Re-evaluation of the activity of the Thoen Fault in the Lampang Basin, northern Thailand, based on geomorphology and geochronology
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2011
Received: 7 September 2010
Accepted: 1 June 2011
Published: 26 January 2012
We applied remote sensing techniques and geomorphic index analysis to a study of the NE-SW-striking Thoen Fault, Lampang Basin, northern Thailand. Morphotectonic landforms, formed by normal faulting in the basin, include fault scarps, triangular facets, wine-glass canyons, and a linear mountain front. Along the Thoen Fault, the stream length gradient index records steeper slopes near the mountain front; the index values are possibly related to a normal fault system. Moreover, we obtained low values of the ratio of the valley floor width to valley height (0.44–2.75), and of mountain-front sinuosity (1.11–1.82) along various segments of the fault. These geomorphic indices suggest tectonic activity involving dip-slip displacement on faults. Although the geomorphology and geomorphic indices in the study area indicate active normal faulting, sedimentary units exposed in a trench at Ban Don Fai show no evidence of recent fault movement. In Ban Don Fai trench No. 2, accelerator mass spectrometry radiocarbon (AMS) ages and optically stimulated luminescence (OSL) ages indicate that deposition of the lowest exposed sedimentary unit occurred between 960 and 910 years ago. Therefore, the most recent movement upon the Ban Don Fai segment of the Thoen Fault occurred more than 960 years ago.
Thailand is located to the east of the Andaman-Sumatra earthquake belt, and no large earthquake (i.e., magnitude ≥6 on the Richter scale) has recently occurred in this region. Thus, Thailand has not been considered a seismically active country. However, historical earthquakes in Thailand have been reported by Nutalaya et al. (1985), based on historical texts, annals, stone inscriptions, and astrological documents in the Thai language. These earthquakes are likely to have originated on the active faults of Myanmar and southern China (Fenton et al., 2003). Although a few moderate earthquakes (i.e., magnitude 3–6 on the Richter scale) have recently been recorded in Thailand, seismicity in Thailand is generally considered to be low, and there is no clear association of seismicity with mapped faults (Bott et al., 1997; Fenton et al., 2003). In addition, geological and geomorphological investigations reveal that Quaternary faults in northern Thailand are characterized by long recurrence intervals of thousands to tens of thousands of years (Bott et al., 1997; Kosuwan et al., 1999; Fenton et al., 2003).
In this paper, we document movements along the Thoen Fault (Fig. 1(B)). We used remote sensing techniques and aerial photographs to identify and analyze the characteristic morphotectonic landforms that result from fault movements along the southeastern margin of the Lampang Basin. Based on this analysis, we identified a suitable site for trenching, and compiled the trench-log stratigraphy at this site. Quaternary dating methods, including optically stimulated luminescence (OSL) and accelerator mass spectrometry (AMS) radiocarbon dating, were used to determine the ages of sedimentary layers in the trench. The Thoen Fault can be divided into six segments based on fault geometry: the Ban Don Fai, Ban Mai, Ban Mae Ip, Mae Than, Sop Prap, and Doi Ton Ngun segments (Fig. 1(B)). Some of these segments were examined as part of a paleoearthquake study; however, paleoearthquake data are insufficient in terms of determining the timing of the most recent event. Trenching studies across the fault segments are necessary to reconstruct the history of displacement. Normal faulting along the Ban Don Fai segment has produced distinct morphotectonic landforms that represent the most important data in terms of site selection for a paleoearthquake study. Thus, our study focuses on the Ban Don Fai segment (segment 1 in Fig. 1(B)).
2. Tectonic Setting
In the Indochina region, since the late Paleogene, the collision of the Indian and Eurasian plates has resulted in predominantly strike-slip faults that strike NW-SE and NE-SW, and dip-slip faults that strike N-S (Tapponnier et al., 1986; Peltzer and Tapponnier, 1988). Important and well-known fault zones in this region include the Red River Fault Zone in Vietnam (Tapponnier et al., 1986; Morley, 2007), the Sagaing Fault Zone in Myanmar (Tapponnier et al., 1986; Morley, 2007), and the Mae Ping and Three Pagoda fault zones in western Thailand (Morley, 2002; Fenton et al., 2003). During the late Eocene, collision of the Indian and Eurasian plates resulted in left-lateral displacements along the NW-SE striking Red River, Mae Ping, and Three Pagoda faults (Lacassin et al., 1997), but most recently these faults have been characterized by right-lateral displacements (Lacassin et al., 1997; Morley, 2002; Fenton et al., 2003). The left-lateral displacement along the Red River Fault amounted to hundreds of kilometers in the Eocene–Oligocene, related to extension within the South China Sea (Morley, 2002). The clockwise rotation of SE Asia coincided with a reversal in the sense of fault movement along the Mae Ping and Three Pagoda faults in the early Miocene, when these faults changed from left-lateral to right-lateral NW-SE-striking faults. At the same time, the Red River Fault continued as a left-lateral strike-slip fault (Huchon et al., 1994; Lacassin et al., 1997). By the middle Miocene, all of the NW-SE-striking strike-slip faults in the Indochina region (Red River, Mae Ping, and Three Pagoda faults) had become right-lateral strike-slip faults (Longley, 1997). The main strike-slip faults (Red River, Mae Ping, and Three Pagoda faults) together form a transtensional regime that is related to the opening of Cenozoic basins in SE Asia (Ducrocq et al., 1992).
Thailand lies mainly in a zone of strike-slip deformation, between the Red River Fault Zone to the east and the compressive Sagaing Fault Zone to the west (Morley, 2007). Cenozoic basins in northern Thailand are mainly N-S-trending graben and half-graben with sediments ranging in thickness from 1,000 to 3,000 m (Polachan et al., 1991). These Cenozoic basins are governed by N-S extensional faults which are inferred to be causally related to right-lateral slip movements on the NW-SE-striking faults, and left-lateral slip on the NE-SW-striking faults (Polachan et al., 1991; Pakcham, 1993). The geometries of the Cenozoic basins and the locations of faults may possibly be controlled by pre-existing fabrics in the basement rocks (O’Leary and Hill, 1989; Morley, 2007). A combination of both dip-slip and left-lateral strike-slip movement (i.e., oblique sinistral extension) is recognized as being required to explain the evolution of these basins (Morley et al., 2001, 2004, 2007; Morley, 2002, 2007).
3. Active Faults in Thailand
Paleoearthquake studies aim to determine the occurrence of past earthquakes on active faults. An active fault can be defined as one that has moved at least once during the period that includes the late Pleistocene and extends through to the present day (Geological Survey of Japan, 1983). Moreover, an active fault may generate another earthquake in the near future.
Based on seismological and geological evidence, Nutalaya et al. (1985) were the first to introduce the concept of seismic source zones in Thailand and neighboring countries. Hinthong (1995, 1997) conducted a project titled “Study of Active Faults in Thailand”, and used geological, historical, and seismological data to identify 23 active or suspected active faults in Thailand (Fig. 1(A)). Siribhakdi (1986) studied seismogenic regimes in Thailand, and reported on the earthquakes that had occurred in Thailand throughout the past 1,500 years. Many of these earthquakes were closely related to the Three Pagoda Fault (number 13 in Fig. 1(A)), the Si Sawat Fault (12 in Fig. 1(A)), the Mae Ping Fault (Moei Fault of Hinthong (1995); 11 in Fig. 1(A)), and the Mae Hong Son Fault (Mae Sariang Fault of Hinthong (1995); 3 in Fig. 1(A)). Thiramongkol (1986) provided evidence of Holocene movement on the Bang Pa Kong Fault along the eastern margin of the lower central plain of Thailand (number 23 in Fig. 1(A)). Charusiri et al. (1996) applied several remote sensing techniques to a study of earthquakes in Thailand and neighboring countries. A seismotectonic (or seismic source) map was compiled by Charusiri et al. (1996). Rhodes et al. (2004) studied the kinematics of the Mae Kuang Fault in northeastern Chiang Mai, northern Thailand, and identified offset contacts and slickenlines on the surface of the fault, indicating a left-lateral slip of 3.5 km and a dip-slip of 600 m. The authors suggested that the fault was initiated between 20 and 5 Ma, simultaneous with a reversal in the movement direction on the Mae Ping and Red River faults, and that it terminates at the northeastern margin of the Chiang Mai Basin. The Mae Kuang Fault does not extend to the western side of the Chiang Mai Basin because it is truncated by the right-lateral Mae Tha Fault.
The Thoen Fault in the Cenozoic Lampang Basin strikes NE-SW, and has been regarded as an active fault (Hinthong, 1995, 1997; Fenton et al., 1997, 2003). Based on morphotectonic landforms and geochronological data, the Department of Mineral Resources in Thailand (DMR, 2006) also classified the Thoen Fault as active. Quartz-rich samples from fault-related colluviums, and charcoal samples, provide displacement ages of 4,000, 3,000, and 2,000 years BP using thermoluminescence (TL) dating and the 14C method, respectively (DMR, 2006). Moreover, from 1990 to the present day, more than two dozen earthquakes with magnitudes of Mb 3.0–5.0 have been detected near this fault. Danphaiboonphon (2005) studied the characteristics of the Thoen Fault, using remote sensing, petrographic analysis, and geophysical investigation, and suggested that it is an oblique strike-slip fault. Several lines of evidence, using geomorphology and stratigraphy, indicate that the Thoen Fault was an extensional structure during the Holocene (Fenton et al., 1997, 2003), and that the displacements are mainly normal dip-slip and subordinate left-lateral slip. The slip rate of the fault is about 0.6 mm/yr (Fenton et al., 2003). Pailoplee et al. (2009) excavated two trenches on the Ban Mai (number 2 in Fig. 1(B)) and Doi Ton Ngun (6 in Fig. 1(B)) segments of the Thoen Fault in the Lampang Basin. Based on trench-log interpretations, the Ban Mai segment records a single main paleoearthquake, at 3,800 years ago; the slip rate is approximately 0.06 mm/yr. The Doi Ton Ngun segment records evidence for two paleoearthquake events at 3,500 and 1,800 years ago; the average slip rate since the last fault movement is 0.18 mm/yr, and the recurrence interval for earthquakes is 1,700 years. Based on the current study of seismicity (i.e., the b value of the Gutenberg-Richter (G-R) relationship, where a low value indicates high earthquake activity) upon the Thoen Fault (Lampang Basin) and upon the Phrae Fault (Phrae Basin), the b value for the Thoen Fault is lower than that for the Phrae Fault (Pailoplee et al., 2009). Pailoplee et al. (2009) also suggested that the Thoen Fault in the Lampang Basin is capable of generating more earthquake activity than the Phrae Fault.
4. Interpretation of Remote Sensing Data
The Thoen Fault is well defined, visible as a sharp lineament on aerial photographs and satellite images (Fig. 4). Detailed interpretations of aerial photographs reveal fault scarps at Ban Mai, Ban Don Fai, and Ban Samai Nuea ((A) and (C) in Fig. 4), and reveal the following six geometrical fault segments along the southeastern margin of the Lampang Basin: Ban Don Fai, Ban Mai, Ban Mae Ip, Doi Ton Ngun, Mae Than, and Sop Prap (Fig. 1(B)).
5. Analyses Based on Geomorphic Indices
Geomorphic indices are useful for the level of tectonic activity, and zones of active tectonism (Keller and Pinter, 1996; Bull, 2008). Geomorphic indices represent preliminary tools for identifying areas that are experiencing rapid tectonic deformation (Keller and Pinter, 1996; Bull, 2008).
Geomorphic indices, including the streamlength gradient index (SL), the ratio of valley floor width to valley height (Vf), and mountain-front sinuosity (Smf), were used in the present study to identify tectonic activity within the Lampang Basin. All the parameters for the geomorphic index analysis are taken from the Mae Tha (map sheet 4945 III) and Sop Prap (map sheet 4844 I) 1:50,000 topographic maps.
5.1 Stream length gradient index (SL)
5.2 Ratio of valley floor width to valley height (Vf)
Bull and McFadden (1977) showed that Vf values in the active tectonic zones of arid areas are characterized by Vf values from 0.05 to 0.9, whereas Vf values in less active and inactive tectonic areas tend to fall in the ranges 0.5–3.6 and 2–47, respectively. The Vf index has seldom been applied to active tectonic areas in the tropics. A Vf analysis along the Lo River Fault in northern Vietnam produced low values (0.06 to0.61), indicating recent uplift upon the fault (Cuong and Zuchiewicz, 2001).
Parameters for calculating the ratio of Valley floor width to Valley height (Vf) in the southeastern Lampang Basin.
Sop prap area/Stream name and location (No.)
Huai Mae So (1)
Huai Samai (2)
Huai Som (3)
Huai Pa Phai (4)
Huai Mae Wa (5)
Huai Kom Ko (6)
Huai Mae Thok Noi (7)
Ban Mai Area/Stream name and location (No.)
Huai Sam Kha1 (8)
Huai Sam Kha2 (9)
Huai Mae Sapao (10)
Huai Mae Iak (11)
Huai Mae Mai (12)
Huai Mae Tap (13)
5.3 Mountain-front sinuosity (Smf)
Parameters for calculating values of mountain-front sinuosity (Smf) in the southeastern Lampang Basin.
5.4 Summary of analyses based on geomorphic indices
SL indices for the Thoen Fault, along the southeastern margin of the Lampang Basin, indicate a steeper slope near the mountain front, possibly the result of normal faulting. Moreover, most of the Vf and Smf values obtained for the Ban Mai, Ban Don Fai, and Sop Prap segments are low (0.44–2.75 for Vf and 1.11–1.82 for Smf; Tables 1 and 2), which may indicate an area of weakly active tectonism characterized by normal dip-slip fault movement.
6. Trench Investigations
Top soil: reddish-brown clayey sand. This is a soil used for agriculture, and organic matter is commonly found. The unit is approximately 30 cm thick.
Unit A: sand and gravel. The gravels consist mainly of sub-angular to angular clasts of sandstone and shale, and clast size varies from pebble to cobble. The thickness of this unit ranges from 10 cm to 1 m.
Unit B: brown clayey sand with gravel. Most of the clasts in the gravel are subangular and consist of sandstone, shale, and quartz. The unit is exposed on the southeastern side of the trench, but was not found on the northwestern side. The thickness of the unit ranges from 10 cm to 50 cm.
Unit C: brown sandy clay, with a little gravel. Most of the gravel clasts are sandstone. The unit is exposed only on the southeastern side of the trench, where its thickness ranges from 10 to 50 cm.
Unit D: sand with gravel. Most of the gravel clasts (of pebble size) are of sandstone and shale. The unit is exposed on the southeastern side of the trench, but it is absent at the point marked ‘x’ in Fig. 13. The thickness of the unit ranges from 10 to 30 cm.
Unit E: reddish-brown clayey sand, with sparsely distributed pebbles. This unit is limited to the southeastern part of the trench, where it is approximately 30 cm thick.
Unit F: gravel, sand, and silt with carbonaceous clay. The gravel clasts are mainly subangular to rounded, and most consist of quartz, sandstone, and shale. The unit contains graded beds of 10–50 cm in thickness. A lenticular layer of sand (20 cm thick) occurs between layers of gravel. The total thickness of this unit exceeds 1.5 m.
The grain size of sediment in this trench ranges from clay to coarse gravel. The stratigraphic relationships between unit F and overlying units indicate that the top of unit F is an erosional surface (Fig. 13). The sediments in unit F are poorly sorted. Clasts in gravel layers are subangular to rounded, and the unit contains a lenticular layer of sand and graded beds. The clasts are randomly oriented, with some elongate gravel clasts oriented with their long axes at a high angle to bedding. The sedimentary structures indicate that unit F was deposited by a gravity flow (e.g., Steel and Gloppen, 1980). The sediments of units A–E are poorly sorted, and the mixed sand, silt, and gravel of these units was possibly deposited from a sandy gravity flow. The sediments in this trench are laterally continuous, and no faults are observed.
7. Geochronological Investigations
The trench-log stratigraphy in Ban Don Fai trench No. 2 shows no evidence for recent fault movement, but to put this finding in context it is necessary to determine the age of the sediments exposed in the trench. Having established the stratigraphy of the Ban Don Fai trench No. 2, we then proceeded to collect samples for OSL and AMS radiocarbon dating.
7.1 AMS radiocarbon dating
Result of AMS radiocarbon dating (C-14) of carbonaceous sediments from Ban Don Fai trench No. 2.
14C measured radiocarbon age (yr BP)
13C/12C (per mil)
14 C conventional radiocarbon age (yr BP)
940 ± 40
940 ± 40
940 ± 40
960 ± 40
910 ± 40
920 ± 40
7.2 Optically Stimulated Luminescence (OSL)
OSL dating is based on detecting the amount of luminescence and the radiation rate (per year) for the radioactive isotope (Vafiadou et al., 2007). The method is widely used in dating geological sediments such as aeolian quartz-rich sediments, marine sands, and colluvial materials (Murray and Olley, 2002). Six samples from units C, E, and F in Ban Don Fai trench No. 2 were prepared for OSL dating (Fig. 13). Samples were dried, and the water content analyzed. Each sample was sieved using a 0.84 mm mesh filter for annual dose analysis (300 g). Grains between 0.25 and 0.075 mm in size were extracted by re-sieving the remaining sample. Thereafter, these samples were treated with 35% hydrochloric acid (HCl) for at least 30 minutes to remove carbonates and organic material. Ferromagnetic fragments in the samples were separated from quartz using an isodynamic magnetic separator. Feldspar was removed by treatment with 24% hydrofluoric acid (HF). X-ray diffraction analysis (XRD) was used to ensure no feldspar remained in the samples; if feldspar was detected, we treated the samples again with hydrofluoric acid until all feldspar had been removed.
OSL dating results for quartz concentrates from sediment samples collected in the Lampang Basin, northern Thailand.
For the annual dose, the concentrations of U, Th, and K were analyzed using gamma spectrometry at Chulalongkorn University. The annual dose was computed using the concentration of K, U, and Th in the standard table described by Bell (1979). The results of annual doses and OSL dating are summarized in Table 4.
Figure 13 shows the stratigraphic units, and the measured OSL and AMS radiocarbon dates for sediments from Ban Don Fai trench No. 2. The OSL ages indicate that the sediments were deposited during the past 910 years. Three AMS radiocarbon dates indicate that the sediments in the lowest unit were deposited from about 960 to 920 years BP, and these dates are consistent with the OSL ages for sediments in unit F. Thus, the OSL method is useful for estimating the age of deposition of the quartz-rich sample. This result is encouraging in terms of the future use of OSL dating.
8.1 Sense of fault movement
The Thoen Fault, along the southeastern margin of the Lampang Basin, has been regarded as an active fault (Fenton et al., 1997, 2003; DMR, 2006). Morley et al. (2007) and Fenton et al. (2003) suggested that the fault is characterized mainly by normal dip-slip and subordinate left-lateral slip.
Measurements of geomorphic indices (SL, Vf, and Smf indices) in the Lampang Basin are consistent with dip-slip movement on the Thoen Fault. The SL indices from the southeastern margin of the basin indicate steeper slopes near the mountain front, and most of the Vf and Smf values from the Ban Mai, Ban Don Fai, and Sop Prap segments are quite low (0.44–2.75 for Vf and 1.11–1.82 for Smf). The geomorphic characteristics of the Thoen Fault are similar to those of the Lo River Fault in northern Vietnam, where values of Vf (0.06–0.61) and Smf (1.04–1.16) are low because of recent tectonic uplift (Cuong and Zuchiewicz, 2001).
The Thoen Fault is well defined by geomorphology, and is evident as sharp lineaments on aerial photographs and satellite images (Fig. 4), associated with morphotectonic landforms such as fault scarps, triangular facets, wine-glass canyons, and a linear mountain front. Detailed interpretations of aerial photographs clearly reveal fault scarps at Ban Mai, Ban Don Fai, and Ban Samai Nuea ((A) and (C) in Fig. 4). A series of triangular facets on the NW-facing escarpment (Fig. 5) might represent stage VIII of Hamblin’s model (Fig. 6). A series of streams crossing the Ban Don Fai, Sop Prap, and Ban Mai segments of the fault pass through wine-glass canyons (Fig. 7) and V-shaped valleys, suggesting multiple episodes of tectonic uplift.
A sequence of alluvial gravels and lacustrine clays is cut by a NE-SW-striking normal fault along Highway 11 (from Lampang to Phrae) at 28 km from Lampang. This offset is exposed on the western side of the main escarpment along the Ban Mai segment. The total vertical displacement is 1.3–1.6 m (Charusiri et al., 1997; Fenton et al., 2003). The timing of the faulting is interpreted to be Late Quaternary (Fenton et al., 2003). The relationship between this fault and the Thoen Fault remains unknown, although its location and orientation suggest that it is a synthetic fault (i.e., it has the same dip and sense of movement as the main fault) (Fenton et al., 2003).
8.2 Age of fault movement
Geomorphological features and geomorphic indices in the study area indicate active normal faulting. However, the sediments in the trench at Ban Don Fai show no clear-cut evidence of recent fault movement. At Ban Don Fai trench No. 2, AMS radiocarbon and OSL dates show that the sediments of the lowest unit (Unit F in Fig. 13) were deposited between 960 and 910 years ago. The lack of evidence in the trench for recent fault movement indicates that the fault is located below the depth of the trench; i.e., the most recent movement upon the fault pre-dates the deposition of the oldest sediments in the trench. In the case that the trench did not intercept the fault trace, the most recent movement on the fault may be younger than the oldest sediments in the trench; however, the location of the trench was decided based on a careful analysis of aerial photographs, and based on the distribution of morphotectonic landforms observed in the field. Thus, it is possible that the most recent movement on the Ban Don Fai fault segment occurred more than 960 years ago. Based on TL dating of sediments at trench sites (Pailoplee et al., 2009), the most recent movement on the Ban Mai segment of the fault took place about 3,800 years ago (2 in Fig. 12), while the last movement on the Doi Ton Ngun segment was about 1,800 years ago. However, the TL method of dating involves uncertainties. The apparent TL ages calculated for fluvial sediments are often 3–8 times higher than TL or AMS radiocarbon dates for adjacent buried soils (McCalpin et al., 1994). Fluvial sediments are usually deposited episodically by water flowing in the river channel. They probably receive limited exposure to light, and as a consequence, they are likely to retain a large inherited TL signal (McCalpin et al., 1994). Alluvial sediments are rapidly deposited by gravity flows, which may also result in a large inherited TL signal. Thus, TL dates for fluvial and alluvial sediments may systematically result in overestimating the ages of deposition (Forman, 1989; McCalpin et al., 1994). For this reason, the TL dating method is unsuitable for determining the deposition ages of fluvial and alluvial sediments in the Lampang Basin.
The Thoen Fault in the Lampang Basin, northern Thailand, strikes NE-SW. Morphotectonic landforms caused by normal faulting in the Lampang Basin are well represented by fault scarps, triangular facets, wine-glass canyons, and linear mountain fronts. On the other hand, morphotectonic landforms that would indicate strike-slip faulting are not found.
Along the fault at the southeastern margin of the Lampang Basin, the stream length gradient index (SL index), as measured near the mountain front, records steeper slopes which possibly relate to normal faulting. Moreover, along the Ban Mai, Ban Don Fai, and Sop Prap segments of the fault, the ratio of valley floor width to valley height (Vf)is generally low (0.44–2.75), as are values of mountain-front sinuosity (Smf) (1.11–1.82). Low Vf values reflect deep V-shaped valleys, and low Smf values are associated with active tectonic zones. Together, these geomorphic indices suggest an area of weakly active tectonism characterized by dip-slip normal fault movement.
Although the geomorphological features and geomorphic indices in the study area are consistent with active normal faulting, the sediments exposed in the trench at Ban Don Fai provide no clear-cut evidence of recent fault movement. In Ban Don Fai trench No. 2, AMS radiocarbon and OSL dating indicate that the sediments of the lowest exposed unit were deposited between 960 and 910 years ago. Accordingly, we conclude that the most recent fault movement along the Ban Don Fai segment of the Thoen Fault occurred more than 960 years ago.
We would like to thank the Royal Thai Government for supporting this research; the Active fault and Earthquake Research Center, AIST, Japan, for assistance in funding the AMS radiocarbon dating; and the Department of Geology, Chulalongkorn University, Thailand, for help in providing the OSL equipment. We thank the Environmental Geology Division, DMR, for providing all facilities during the fieldwork in Lampang province. Dr. Akira Takada, editor, Dr. Brady Rhodes, and anonymous reviewers are thanked for a thorough review that greatly improved the manuscript. We extend special thanks to Dr. Santi Pailoplee for his advice on OSL dating; Mr. Suwith Kosuwan, Mr. Preecha Saithong, and Ms. Wunnaporn Punyawai for their help during fieldwork and managing the collection of samples; Mr. Surasak Bunlue for his discussion; and Dr. Yu Horiuchi for proofreading parts of the manuscript.
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