Vanachawan Hunyek
Chakkaphan Sutthirat
Alongkot Fanka- Department of Geology, Faculty of Science, Chulalongkorn University, Bangkok, Thailand
Volcanic rocks and associated dikes have been exposed in Wang Nam Khiao area, Nakhon Ratchasima Province, northeastern Thailand where complex tectonic setting was reported. These volcanic rocks are classified as rhyolite, dacite, and andesite whereas dikes are also characterized by andesitic composition. These dikes clearly cut into the volcanic rocks and Late Permian hornblende granite in the adjacent area. Rhyolite and dacite are composed of abundant plagioclase and quartz whereas andesite and andesitic dike contain mainly plagioclase and hornblende with minor quartz. The volcanic rocks typically show plagioclase and hornblende phenocrysts embedded in fine-grained quartz and glass groundmass whereas dike rocks contain less glass matrix with more albitic laths. P–T conditions of crystallization are estimated, on the basis of Al-in-hornblende geobarometry and hornblende geothermometry, at about 4.5–5.5 kbar, 861–927°C and 4.8–5.5 kbar, 873–890°C for the magma intrusions that fed volcanic rocks and andesitic dikes, respectively. Whole-rock geochemistry indicates that these rock suites are related to calc-alkaline hydrous magma. The enriched large-ion lithophile elements (LILE; e.g., Rb, Sr) and depleted high-field-strength elements (HFSE; e.g., Nb, Ce, Ti), with similar rare earth element (REE) patterns indicate arc magmatism. The results of this study are comparable with the continental arc magmatism along the Loei Fold Belt (LFB) as a consequence of the Late Permian Palaeo-Tethys subducted beneath Indochina Terrane.
Introduction
Thailand and SE Asia are assembled from several tectonic terranes across from east to west (Bunopas, 1981; Charusiri et al., 2002; Sone and Metcalfe, 2008) including Indochina Terrane (Bunopas, 1981; Charusiri et al., 2002; Sone and Metcalfe, 2008), Loei Fold Belt (LFB; Bunopas, 1981), Sukhothai Terrane (Sone and Metcalfe, 2008), and Sibumasu (Sone and Metcalfe, 2008) or Shan-Thai Terrane (Bunopas, 1981; Charusiri et al., 2002), respectively (Figure 1). These terranes present diverse magmatic rocks, both plutonic (e.g., Cobbing et al., 1986, 1992; Nakapadungrat and Putthapiban, 1992; Charusiri et al., 1993; Searle et al., 2012; Ng et al., 2015a, b) and volcanic rocks (e.g., Jungyusuk and Khositanont, 1992; Intasopa, 1993; Intasopa and Dunn, 1994; Panjasawatwong et al., 2006; Barr and Charusiri, 2011; Boonsoong et al., 2011) corresponding to tectonic events in several episodes (Bunopas, 1981; Charusiri et al., 2002).
Figure 1. (A) Index map of Thailand showing the study location and the main tectonic terranes including Indochina Terrane; Sibumasu (Shan-Thai) Terrane; Loei Fold Belt (LFB); Sukhothai Terrane (ST); Chanthaburi Terrane (CT) (modified from Charusiri et al., 2002; Sone and Metcalfe, 2008; Sone et al., 2012; Metcalfe, 2013; Zaw et al., 2014). (B) Geological map of the study area, Wang Nam Khiao area, Nakhon Ratchasima, and sample locations of this study (modified after Putthaphiban et al., 1989a, b; Kemlheg and Wichidchalermpong, 1992a, b).
The LFB is located along the western edge of the Indochina Terrane (Figures 1, 2). In LFB, plutonic rocks have been defined as the Eastern Granite Belt of Thailand (Nakapadungrat and Putthapiban, 1992; Charusiri et al., 1993) whereas volcanic rocks, mostly reported in the northern part of LFB especially in Loei (Panjasawatwong et al., 2006; Kromkhun et al., 2013), Phetchabun (Boonsoong et al., 2011; Vivatpinyo et al., 2014), and Nakhon Sawan (Khositanont et al., 2008) areas, belong to Loei–Phetchabun–Ko Chang Volcanic Belt (Jungyusuk and Khositanont, 1992) (Figure 2). The main Late Permian–Triassic, Devonian–Carboniferous, and Silurian volcanic rocks have also been reported (Intasopa and Dunn, 1994; Panjasawatwong et al., 2006; Zaw et al., 2007; Boonsoong et al., 2011). These rocks resulted from amalgamation of tectonic terranes containing multiple generations of successive arc-related magmatic events (Charusiri et al., 2002; Zaw et al., 2014). Therefore, the magmatic rocks through the LFB, especially in the central and southern parts lacking of geological study (Figure 2), are very important to understand magmatism and tectonic evolution of the western Indochina Terrane.
Figure 2. Map shows distribution of the magmatic rocks in Thailand including the granite belts (modified after Nakapadungrat and Putthapiban, 1992) and volcanic rocks (Jungyusuk and Khositanont, 1992) together with the main tectonic terranes (modified from Charusiri et al., 2002; Sone and Metcalfe, 2008; Metcalfe, 2013; Zaw et al., 2014). Zircon U–Pb ages of the magmatic rocks in Loei Fold Belt are also present in the map. Abbreviations: LFB, Loei Fold Belt; ST, Sukhothai Terrane; CT, Chanthaburi Terrane.
The study area, Wang Nam Khiao in Nakhon Ratchasima province, Central Thailand, is located in the critical junction of several tectonic terranes (Figure 1A) where volcanic rocks and related dikes are also exposed. Detailed investigation of these rocks has never been reported; therefore, this study provides the results coming from petrology, mineral chemistry, and whole-rock geochemistry of these rocks before reconstruction of magmatic process and tectonic model of the area. The results are used to constrain the magmatic–tectonic scenario of central Thailand in the frame of the Indochina Terrane amalgamation during Carboniferous–Triassic.
Geological Setting
Pre-Cenozoic volcanic, pyroclastic, and hypabyssal rocks in Thailand have been reported (e.g., Jungyusuk and Khositanont, 1992; Barr and Charusiri, 2011) mostly in the northern parts of Thailand (Figure 2). These rocks are divided into four volcanic belts (Jungyusuk and Khositanont, 1992) including Loei–Phetchabun–Ko Chang, Nan–Uttaradit, Chiang Khong–Tak, and Chiang Rai–Chiang Mai Volcanic Belts placing along N-S from east to west, respectively (Figure 2).
Loei–Phetchabun–Ko Chang Volcanic Belt extends from Loei southward to Phetchabun, Nakhon Sawan, Wang Nam Khiao (the study area), and Ko Chang island in the Gulf of Thailand (Figure 2). Volcanic rocks in Loei area are divided into three sub-belts including the eastern, central, and western sub-belts, based on their magmatic events (Intasopa and Dunn, 1994). The eastern volcanic sub-belt is characterized mainly by rhyolite occurred in a magmatic arc environment in Early Silurian (zircon U–Pb ages of 428 ± 7, 434 ± 4 Ma by Khositanont et al., 2008) or Late Devonian (Rb–Sr isochron age of 374 ± 33 Ma by Intasopa and Dunn, 1994). The central volcanic sub-belt contains mainly pillow basalts, hyaloclastite, and breccia, which have formed during Late Devonian (Rb–Sr isochron age of 361 ± 11 Ma by Intasopa and Dunn, 1994) as mid-oceanic ridge and island-arc basalts (Panjasawatwong et al., 2006). The western volcanic sub-belt contains many types of rocks varying from andesite to dacite (Intasopa and Dunn, 1994; Boonsoong et al., 2011; Kromkhun et al., 2013), which extend to Phetchabun area (Boonsoong et al., 2011; Kamvong et al., 2014; Salam et al., 2014) and Laos (Qian et al., 2015). These volcanic rocks occurred as arc magmatism during Carboniferous to Middle Triassic (Zaw et al., 2007, 2014; Khositanont et al., 2008; Salam et al., 2014). Their ages were determined by zircon U–Pb dating such as of 230–254 Ma (Khositanont et al., 2008), 245.9–241.0 Ma (Kamvong et al., 2014), 245.9–258.6 Ma (Salam et al., 2014), 238–323 Ma (Zaw et al., 2007, 2014), and 314.6–349.6 Ma (Qian et al., 2015). In terms of the geochronology and geochemistry, this arc volcanism is comparable with the arc magmatism of plutonic rocks in Carboniferous to Triassic (Salam et al., 2014; Zaw et al., 2014; Fanka et al., 2016, 2018).
In the study area, Permo-Triassic volcanic rocks have also been reported (Putthaphiban et al., 1989a, b; Kemlheg and Wichidchalermpong, 1992a, b) in association with a plutonic complex (Fanka, 2016; Fanka et al., 2016, 2018). This complex includes hornblendite, hornblende gabbro, biotite granite, hornblende granite, and biotite–hornblende granite, defined as multiple arc magmatic events resulting from a Palaeo-Tethys subduction beneath Indochina Terrane during Late Carboniferous to Early Permian (zircon U–Pb ages of 314–285 Ma from biotite granite), Late Permian (zircon U–Pb ages of 253–257 Ma from hornblende granite and hornblende gabbro), and Middle Triassic (zircon U–Pb ages of 237 Ma from biotite–hornblende granite) (Fanka et al., 2018).
Materials and Methods
Representative volcanic rocks and related dikes were collected from the unweathered zones of Wang Nam Khiao area, Nakhon Ratchasima, northeast Thailand, for petrographic description, and mineral chemical and whole-rock geochemical analyses.
Microprobe analyses were performed on polished-thin sections using an electron probe micro-analyzer (EPMA JEOL JXA-8100). Analytical conditions were set up at 15 kV and about 2 μA beam current with a focus beam spot of 1 μm. Mineral and pure oxide standards were used for calibration at the same conditions followed by automatic ZAF correction and finally reported as weight percent oxides.
Nine volcanic rocks and two related dikes were subsequently selected and prepared for whole-rock geochemical analysis. Major and minor oxides were analyzed by an X-ray fluorescence spectrometer, Bruker AXS S-4 Pioneer along with rock standards (JG-2, JR-1, JG-1a, JB-1b, JA-2, GSP-2, BHVO-2, STM-1) for calibration. Loss on ignition (LOI) was calculated by the weight difference of the sample after heating in a furnace at 1050°C for 3 h. All research facilities reported previously are based at the Department of Geology, Faculty of Science, Chulalongkorn University.
In addition, the selected rock samples were digested using mixed hydrofluoric acid and nitric acid as suggested by Shapiro (1975) for analyses of trace and rare earth elements (REEs) using an inductively coupled plasma-mass spectrometer (ICP-MS) iCAP Q at the Scientific and Technological Research Equipment Centre, Chulalongkorn University.
Results
Field Survey and Petrographic Description
Volcanic rocks cover an area of about 10 × 12 km2 in the vicinity of Wang Nam Khiao (Figure 3A). Dikes are found cutting these volcanic rocks (Figure 3B) and the adjacent Late Permian hornblende granite (Figure 3C). These volcanic rocks are classified as rhyolite, dacite, and andesite whereas the dikes have andesitic composition. Rhyolite and dacite are usually light gray to gray (Figure 3A) and commonly show porphyritic texture. For andesite, apart from its greenish gray color resulting from enrichment of hornblende phenocrysts, the other appearances are similar to rhyolite and dacite phenocrysts. However, microscopic descriptions and geochemical analyses are meaningful for classification of these volcanic samples.
Figure 3. Exposures of (a) dacite, (b) andesite cut by andesitic dike, and (c) andesitic dike cut into Late Permian hornblende granite dated by Fanka et al. (2018). Photomicrographs taken in cross-polarized light showing mineral assemblages of (d) dacite, (e) andesite, and (f) andesitic dike. Descriptions of mineral assemblage and texture are reported in the main text. Mineral abbreviations: Q, quartz; Pl, plagioclase; Hb, hornblende; Opq, opaque minerals.
Microscopically, rhyolite and dacite similarly present abundant plagioclase phenocrysts (≤1 mm) with few hornblende phenocrysts (≤0.3 mm) embedded in fine-grained groundmass of quartz and plagioclase; moreover, their higher proportion of glass matrix (up to 30%) exhibits obviously vitrophyric texture (Figure 3D). Plagioclase phenocrysts are typically subhedral crystal showing significant albite twins with subordinate carlsbad–albite twins whereas hornblende phenocrysts are subhedral to euhedral. Andesite shows porphyritic texture with less glass matrix in comparison with rhyolite and dacite. Moreover, it comprises abundant phenocrysts (≤1 mm) of plagioclase and hornblende with equal proportion (Figure 3E) surrounded by fine-grained groundmass of quartz, plagioclase, and opaque minerals. Both plagioclase and hornblende phenocrysts are mostly subhedral to euhedral.
Andesitic dikes contain more abundances of subhedral–euhedral hornblende (≤1 mm) and subhedral–euhedral plagioclase laths (0.3–0.5 mm) with accessory opaque minerals and glass (Figure 3F). They typically show interstitial texture with plagioclase lath and hornblende. These textures are obviously different from the volcanic samples reported previously.
Mineral Chemistry
Microprobe analyses of plagioclase and hornblende are reported in Tables 1, 2, respectively, and are illustrated in Figure 4. Compositions of mineral are effectively used to estimate pressure and temperature of crystallization, which will be reported and discussed in Section “Temperature and Pressure Estimation.”
Table 1. Representative EPMA analyses of plagioclase in volcanic rocks and dikes from Wang Nam Khiao area, Nakhon Ratchasima, Thailand.
Table 2. Representative EPMA analyses of hornblende in volcanic rocks and dikes from Wang Nam Khiao area, Nakhon Ratchasima, Thailand.
Figure 4. Mineral chemical plots of (A) plagioclase (after Smith and Brown, 1974) and (B) calcic-amphibole (after Leake et al., 1997) from the volcanic rocks and related dikes in the Wang Nam Khiao area, Nakhon Ratchasima, Thailand.
Plagioclases are abundant in all samples of volcanic and dike samples (Figures 3D–F). Plagioclase in the volcanic rocks yielded similar compositional ranges; these are 2.01–2.02 wt.% CaO, 10.63–10.77 wt.% Na2O, and 0.32–0.47 wt.% K2O for rhyolite; 0.14–1.32 wt.% CaO, 10.83–11.67 wt.% Na2O, and 0.02–0.38 wt.% K2O for dacite; and 0.87–2.11 wt.% CaO, 10.73–11.24 wt.% Na2O, and 0.14–0.37 wt.% K2O for andesite (Table 1). Moreover, they are also compositionally similar to the plagioclase of the andesitic dikes with 1.17–2.19 wt.% CaO, 10.43–11.12 wt.% Na2O, and 0.06–0.44 wt.% K2O (Table 1). These plagioclases are mostly albites and few oligoclases, with the albite content ranging as Ab88–89 in the rhyolite, Ab92–99 in the dacite, Ab89–95 in the andesite, and Ab85–99 in the andesitic dikes (Figure 4A).
Amphiboles in all volcanic samples and andesitic dikes yielded similar compositional ranges with 47.01–48.51 wt.% SiO2, 9.34–11.13 wt.% Al2O3, 8.22–14.76 wt.% FeOt, 11.54–16.52 wt.% MgO, and 10.21–11.32 wt.% CaO. According to the international classification scheme, the analyzed amphiboles from all samples are classified as edenites (Figure 4B).
Whole-Rock Geochemistry
Major and minor compositions of the representative rhyolite, dacite, andesite, and related andesitic dikes in the Wang Nam Khiao area, Nakhon Ratchasima, Thailand, are shown in Table 3. These volcanic rocks and related dikes show slightly different major and minor compositions.
Table 3. Representative whole-rock geochemistry of volcanic rocks and related dikes from the Wang Nam Khiao area, Nakhon Ratchasima, Thailand (major and minor oxides in wt%, trace elements and REE in ppm).
SiO2 contents are expectedly higher in the rhyolite and lower in the andesite. The other major oxides of all volcanic rocks include 11.33–15.30 wt.% Al2O3, 1.90–10.27 wt.% FeOt, 2.64–7.53 wt.% CaO, 3.20–5.29 wt.% Na2O, and 1.88–2.54 wt.% K2O. Andesitic dikes present 54.60–59.78 wt.% SiO2, 11.74–13.02 wt.% Al2O3, 6.87–8.21 wt.% FeOt, 4.91–6.83 wt.% CaO, and 3.33–3.40 wt.% Na2O. These andesitic dikes display slightly higher MgO content (8.38–10.35 wt.%) than those of volcanic rocks (3.47–6.70 wt.% for andesite, 2.61–9.21 wt.% for dacite, and 1.52 wt.% for rhyolite). Na2O + K2O contents of dikes (4.70–5.55 wt.%) are similar to those of andesite (3.55–6.07 wt.%), which are lower than those of dacite (4.85–6.67 wt.%) and rhyolite (7.30 wt.%), respectively.
On a Nb/Y versus Zr/Ti diagram (Winchester and Floyd, 1977) (Figure 5), the analyzed samples plot in the fields of rhyolite, dacite, and andesite, accordingly. Harker variation diagrams (Harker, 1909) show negative correlation of SiO2 against TiO2, CaO, FeO, and MgO and positive correlations of SiO2 versus Na2O and K2O (Figure 6). These chemical charters are compatible with their mineral assemblages, especially increasing proportions of albite and quartz and decreasing proportion of hornblende from the andesite toward dacite and rhyolite, respectively. The linear correlations indicate that these rocks are related through a single magmatic differentiation.
Figure 5. Nb/Y versus Zr/Ti diagram (after Winchester and Floyd, 1977) indicating compositional ranges of andesite, dacite, and rhyolite of the rock samples.
Figure 6. Variation diagrams (Harker, 1909) of SiO2 against other major and minor oxides for (A–D) negative and (E–F) positive correlation of volcanic rocks and dikes in Wang Nam Khiao area, Nakhon Ratchasima, Thailand.
Primitive mantle-normalized spider diagrams (Figure 7A) of most rock samples reveal almost fractionation patterns from the large-ion lithophile elements (LILE) to high-field-strength elements (HFSE) with slightly positive anomalies of Rb, K, and Sr and negative anomalies of Nb, Ce, and Ti. In addition, the chondrite-normalized REE patterns of all rock types are slightly high in light REE (LREE) when data of chondrite from Sun and McDonough (1989) were used for normalization. Regarding chondrite-normalized La/Yb, (La/Yb)N ratios of dike samples (8.64–9.41) are in the range of volcanic rocks (6.05–14.54 for andesite, 10.77–21.86 for dacite, and 10.77 for rhyolite). In terms of (La/Sm)N ratios, volcanic rocks are 2.58 in the rhyolite, 2.58–5.89 in the dacite, and 2.35–3.06 in the andesite whereas andesitic dikes are 2.57–2.93. Moreover, the primitive mantle-normalized spider diagrams and chondrite-normalized REE patterns are comparable with the typical volcanic arc setting reported by Blein et al. (2001) and Reubi and Nicholls (2004); however, the samples’ patterns present slightly lower HREE than those typical volcanic arc patterns (Figures 7A,B).
Figure 7. (A) Primitive mantle-normalized spider diagrams (primitive mantle values from Sun and McDonough, 1989) and (B) chondrite-normalized REE patterns (chondrite values from Sun and McDonough, 1989) of the studied rocks and shade patterns volcanic rocks from typical arc setting (data from Blein et al., 2001; Jicha et al., 2004; Reubi and Nicholls, 2004; Jicha and Singer, 2006) for comparison.
Discussion
Temperature and Pressure Estimation
Microprobe data have been used to estimate pressure and temperature of crystallization in volcanic rocks as suggested by Kuprubasi et al. (2014). Although some mineral textures (e.g., zoned texture, corona texture, reaction rim, alteration) in volcanic rocks are not in equilibrium, the undisturbed single and/or coexisting minerals as phenocrysts can be used to estimate the P–T condition of crystallization (Foden and Green, 1992; Kuprubasi et al., 2014). Therefore, mineral compositions of undisturbed phenocrysts were used for the calculation of P–T conditions. Plagioclase compositions are sensitive to melt-water concentration (Lange et al., 2009) and alteration processes (Zhu and Lu, 2009; Hovelmann et al., 2010; Yuan et al., 2019); therefore, hornblende is efficiently used to calculate the P–T conditions (Schmidt, 1992; Ridolfi et al., 2010; Ridolfi and Renzulli, 2012). Al-in-hornblende geobarometer and hornblende geothermometer are employed to calculate the P–T conditions of crystallization in this study.
Ridolfi et al. (2010) proposed a hornblende geothermometer for the calc-alkaline volcanic system related to subduction based on the experimental data and natural data from worldwide calc-alkaline volcanoes, with the uncertain calibration of ±57°C by using the Silicon index (Si∗) of hornblende composition in the equation: T (°C) = −151.487Si∗ + 2041, where T is temperature and Si∗ = Si + ([4]Al/15) – (2[4]Ti) – ([6]Al/2) – ([6]Ti/1.8) + (Fe3+/9) + (Fe2+/3.3) + (Mg/26) + (BCa/5) + (BNa/1.3) – (ANa/15) + (A[Na + K]/2.3). Based on the hornblende geothermometry, calculated temperatures of the representative volcanic rocks vary from 861 to 927°C whereas the dike samples yield about 873 to 890°C (Table 2). These estimated temperatures are comparable with the crystallization temperature range of calibrated geothermometer for andesite–rhyolite in the calc-alkaline volcanic system (Ridolfi et al., 2010; Walker et al., 2013; Waters and Lange, 2015; Chen et al., 2017).
The Al-in-hornblende geobarometry has been widely used to calculate the pressure of magmatic crystallization (e.g., Hammarstrom and Zen, 1986; Schmidt, 1992; Helmy et al., 2004; Hossain et al., 2009) using the aluminum partition in hornblende, which was provided by experimental studies (Hollister et al., 1987; Johnson and Rutherford, 1989; Schmidt, 1992; Anderson and Smith, 1995). In this study, the calibration equation: Al-in-hornblende geobarometry P (kbar) = 4.76 Altot - 3.01 with error ± 0.6 kbar of Schmidt (1992) in the H2O-saturated condition was employed to calculate the pressure of magmatic crystallization. The calculated results are presented in Table 2. The calculated pressures of the volcanic rocks and related dikes fall in similar ranges of 4.5–5.5 and 4.8–5.5 kbar, respectively. As the calculated pressure from hornblende geobarometer has been used to indicate the depths of magma reservoir beneath arc volcanoes (Scott et al., 2012; Costa et al., 2013; Rivera et al., 2017), these calculated pressures can indicate the crystallization pressures of the phenocrysts from a magma reservoir that extruded to the surface.
Moreover, the pressures calculated from hornblende phenocrysts are used to estimate the depth by using the geobarometric gradient of 0.33 kbar/km (Bethel-Thompson et al., 2014). As a result, depths of crystallization are estimated at 14–17 km for the magma intrusion that fed volcanic rocks and dikes (Table 2). The depths should indicate the crystallization depths of the phenocrysts before complete crystallization of volcanic rocks at the shallower up to the surface. These depths (14–17 km) and the calculated temperature range of crystallization (861–927°C) indicate geothermal gradient of about 50–65°C/km which is comparable with an active continental margin (Rothstein and Manning, 2003; Annen et al., 2006; Chi and Reed, 2008). The combination of crystallization temperatures, pressure, and depths indicates that their original magmas should have stored and partially crystallized in the middle continental crust, which are the same provenance reported for plutonic rocks (e.g., hornblende granite, biotite–hornblende granite, biotite granite) in the adjacent area (Peacock, 1993; Winter, 2001; Kelemen et al., 2003; Richards, 2003; Fanka et al., 2018).
Petrogenesis
Based on petrochemistry, the studied volcanic rocks are classified as rhyolite, dacite, and andesite whereas the related dikes also show andesitic composition. Harker variation diagrams (Figure 6) present close relation of these rock types which reflect the same magmatic differentiation. Moreover, the most typical occurrences of hornblende in all rock types should imply crystallization of a hydrous magma (Foden and Green, 1992; Best, 2003). The hydrous magmatic model of these volcanic rocks and dikes is also supported by the hydrous calc-alkaline magmatism reported by Fanka et al. (2016, 2018) for the plutonic rocks in the Wang Nam Khiao area.
Enrichment of LILE (e.g., Rb, Sr) and depletion of HFSE (e.g., Nb, Ce, Ti) presented in Figure 7A suggest an arc-derived magmatic affinity in a subduction zone (Pearce, 1983; Ryerson and Watson, 1987; Kelemen et al., 1990, 1993; Ringwood, 1990; Blein et al., 2001; Reubi and Nicholls, 2004; Jicha et al., 2004; Jicha and Singer, 2006; Fanka et al., 2016, 2018). In addition, REE patterns of these rock samples (Figure 7B) also reflect fractionated pattern of magmatism.
In summary, all characteristics of petrography, geochemistry, and mineral chemistry features of volcanic rocks and related dikes indicate clearly that these rocks are derived from the calc-alkaline magmatic affinity related to continental arc margin. Their occurrences are supported by the multiple episodes of arc magmatism in the Wang Nam Khiao area, Nakhon Ratchasima suggested by Fanka et al. (2016, 2018) who have reported crucial evidences in terms of the ages of hornblendite and granitic rocks (Figure 1B).
Tectonic Implications
According to the field evidence, the dike clearly intrudes into the Late Permian hornblende granite (Figure 3C); therefore, this dike probably formed during/after the emplacement of the Late Permian hornblende granite. Moreover, the formation of the studied volcanic rocks and dikes can be combined with other magmatism in the study area (Figure 1) reported as multiple arc magmatism comprising Carboniferous biotite granite, Late and Triassic biotite–hornblende granite, and Permian hornblendite and hornblende gabbro (Figure 8). Moreover, the magmatic events of the studied rocks can be comparable with the magmatism from both plutonic rocks (e.g., Zaw et al., 2007, 2014; Khositanont et al., 2008; Salam et al., 2014) and volcanic rocks (e.g., Qian et al., 2015) in other areas belonging to LFB (Figure 2).
Figure 8. Zircon U–Pb ages of plutonic rocks and the estimated age of the dike cut into the Late Permian hornblende granite exposed in the Wang Nam Khiao area, Nakhon Ratchasima, Thailand (modified from Fanka et al., 2018).
Based on the geological data above together with the previous tectonic models in Thailand and SE Asia (e.g., Bunopas et al., 1989; Bunopas and Vella, 1992; Charusiri et al., 1993, 2002; Sone and Metcalfe, 2008; Barr and Charusiri, 2011; Searle et al., 2012; Zaw et al., 2014; Fanka et al., 2018), here, the tectonic evolution model indicating magmatism of the Wang Nam Khiao area in LFB is suggested in Figure 9.
Figure 9. Schematic tectonic evolution model and arc magmatism in the Wang Nam Khiao area, Nakhon Ratchasima belonging to Loei Fold Belt during (A) Carboniferous to Early Permian, (B) Late Permian, and (C) Middle Triassic (modified from Fanka et al., 2018).
The geological data have confirmed that the arc magmatisms along the LFB resulted from the Paleo-Tethys subduction beneath Indochina Terrane in several episodes (Fanka et al., 2016, 2018). According to geochronology of volcanic rocks in LFB, the magmatism might be started from Early Silurian (Khositanont et al., 2008) or Late Devonian (Intasopa and Dunn, 1994) as arc magmatism evidenced from the volcanic rocks in eastern volcanic sub-belt in Loei area. Moreover, these ages are supported by the ages of inherited zircons from Late Permian hornblende gabbro (Fanka et al., 2016) yielded zircon U–Pb ages of 444 ± 10 Ma, and inherited zircons from Carboniferous biotite granite (Fanka et al., 2018) yielded zircon U–Pb ages of 429 ± 24 Ma in the Wang Nam Khiao area (Figure 8).
In Carboniferous to Early Permian (Figure 9A), the subduction of Paleo-Tethys under Indochina Terrane (Bunopas, 1981; Sone and Metcalfe, 2008; Metcalfe, 2011, 2013; Fanka et al., 2018) generated the arc magmatism including Carboniferous biotite granite (zircon U–Pb ages of 314.6–287.9 Ma) in Wang Nam Khiao area (Fanka et al., 2018) (Figure 8), which is consistent with the occurrence of the plutonic rocks in Phetchabun area (zircon U–Pb ages of 323–310 Ma from Zaw et al., 2007) (Figure 2), and volcanic rocks along LFB, e.g., from the Muang Feuang and Pak Lay regions, Laos (zircon U–Pb ages of 349.6–314.6 Ma from Qian et al., 2015) (Figure 2).
Afterward, during the Late Permian, the magmatisms strongly occurred in the LFB evidenced from the exposures of various arc magmatic rocks including volcanic rocks and dikes in this study, Late Permian hornblende granite (zircon U–Pb ages of 253.4 ± 4.3 Ma from Fanka et al., 2018), hornblendite, and hornblende gabbro (zircon U–Pb ages of 257.1 ± 3.4 Ma from Fanka et al., 2016) in the Wang Nam Khiao area (Figures 2, 8). These rocks appear to have crystallized in different depths of the arc-related subduction between Paleo-Tethys and Indochina Terrane (Figure 9B). Moreover, the magmatisms in this period have also been reported widely along LFB (Figure 2) (e.g., Khositanont et al., 2008; Salam et al., 2014; Zaw et al., 2014). They are composed of plutonic rocks (e.g., zircon U–Pb ages of 254–250 Ma from Khositanont et al., 2008) and volcanic rocks (zircon U–Pb ages of 258.6–245.9 Ma from Salam et al., 2014).
Subsequently, in Middle Triassic, the arc magmatism related to subduction of Palaeo-Tethys and Indochina Terrane (Figure 9C) had still proceeded along with the formation of Middle Triassic biotite–hornblende granite (zircon U–Pb ages of 237.6 ± 3.8 Ma from Fanka et al., 2018) (Figure 8) and continued colliding until the Late Triassic (Sone and Metcalfe, 2008; Ridd, 2012; Kamvong et al., 2014; Salam et al., 2014) or Middle Jurassic (Nualkhao et al., 2018). This magmatic event is supported by the occurrence of the plutonic rocks in Pak Chong area (zircon U–Pb ages of 241 ± 6 Ma in Morley et al., 2013 and Arboit et al., 2016), Phetchabun area (zircon U–Pb ages of 249.2–245.9 Ma from Salam et al., 2014), Loei area (zircon U–Pb ages of 230 ± 4 Ma, from Khositanont et al., 2008), and volcanic rocks in Loei area [zircon U–Pb ages of 245.9–241 Ma from Kamvong et al. (2014)] along LFB (Figure 9).
Conclusion
Volcanic rocks and related dikes in the Wang Nam Khiao area, Nakhon Ratchasima, Northeast Thailand, provide informative evidences of ancient magmatism and geological process as concluded in the following:
1. Volcanic rocks are petrochemically classified as rhyolite, dacite, and andesite whereas their related dikes yield andesitic composition. Plagioclase, hornblende, and quartz appear to be the main compositions in all rock types, but their proportions are obviously different.
2. Mineral composition, mineral chemistry, and geochemistry indicate the hydrous calc-alkaline magma resulted from continental arc subduction.
3. LILE (e.g., Rb, Sr) enrichment and HFSE depletion (e.g., Nb, Ce, Ti) together with the slightly high LREE patterns indicate arc magmatism.
4. Al-in-hornblende geobarometer and hornblende thermometer indicate that the crystallization P–T conditions of the phenocrysts, which ascend with the magma that subsequently fed the volcanic rocks and the andesitic dikes, range between 4.5 and 5.5 kbar and 861–972°C, as well as 4.8–5.5 kbar and 873–890°C, respectively, reflecting the middle crust region.
5. Relationship of the dike cross-cutting into the previously dated Late Permian hornblende granite indicates that the volcanic rocks and dikes have taken place during/after Late Permian.
6. The results of this study well support the model of multiple arc magmatisms in LFB that resulted from the subduction of Palaeo-Tethys beneath Indochina Terrane.
Data Availability Statement
The raw data supporting the conclusions of this article will be made available by the authors, without undue reservation.
Author Contributions
VH contributed to data collection, discussion, comment, and manuscript revision. CS contributed to data collection, comment, and manuscript revision. AF contributed to field investigation, laboratory studies, data collection, discussion, manuscript preparation, and revision. All authors contributed to the article and approved the submitted version.
Funding
The first author was supported by the 90th Anniversary of Chulalongkorn University Fund (Ratchadaphiseksomphot Endowment Fund), Graduate School, Chulalongkorn University for her M.Sc. study.
Conflict of Interest
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
Acknowledgments
The authors would like to acknowledge the Department of Geology, Faculty of Science, Chulalongkorn University for laboratory study.
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Keywords: petrology, geochemistry, volcanic rock, Loei Fold Belt, Thailand
Citation: Hunyek V, Sutthirat C and Fanka A (2020) Magma Genesis and Arc Evolution at the Indochina Terrane Subduction: Petrological and Geochemical Constraints From the Volcanic Rocks in Wang Nam Khiao Area, Nakhon Ratchasima, Thailand. Front. Earth Sci. 8:271. doi: 10.3389/feart.2020.00271
Received: 20 April 2020; Accepted: 15 June 2020;
Published: 14 July 2020.
Edited by:
Basilios Tsikouras, Universiti Brunei Darussalam, BruneiReviewed by:
Toshiaki Tsunogae, University of Tsukuba, JapanGianluca Vignaroli, University of Bologna, Italy
Copyright © 2020 Hunyek, Sutthirat and Fanka. This is an open-access article distributed under the terms of the Creative Commons Attribution License (CC BY). The use, distribution or reproduction in other forums is permitted, provided the original author(s) and the copyright owner(s) are credited and that the original publication in this journal is cited, in accordance with accepted academic practice. No use, distribution or reproduction is permitted which does not comply with these terms.
*Correspondence: Alongkot Fanka, YWxvbmdrb3QuZkBjaHVsYS5hYy50aA==; YWxvbmdrb3RmQGdtYWlsLmNvbQ==