrite-normalized REE patterns of the rock samples under study. The FIGURE 7.normalization Chondrite-normalized factors were REE referred patterns from of the MacDonough rock samples and under Sun study. (1995). The normalization The studied factors were referredsamples from demonstrated MacDonough similar and chondrite-normalizedSun (1995). The studied REE samples patterns demonstrated with the Post similar Archaean chondrite- normalizedAustralian REE patterns Shales with(PAAS) the provided Post Archaean by (McLennan, Australian 1989). Shales (PAAS) provided by (McLennan 1989).

Journal of Applied Geology 135 AMINUDDIN et al. tolith. Therefore, a plot of the rock samples’ terranes that sutures together as a result of chemical compositions under study (Figure 8) the Indosinian Orogeny. In particular, contact revealed them to be predominantly derived and regional metamorphisms of greenschist to from the quartzose sedimentary protolith. This amphibolite facies were near the Triassic and is described in Figure 8a, wherein only four Cretaceous intrusions such as the Kemahang samples could be plotted outside the quart- Granite. In the chemical classification efforts, zose sedimentary protolith. Moreover, only one the Taku Schist’s metasedimentary rocks were sample (2104A) is plotted in the intermediate found to consist of greywacke and shale. They igneous protolith as seen in Figure 8a and Fig- could also be grouped into the quartzose sed- ure 8b both, which is attributable to the high imentary protolith and the Continental Island Al2O3 and FeO concentrations and relatively Arc (CIA) in the context of their tectonic set- low concentration of SiO2. tings. Additionally, the Taku Schist’s metasedimentary rocks would be subjected to several 5.3 Tectonic setting episodes of contraction that would amalga- In general, chemical data is a beneficial instru- mate the Sibumasu sedimentary cover with ment in assessing the tectonic setting for an- the accretionary wedge and genetically corre- cient sedimentary depositional environments. lated Bentong-Raub mélange towards different Accordingly, Bhatia and Crook (1986) have greenschist to amphibolite facies conditions of positioned varying discriminant diagrams of varying depths in relation with the upper plate tectonic environments concerning sedimentary of the Sukhothai Arc. rocks’ geochemical attributes. Henceforth, the TiO2 vs. Fe2O3 + MgO ratio (Figure 9a) were ACKNOWLEDGEMENTS considered, wherein most of the samples were The authors would like to thank the editor and plotted onto the Continental Island Arc (CIA) two anonymous reviewers for their construc- field. In contrast, several others were plotted tive comments to improve the manuscript. Our onto the Active Continental Margin (ACM) thanks also go to staff members of Geologi- field. However, immobile trace elements were cal Engineering Department, Universitas Gad- known to be highly beneficial in the identifica- jah Mada (UGM), Indonesia; School of Material tion of paleotectonic environments for metased- and Mineral Resources Engineering, Universiti imentary deposits, such as Ti, Sc, Zr, La, and Th. Sains Malaysia (USM), Malaysia; and Depart- Therefore, the Ti/Zr vs. La/Sc diagram (Bhatia ment of Earth Resources Engineering, Kyushu and Crook, 1986) allowed the visual correlation University, Japan, for their supports during this between the analyzed samples with the CIA research was carried out. This work is a part of and ACM settings (Figure 9b). Moreover, a pro- a Ph.D. study supported by JICA AUN/SEED- jection into the diagram of La vs. Th (Figure 9c) Net scholarship. reveals that the protolith deposits were com- parable to those found in modern continental REFERENCES island arc basins. Additionally, the ternary di- Ali, Md.M.A., Willingshofer, E., Matenco, L., Fran- agrams of La–Th–Sc and Th–Sc–Zr/10 yielded cois, T., Daanen, T.P., Ng, T.F., Taib, N.I., and the samples under study as a group of the CIA Shuib, M.K. (2016) Kinematics of post-orogenic field (Figures 10a and 10b). extension and exhumation of the Taku Schist, NE Peninsular Malaysia. Journal of Asian Earth Sci- 6C ONCLUSION ences. 127:63-75. Bhatia, M.R., and Crook, K.A.W. (1986) Trace ele- The petrographic analysis results show the ment characteristics of graywackes and tectonic Taku Schist form of sediments and subordi- setting discriminant of sedimentary basins. Con- nate magmatic rocks were metamorphosed to tributions to Mineralogy Petrology. 92:181-193. greenschist-amphibolite facies; in lines with Bignell, J.D. and Snelling, N.J. (1977) K-Ar ages the progression of Indosinian Orogeny, which on some basic igneous rocks from Peninsula revealed the Western and Eastern Belts of Malaysia and Thailand. Bulletin of the Geological Society of Malaysia 8:89-93. Peninsular Malaysia represent the lateral ex- Ferrari, O.M., Hochard, C., and Stampfli, G.M. tensions of the S-type Sibumasu and Indochina

136 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

(a) 8 2001A (Grs) 6 2107A (Grs) Intermediate 4 Felsic Igneous 2105B (Grs) Igneous 2 Provenance 2103A (Grs) 2105A (Grs) 0 2106A (Grs) F2 -2 2106B (Grs) -4 2101A (Grs) 2102A (Grs) -6 Quartzose Maﬁc Igneous 2003E (Grs) -8 Sedimentary Provenance 2003A (Grs) -10 2104A (Grs) 1901A (Amp) -8 -6 -4 -2 0 2 4 6 8 10 F1

(b) 8 2001A (Grs) 6 Quartzose 2107A (Grs) 4 Sedimentary 2105B (Grs) 2 Provenance 2103A (Grs) Maﬁc Igneous 2105A (Grs) 0 2106A (Grs)

F4 Provenance -2 2106B (Grs) -4 2101A (Grs) 2102A (Grs) Felsic Igneous -6 2003E (Grs) Intermediate Provenance -8 Igneous 2003A (Grs) Provenance -10 2104A (Grs) 1901A (Amp) -15 -10 -5 0 5 10 F3

FIGURE 8. Discriminant diagrams of the rock samples (after Roser and Korsch, 1988). The samples were Figureprone to be8: classiﬁed Discriminant as quartzose diagrams sedimentary of protolith.the rock However, samples several (after samples Roser were and plotted Korsch, on the 1988).felsic and The intermediate samples igneous were protoliths. prone F1 = to -1.773 be× TiO classified2 + 0.607 × asAl2 O quartzose3 + 0.76×Fe2 O sedimentary3 - 1.5×MgO + provenance.0.616×CaO + 0.509 However,×Na2O - 1.224 several×K2O - 9.09, samples F2 = 0.445 × wereTiO2 + 0.07 plotted×Al2O3 - on 0.25 × theFe2O 3 - felsic 1.142× MgO and + 0.438×CaO + 1.475×Na2O + 1.426×K2O - 6.861, F3 = 30.638×TiO2/Al2O3 - 12.541×Fe2O3/Al2O3 intermediate igneous provenances. F1=−1.773TiO2 + 0.607Al2O3 + 0.76Fe2O3 − + 7.329×MgO/Al2O3 + 12.031×Na2O/Al2O3 + 35.4×K2O/Al2O3 - 6.382 and F4 = 56.5×TiO2/Al2O3 - 1.5MgO10.879×Fe 2O +3/Al 0.616CaO2O3 + 30.875 ×MgO/Al + 0.509Na2O2O3 - 5.404× −Na 2O/Al 1.224K2O3 +2 11.11O- × 9.09,K2O/Al 2 F2=0.445TiOO3 - 3.89. 2 + 0.07Al2O3 - 0.25Fe2O3 − 1.142MgO + 0.438CaO + 1.475Na 2O + 1.426K2O - 6.861, F3=30.638TiO2/Al2O3 - 12.541 Fe2O3/Al2O3 + 7.329MgO/Al2O3 + 12.031 Na2O/Al2O3 + 35.4 K2O/Al2O3 - 6.382 and F4=56.5TiO2/Al2O3 - 10.879Fe2O3/ Al2O3 + 30.875MgO/Al2O3 - 5.404Na2O/Al2O3 + 11.11K2O/Al2O3 - 3.89.

Journal of Applied Geology 137 AMINUDDIN et al.

(a) 1.4 2001A (Grs) 1.2 2107A (Grs) 2105B (Grs) 1.0 2103A (Grs) OIA 2105A (Grs) 0.8 2106A (Grs)

(wt %) (wt 2106B (Grs) 2 0.6 2101A (Grs)

TiO CIA 2102A (Grs) 0.4 ACM 2003E (Grs) PM 2003A (Grs) 0.2 2104A (Grs) 1901A (Amp) 0.0 0 2 4 6 8 10 12 14 16 Fe2O3 + MgO (wt%)

(b)

2001A (Grs) 60 2107A (Grs) 2105B (Grs) OIA 2103A (Grs) 2105A (Grs) 40 2106A (Grs) 2106B (Grs) 2101A (Grs) Ti/Zr 2102A (Grs) 20 ACM 2003E (Grs) 2003A (Grs) CIA 2104A (Grs) PM 1901A (Amp) 0 0 2 4 6 8 10 12 La/Sc

(c) 70 2001A (Grs) 60 2107A (Grs) 2105B (Grs) 50 2103A (Grs) ACM 2105A (Grs) 40 2106A (Grs) CIA 2106B (Grs) 30 2101A (Grs)

La (ppm) 2102A (Grs) 20 2003E (Grs) OIA 2003A (Grs) 10 2104A (Grs) 1901A (Amp) 0 0 5 10 15 20 25 30 35 Th (ppm)

Figure 9: Discriminant diagrams depicting potential tectonic setting for the studied FIGURE 9. Discriminant diagrams depicting potential tectonic setting for the studied rocks. (a) By using the rocks. (a) By using TiO (wt.%) vs. Fe O +MgO (wt.%) diagram (after Bhatia and TiO (wt.%) vs. Fe O +MgO (wt.%)2 diagram (after2 Bhatia3 and Crook, 1986), most of the samples could be 2 Crook, 1986),2 3 most of the samples could be plotted onto the CIA field with several plotted onto the CIA field with several samples onto the ACM field. (b) Using Ti/Zr vs. La/Sc diagram (after samples onto the ACM field. (b) By using Ti/Zr vs. La/Sc diagram (after Bhatia and Bhatia and Crook, 1986), the analyzed samples could correlate with the CIA and ACM settings. (c) By using Crook, 1986), the analyzed samples could correlate with the CIA and ACM settings. La (ppm) vs. Th (ppm) diagram (after Bhatia and Crook, 1986), the samples mostly belong to the CIA field. ACM:(c) active By continental using La margin,(ppm) vs.CIA: Th continental (ppm) diagram island arc, (after OIA: oceanic Bhatia island and arc, Crook, PM: passive1986), margin. the samples mostly belong to the CIA field. ACM: active continental margin, CIA: continental island arc, OIA: oceanic island arc, PM: passive margin. 138 Journal of Applied Geology PETROGRAPHYAND GEOCHEMISTRYOF METASEDIMENTARY ROCKSFROMTHE TAKU SCHIST,KELANTAN

(a) La Terrigenous Sands and Shales from Core or Log Data. Journal of Sediment Petrology. 58:820-829. Hutchison, C.S. (1975) Ophiolite in Southeast Asia. 2001A (Grs) 2107A (Grs) Geological Society America Bulletin. 86: 797-806. 2105B (Grs) 2103A (Grs) Hutchison, C.S. (2009) Metamorphism. In Geology 2105A (Grs) st 2106A (Grs) ACM of Peninsular Malaysia, 1 ed.; Hutchison, C. S., 2106B (Grs) 2101A (Grs) Tan, D. N. K, Eds.; The University of Malaya 2102A (Grs) CIA 2003E (Grs) and The Geological Society of Malaysia: Kuala 2003A (Grs) Lumpur, Malaysia. 2104A (Grs) OIA 1901A (Amp) Imai, N., Terashima, S., Itoh, S., and Ando, A. (1995) 1994 compilation of analytical data for minor and trace elements in seventeen GSJ geochemical ref- Th Sc erence samples, "Igneous rock series". Geostan- dards Newsletter. 19:135-213. (b) Th Jean-Alix, B., Dauphas, N., Gillet, P., Bollinger, C., Joel, E., Bischoff, A., and Yamaguchi, A. (2016) 2001A (Grs) 2107A (Grs) Evidence from Tm anomalies for non-Cl refrac- 2105B (Grs) 2103A (Grs) tory lithophile elements proportions in terrestrial 2105A (Grs) planets and achondrites. Geochimica et Cos- 2106A (Grs) 2106B (Grs) mochimica Acta. 176:1-17. 2101A (Grs) 2102A (Grs) Khoo, T.T. (1980) Some comments on the emplace- 2003E (Grs) 2003A (Grs) ACM ment level of the Kemahang granite, Kelantan. 2104A (Grs) 1901A (Amp) Bulletin of the Geological Society of Malaysia. PM 13:93-101. CIA Khoo, T.T. and Lim, S.P. (1983) Nature of the con- OIA tact between the Taku Schists and adjacent rocks Sc Zr/10 in the Manek Urai area, Kelantan and its im- Figure 10: Triplots of discriminant diagrams for the tectonic setting plications. Geological Society Malaysia Bulletin. FofIGURE the analyzed10. rocks. Triplots (a) La-Th-Sc of discriminant diagram (after Bhatia diagrams and Crook, for 16:139-158. 1986). (b) Th-Sc-Zr/10 diagram (after Bhatia and Crook, 1986). theMost of tectonic the studied setting samples of were the plotted analyzed on the Continental rocks. Island (a) Lopez, J.P., Bellos, L.I., Diaz-Alvarado, J., and Cas- La–Th–ScArc (CIA) field. diagram ACM: active (after continental Bhatia margin, andCrook, CIA: continental 1986). tro, A. (2018) Hybridization between I-type and S- island arc, OIA: oceanic island arc, PM: passive margin. (b) Th–Sc–Zr/10 diagram (after Bhatia and Crook, type granites in the Ordovician Famatinian mag- 1986). Most of the studied samples were plotted on matic arc, Tafi del Valle, Tucuman, NW Argentina. the Continental Island Arc (CIA) field. ACM: ac- Geologica Acta. 16:25-43. tive continental margin, CIA: continental island arc, MacDonald, S. (1968) The Geology and Mineral Re- OIA: oceanic island arc, PM: passive margin. sources of North Kelantan and North Tereng- ganu; Geological Survey West Malaysia: Ipoh, Malaysia. (2008) An alternative plate tectonic model for McDonough, W.F. and Sun, S. (1995) The composi- the Palaeozoic-Early Mesozoic Palaeotethyan tion of the Earth. Chemical Geology. 120:223-253. evolution of Southeast Asia (Northern Thailand- McLennan, S.M. (1989) Rare earth elements in sedi- Burma). Tectonophysics. 451:345-365. mentary rocks: Influence of provenance and sed- Francois, T., Md Ali, M.A., Matenco, L., Willing- imentary processes. Reviews in Mineral. 21:169- shofer, E., Ng. T.F., Taib, N.I., and Shuib, M.K. 200. (2017) Late Cretaceous extension and exhumation Metcalfe, I. (2000) The Bentong-Raub Suture Zone. of the Stong and Taku magmatic and metamor- Journal of Asian Earth Sciences. 18:691-712. phic complexes, NE Peninsular Malaysia. Journal Metcalfe, I. (2002) Permian tectonic framework and of Asian Earth Sciences. 143:296-314. paleogeography of SE Asia. Journal of Asian Ghani, A.A. (2000) Mantled feldspar from the Nor- Earth Sciences. 20:551-566. ing granite, Peninsular Malaysia: petrography, Metcalfe, I. (2013) Tectonic evolution of the Malay chemistry, and petrogenesis. Bulletin of the Ge- Peninsula. Journal of Asian Earth Sciences. ological Society of Malaysia. 44:109-115. 76:195-213. Ghani, A.A., Searle, M., Robb, L., and Chung, S.-L. Morley, C.K. (2012) Late Cretaceous-Early Palaeo- (2013) Transitional I-S type characteristics in the gene tectonic development of SE Asia. Earth- Main Range Granite, Peninsular Malaysia. Jour- Science Reviews. 115:37-75. nal of Asian Earth Sciences. 76:225-240. Ng, S.W.P., Whitehouse, M.J., Searle, M.P., Robb, Herron, M.M. (1988) Geochemical Classification of L.J., Ghani, A.A., Chung, S.L., Oliver, G.J.H.,

Journal of Applied Geology 139 AMINUDDIN et al.

Sone, M., Gardiner, N.J., and Roselee, M.H. Searle, M.P., Whitehouse, M.J., Robb, L.J., Ghani, (2015) Petrogenesis of Malaysian granitoids in A.A., Hutchison, C.S., Sone, M., Ng, S.W.-P., Rose- the Southeast Asian tin belt: Part 2. U-Pb zircon lee, M.H., Chung, S.-L., and Oliver, G.J.H. (2012) geochronology and tectonic model. Geological Tectonic evolution of the Sibumasu-Indochina Society America Bulletin. 127:1238-1258. terrane collision zone in Thailand and Malaysia: Palin, R.M., and Dyck, B.J. (2020) Metamorphism of constraints from new U-Pb zircon chronology of Pelitic (Al-rich) Rocks. Encyclopedia of Geology, SE Asian tin granitoids. Journal of the Geological 2nd Edition: Reference Module in Earth Systems Society. 169:489-500. and Environmental Sciences, Elsevier. Palin, R.M., Santosh, M., Cao, W., Li, S.S., Tang, Y., Sang, L., Yuan, Y., Zhang, Y., and Yang, Hernández-Uribe, D., and Parsons, A. (2020) Y. (2012) Geochemistry of Late Triassic pelitic Secular change and the onset of plate tectonics on rocks in the NE part of Songpan-Ganzi Basin, Earth. Earth-Science Reviews. 207:103-172. western China: Implications for source weather- Ridd, M.F. (2012) The role of strike-slip faults in the ing, provenance, and tectonic setting. Geoscience displacement of the Palaeotethys suture zone in Frontiers. 3(5):647-660. Wimmenauer, W., 1984. Southeast Thailand. Journal of Asian Earth Sci- The pre Variscan crystalline basement of the Black ences. 51:63-84. Forest. In German. Fortschr. Mineral. 62:69-86. Roser, B.P. and Korsch, R.J. (1988) Provenance Signa- tures of Sandstone-Mudstone Suites Determined Winter, J.D. (2001) An Introduction to Igneous and Using Discriminant Function Analysis of Major- Metamorphic Petrology; Prentice-Hall Inc.: Up- Element Data. Chemical Geology. 67:119-139. per Saddle River, New Jersey.

140 Journal of Applied Geology