- Open Access
Hydrothermal system in the Tatun Volcano Group, northern Taiwan, inferred from crustal resistivity structure by audio-magnetotellurics
© Komori et al.; licensee Springer. 2014
- Received: 12 February 2014
- Accepted: 2 September 2014
- Published: 11 October 2014
The present study proposes an improved conceptual model for the hydrothermal system in the Tatun Volcano Group in northern Taiwan. In the study, audio-magnetotellurics (AMT) surveys were conducted to reveal the spatial distribution of resistivity, which is highly sensitive to fluids and hydrothermal alteration. By combining the obtained resistivity structure with other geophysical and geochemical evidence, the following hydrothermal system was inferred. Beneath Chishinshan, vapor-dominant hydrothermal fluids, supplied from a deeper part, are maintained in a low to relatively low resistivity region (5 to 20 Ω m) that is covered by a clay-rich cap, represented by an upper extremely low resistivity layer. Fluid ascent is suggested by a pressure source and clustered seismicity. Exsolved gases result in fumarolic areas, such as Siao-you-keng, while mixing of gases with shallow groundwater forms a shallow flow system of hydrothermal fluids in the Matsao area, represented by a region of less than 10 Ω m. The fumarole in the Da-you-keng area originates from vapor-dominant hydrothermal fluids that may be supplied from a deeper part beneath Cing-tian-gang, suggested by a pressure source and low to relatively low resistivity. Horizontally extended vapor-bearing regions also suggest the possibility of future phreatic eruptions. The proposed conceptual model may provide clues to detecting precursors of potential volcanic activity.
- Tatun Volcano Group
- Hydrothermal system
- Vapor-dominant region
- Pressure sources
- Gas and groundwater geochemistry
Electric resistivity is one useful physical parameter for exploring the nature of a hydrothermal system because of its great sensitivity to the existence of fluid and hydrothermal alteration. In general, bulk resistivity decreases with increases in pore water connectivity, saturation, salinity, temperature, and smectite content due to rock alteration (e.g., Revil et al. , ; Waxman and Smits ). Many studies to date have found resistivity anomalies corresponding to the paths and phase states of hydrothermal fluids, and to the fluid-bearing structure in volcanic and geothermal areas (e.g., Ogawa et al. ; Kanda et al. ; Aizawa et al. ; Komori et al. , [2013a]; Revil et al. ). Therefore, resistivity anomalies may provide critical constraints leading to better models of hydrothermal systems. The present study proposes an integrated hydrothermal model that combines newly revealed electric resistivity structures of the crust with geophysical and geochemical evidence. We discuss implications for potential future phreatic eruptions for the TVG.
2.1 AMT surveys
2.1.1 Electromagnetic studies at the TVG
The magnetotellurics (MT) principle (e.g., Cagniard ; Vozoff ; Simpson and Bahr ) is based on electromagnetic induction and has been widely used at hydrothermal and volcanic areas for estimating the crustal electric resistivity structures associated with their activity. MT was first used by Chen et al. () and Chen  in the TVG to provide preliminary 1-D and 2-D structures, respectively. In addition, Kagiyama et al. () conducted extensive and dense VLF-MT surveys to investigate resistivity features near the surface using a singular electromagnetic frequency of 22.1 kHz. They found low resistivity anomalies (less than 30 Ωm) corresponding to the fumarole and hot spring areas. Their NE-SW trending distributions suggested that the hydrothermal activity might be controlled by polarized permeable paths developed in response to the regional stress field (Chang et al. ; Shyu et al. ; Chen et al. ). Utsugi et al. () conducted dense audio magnetotellurics (AMT) surveys around Mt. Chishinshan to reveal a resistivity structure down to depths of 2-3 km using multiple frequencies of 1 Hz to 10 kHz. This study extended the AMT observation points to the Matsao and Da-you-keng areas to the north, where there are also active fumaroles and hot springs (Figure 1). The present study will show the shallow crustal resistivity structure associated with the intense hydrothermal activity in the TVG in northern Taiwan. Incorporating the data from Utsugi et al. (), we will propose an integrated model of detailed crustal resistivity structures, particularly beneath Mt. Chishinshan, and the Matsao hot spring and Da-you-keng fumarolic areas.
It is notable that in the late 1960s to early 1970s, the Mining Research and Service Organization (MRSO , , , ) conducted extensive electrical resistivity surveys (DC surveys) to obtain the spatial distribution of apparent resistivity in the TVG for the purpose of commercial use of its geothermal energy. Unfortunately, at that time, the detailed resistivity structure could not be revealed because of a lack of inversion techniques and insufficient sounding depths.
2.1.2 Data acquisition and processing
AMT surveys were conducted in October 2011 by Utsugi et al. (), and in December 2012 for the present study, using two Phoenix Geophysics MTU-5 systems. AMT pre-surveys began in 2010. There was no significant change in volcanic activity in the TVG during the time (e.g., Murase et al. ; Wen et al. ). Figure 1 shows the observation points. Those used in 2011 and 2012 were configured to intersect Mt. Chishinshan and the Matsao hot spring and Da-you-keng fumarolic areas. Four Pb- PbCl2 electrodes were used to measure two orthogonal components (N-S and E-W) of the electric field, and one additional electrode was used for grounding. Three orthogonal components (N-S, E-W, and vertical) of the magnetic field were measured using three induction coils. Each consisted of a coil of copper wire wound on a core with high magnetic permeability. At each observation point, continuous data acquisition was carried out for about 4 h. To remove contamination in the data due to local noise, we used Gamble et al.’s () remote reference processing method for mutual referencing within the survey area. Actually, there are noise sources like power lines and inhabited areas around the study area that seriously affected the data even after removing the noise as described above. For this study, we removed any data whose electric and magnetic fields had a coherence of less than 0.7 to maintain high quality.
Skew angle β is a proxy for three-dimensional (3-D) heterogeneity in the media structure, where larger β values mean stronger effects. The β value tends to gradually increase with decreasing frequencies. In particular, relatively larger average β values were estimated at observation points near Mt. Chishinshan. Uncertainties were less than 0.1° for 100 to 10,800 Hz and less than a few degrees for 1 to 100 Hz. The resulting values were a few degrees in the range of several hertz to several hundred hertz, suggesting a relatively minor 3-D effect. In addition, the average β at the same frequencies is as small as 0.5° to 2° at the observation points off Mt. Chishinshan, so it is reasonable to infer that 3-D heterogeneity has a minor effect on a regional scale. It is also notable that the average λ values calculated using the magnitudes of the principal axes of phase tensor ellipses, which are the proxy for the one-dimensional (1-D) structure (Bibby et al. ), were found to be as small as 0.2 to 0.3, suggesting a relatively simple structure beneath the observation sites.
2.1.4 Strike estimation
The direction of the main axes of the phase tensor ellipses reflect a two-dimensional (2-D) strike ([Caldwell et al. 2004]). In order to estimate the regional strike, we focused on the data at lower frequencies. The tensor ellipses at frequencies of 18.8 and 8.1 Hz, shown in Figure 2a, have the following features. Most have main axes trending NW-SE at observation points around Mt. Chishinshan (sites 001, 002, 004, 102, 007) and in the Matsao area (sites 111, 104, 105). Those in the Da-you-keng area (sites 108, 109, 110, 008), however, have main axes in the N-S direction. Thus, we defined three areas, referred to as the Chishinshan, Matsao, and Da-you-keng areas, to estimate the respective direction of the major axes. Note that point 102 was at the intersect and was used in both the Chishinshan and Matsao areas.
Figure 2b shows the rose diagrams of the main axes of the phase tensor ellipses for each area. Uncertainties were lower than a few degrees for 100 to 10,800 Hz, and up to 10° for 1 to 100 Hz. The rose diagrams are rendered in discrete frequencies; this is because there are insufficient data at 530 Hz to 3.6 kHz and 40 to 79 Hz (460 Hz to 3.6 kHz, 16.2 to 116 Hz, and 1 to 6.9 Hz for the Chishinshan area). According to Caldwell et al. (), the dominant direction of the main axes of the phase tensor ellipses reflects the direction of either a regional strike or a conductivity discontinuity. They note that the obtained direction has a 90° ambiguity. The dominant directions of the main axes were estimated primarily from their modes in each area. The rose diagrams at several to several hundred hertz show that there are two rough types of dominant directions: NW-SE (or NE-SW) in the Chishinshan area and N-S (or E-W) at the Da-you-keng area, with the Matsao area having an intermediate direction.
As described above, northern Taiwan has regional NE-SW trending faults (approximately N60° E). Correspondingly, a NE-SW volcanic trend has developed along the Chinshan fault (e.g., Belousov et al. ). The TVG also has an E-W volcanic trend from Mt. Huangzuei to Mt. Tatunshan (Belousov et al. ), suggesting a weak extra E-W trending structure. The structural features noted above are consistent with the dominant directions of the main axes of the phase tensor ellipses. The induction vectors also trend roughly NW-SE and N-S in the Mt. Chishinshan and Da-you-keng areas, respectively, which suggests that the regional strike is perpendicular to the induction vector in each area. Based on these factors, the regional strike was estimated using the dominant directions at low- to middle-frequency ranges (below several hundred Hz) as follows: N57° E for the Chishinshan area, N65° E for the Matsao area, and and N85° W for the Da-you-keng area. This means that the 2-D cross sections are along N33° W for the Chishinshan area (line A-A’ in Figure 1), N25° W for the Matsao Matsao area, and N5° E for the Da-you-keng area. The 2-D cross section of the Matsao area is close to that of the Da-you-keng area, so we combined the Matsao and Da-you-keng areas into one and assumed its 2-D cross section as N10° W (Line B-B’ in Figure 1).
Accordingly, we rotated the impedance tensors to correspond to 2-D strikes oriented to N57° E for the Chishinshan area and N80° E for the Matsao-Da-you-keng area. We then performed a distortion analysis following the method of Bibby et al. (). This procedure estimates a distortion tensor, produced by surface heterogeneity, considering the ellipticity of a phase tensor and β angle. The effect of the distortion was removed from the rotated impedance tensor by multiplying the inversion matrix of the distortion tensor with the impedance tensor.
Sounding observations at Chishinshan area, shown in Figure 3a, have the following features. Site 001 has phases less than 45° in high-frequency ranges, suggesting a high-resistivity region near the surface. At sites 001 and 002, the phase significantly decreases with decreasing frequency from a few tens of hertz to 1 Hz. On the other hand, the phase at site 004 gradually decreases compared to sites 001 and 002. This feature suggests a relatively high-resistivity body at a deeper part beneath sites 001 and 002. At site 005, the phases are greater than 60° through frequencies from 10 kHz to 10 Hz for both the TE and TM modes, and the apparent resistivities of both modes decrease to 1 to 2 Ω m at 10 Hz, a feature quite different from the other sites. This suggests that there is a significant change in the resistivity structure around site 005.
Figure 3b shows the same features for the Matsao-Da-you-keng area. At sites 111 and 105, the phase increases from 45° to 50° to 60° as frequency decreases from 10 kHz to 10 to 20 Hz for both the TE and TM modes, although their phase change patterns differ slightly. Site 108 also phase change pattern similar to sites 111 and 105. At these three sites, the phase significantly decreases to approcimately 30° as frequency decreases from 10 to 20 to 1 Hz. These features suggest a shallow conductive body and a resistive body deeper beneath the sites. At sites 109 and 110, the phase begins decreasing from a few hundred hertz, suggesting that the resistive body mentioned above could rise toward a shallower level beneath sites 109 and 110. At site 008, the phase stays higher than 60° through frequencies from 1 kHz to several hertz, suggesting a conductive body underneath.
2.1.6 2-D analysis
2-D resistivity structure analyses were performed using the inversion code developed by Ogawa and Uchida (). This code performs smoothness-constrained 2-D inversion based on the ABIC minimization method, where trade-off parameters between data misfit, model roughness, and static shift are estimated to minimize the misfit functional, assuming that static shifts follow Gaussian distributions. Error floors for apparent resistivity and phase were set to be 10% and 7% for the Chishinshan and Matsao-Da-you-keng areas, respectively. The resistivity structures were projected to lines A-A’ and B-B’ for the two areas, as shown in Figure 1. To represent the overall topographic change at each observation area, we defined the topography by averaging within 2 km of line A-A’ for the Chishinshan area and within 1.3 km of line B-B’ for the Matsao–Da-you-keng area. Note that the results thus obtained for the average topography do not differ much from those using the actual topography along A-A’ and B-B’.
2.1.7 Sensitivity tests
- (i)Linear sensitivity analyses based on the method of Schwalenberg et al. (). According to that study’s authors, model sensitivity can be described as:(1)
where S j is the sensitivity of grid element j of size Δ j , f i (m) is the forward solution of model m, m j is the resistivity change of grid element j, σ i is the standard deviation of the data, and N is the number of elements = number of observation sites × number of frequencies × data types. This equation states that model resolution is the sum of the gradient of the forward solution to the resistivity change of a given grid element, which we normalize with regard to the standard deviation of the data, weighted by the size of each grid element. There are four types of data and forward solutions, the apparent resistivities and phases of the TE and TM modes.
As shown in Figure 4, a low-resistivity, column-shaped body was found below a depth of 1 km at sites 102 and 005 in the Chishinshan area. This structural feature is represented by the low-frequency range soundings at sites 004, 102, and 005 (Figure 3). However, many data are missing because of their low quality, suggesting that such inverted deeper structures are not unique. It is also known that low-quality data or 2-D analysis of a 3-D situation may introduce inversion artifacts.
Examination of changes in the sounding curves by making distinctive changes in the model.
Case 1: region X1 to X4
Regions X1, X2, and X4 have high resistivities with values more than 100 Ωm. For these cases, changes in RMS misfits were examined by replacing the data for the regions with a conductive body. Region X3, which has low resistivities with values less than 10 Ωm, was replaced with a resistive body. Figure 5b shows the RMS misfits when a 10- Ωm body was substituted for X1, X2, and X4 and a 100- Ωm body was substituted for X3. The horizontal axis indicates the altitude of the uppermost part of the replacing body. The RMS misfits increase with the elevation of the substitute bodies, except in region X4 where there was no significant increase of the RMS misfit, suggesting that region X4 has little sensitivity. The change of TM phase at site 001 (Figure 5c) shows that the calculated sounding curve does not fit well within 3 to 7 Hz at an altitude of -0.54 km, as the RMS misfit is approximately 1.06. This is indicated by the dotted and dashed line in Figure 5b. Thus, RMS misfits greater than 1.06 indicate significant discrepancies from the best-fit model. We thus concluded that computational blocks with sensitivities of at least 10−4.5 can be supported by the observed data.
Region X3 has relatively high sensitivities at deeper depths compared to the other regions (Figure 5a). Its RMS misfit increased significantly when the block was replaced at the same altitude as the other cases (−0.27 km; Figure 5b). This occurred because of the unstable soundings at low frequencies at site 102. Figure 5d shows the change in the TM phase at site 102 that occurs when region X3 is replaced with a 100- Ωm body. Although the modified soundings show rough changes over the range of the uncertainty of the data for altitudes between −0.87 km and −0.57 km, they are still unstable. Taking into account the changes in RMS misfits, we consider the structure beneath the shallow conductive layer at sites 004, 102, and 005 to be valid for the computational block at altitudes from −0.27 to −0.57 km.
Case 2: region Y
Region Y’s resistivity is high, being more than 100 Ωm. Figures 5b and c show the changes in RMS misfit and the phase sensitivities of the phase when region Y is replaced with a 10 Ωm body. As the elevation of the replacing body increases, the RMS misfit increases significantly, and the fit of the calculated to observed soundings worsens at 1 to 3 Hz, as described in case 1. Given this information, we consider that computational blocks with sensitivities of at least 10−4.5 can be supported.
2.1.8 2-D resistivity structure
The northern half of line A-A’ has a resistive surface of several hundred to one thousand ohm meters with a thickness of one hundred to several hundreds of meters. The southern half has a surface with a resistivity of 10 to 30 Ωm, except at its southern end, where the resistivity is greater than 100 Ωm. These features are consistent with the results from previous electrical resistivity surveys (DC surveys) by the MRSO (, , , ) and VLF-MT surveys by Kagiyama et al. (). Two discrete conductive regions with resistivities less than 3 Ω m are present at depths of several hundred meters beneath Mt. Chishinshan (C1 in Figure 6). These were also suggested by the apparent resistivity distribution obtained from the MRSO DC surveys (, , , ).
Line B-B’, shown in Figure 6, has a surface with a resistivity of generally less than a few tens of ohm meters. In particular, the surface at site 110 has a resistivity of less than 3 Ωm, corresponding to the Da-you-keng fumarolic area. There are two conductive regions at depths of a few hundred meters to 1 km beneath the Matsao hot spring area (C3 in Figure 6) and Cing-tian-gang (C2). They are connected to the conductive surface around the Da-you-keng fumarolic area, overlying a resistive body of about a few hundred ohm meters. Two separate conductive regions are suggested by the distribution of apparent resistivity from the MRSO DC survey (, , , ). Thus, by comparing the inferred results with previous work, the resistivity structure obtained along line B-B’ is likewise believed to be reliable.
This section attempts to interpret the resistivity structures obtained in this study, based mainly on reports from geothermal drillings by the MRSO (, , , ) and evidence from geochemistry (Ohba et al. ; Ohsawa et al. ), seismology (Konstantinou et al. ), and leveling (Murase et al. ). For easy reference, we define the following ranges of resistivity: extremely low resistivity (less than 3 Ωm), low resistivity (3 to 10 Ωm), relatively low resistivity (10 to 30 Ωm), relatively high resistivity (30 to 100 Ωm), and high resistivity (greater than 100 Ωm).
3.1 Chishinshan area
3.1.1 Low-permeability cap inferred from extremely low resistivity upper layer
As described in the previous section, the foot of Mt. Chishinshan has an extremely low resistivity layer a few hundred meters thick near the surface, as shown by C1 in Figure 6. This layer corresponds roughly to a region with a temperature of 100°C to 200°C, as shown in Figure 7b, as obtained from temperature loggings (MRSO ). According to the drilling report, the 100°C to 200°C region is rich in smectite, but smectite is not present below depths corresponding to temperatures greater than 220°C (MRSO ). In general, smectite is stable at temperatures less than 180°C to 200°C (e.g., Pytte and Reynolds ; Anderson et al. ; Komori et al. [2013b]). This significantly decreases both the resistivity and permeability of rock matrices (e.g., Ogawa et al. ; Revil and Cathles ; Revil et al. ; Komori et al. [2013b]). Based on these earlier studies, layer C1 appears to be rich in smectite and could behave as a low-permeability cap to prevent hydrothermal fluids from easily discharging.
Layer C1 overlies the low to relatively low resistivity region R1. Beneath this region, there are ‘spasmodic bursts’ of clustered seismicity inferred by the seismological observations of Konstantinou et al. () and a pressure source inferred by Murase et al. ()’s precise leveling surveys, as shown in Figure 6. The authors consider the seismic activity and crustal deformation to be associated with the flow of hydrothermal fluids. Unfortunately, the present study could not reveal a corresponding resistivity structure with high precision. We can, at least, consider that upwelling hydrothermal fluids, supplied from a deeper part, are maintained in region R1, covered by the low-permeability cap C1. This is a typical interpretation of resistivity structures obtained for shallow hydrothermal systems (e.g., Ogawa et al. ; Nurhasan et al. ; Komori et al. [2013a]). In addition, the MRSO () performed well tests at borehole E202, which reaches to R1 as shown in Figure 6 and extracted hydrothermal fluids with a steam ratio greater than 80%. This suggests that region R1 is dominated by vapors. This structure is considered to extend from Mt. Chishinshan toward Leng-shuei-keng and Cing-tian-gang.
3.1.2 Hydrothermally inactive area in the northern half of the Chishinshan area
In contrast to the area beneath Mt. Chishinshan, the northern half of line A-A’ has no extremely low-resistivity layer like layer C1. This suggests that there is no structural feature that confines vapor-rich fluids as described previously. Actually, there are neither fumaroles nor temperature anomalies in this area. One borehole penetrated to a depth of 200 m (shown by rhombus ‘p’ in Figure 1). It has a bottom-hole temperature almost identical to the surface temperature (17°C: CGS ). Based on these factors, no hydrothermal activity appears to be developed in the northern half of the Chishinshan area.
This area does have two relatively high to high resistivity regions at the surface and at greater depths (R2). The high-resistivity surface corresponds to lava flows with little or no hydrothermal alteration (MRSO ; CGS ). MRSO () reported that tertiary sediments are exposed to the surface around Beitou and Liu-huang-ku, a few kilometers southwest of this area. MRSO’s comparison of the results of drilling and a DC survey in the above areas (MRSO ) indicates that weakly altered sediments correspond to an apparent resistivity of approximately 100 Ωm, while strongly altered sediments show resistivities less than 10 Ωm. This supports R2 as consisting of weakly altered tertiary sediments. Alternatively, R2 might be solidified igneous rocks, as suggested by the quite high resistivity of weakly altered lava observed at the surface. At a minimum, we can consider that resistive body R2 corresponds to weakly altered materials. There is also a possibility that region R2 might represent an extensive dry region, due to an absence of conductive fluids (e.g., Rinaldi et al. ), but this can be rejected based on the lack of a significant Bouguer anomaly, which is indicative of low-density material (Hsieh et al. personal communication).
3.2 Da-you-keng area
The Da-you-keng area has an intense fumarole with sulfur precipitation and hot spring water with a temperature of 100°C to 120°C (CGS ; Lee et al. , ). extremely low-resistivity region, shown as C2 in Figure 6, reaches approximately 1 km near the surface of this area, extending relatively deeper beneath Cing-tian-gang. At a depth of 500 m beneath Cing-tian-gang, corresponding to the uppermost part of region C2, a temperature of 100°C has been recorded by a thermal-monitoring well, shown by rhombus ‘q’ in Figure 1 (CGS ). Based on considerations described in the section on the Chishinshan area, region C2 may correspond to a low-permeability cap due to a large amount of smectite.
The underlying low to relatively low resistivity region R3 beneath Cing-tian-gang corresponds to a pressure source inferred by Murase et al. (). Based on the above previous studies, hydrothermal fluids are considered to be maintained in region R3, and these fluids could ascend toward Da-you-keng along paths controlled by the low-permeability cap. The ascent of fluids could induce the seismic burst events near the Da-you-ken-Cing-tian-gang area as shown in Figure 6 (Konstantinou et al. ). According to Ohba et al. (), fumarolic gases from Da-you-keng originate in as a mixture of magmatic vapors and meteoric vapors, which suggests that the hydrothermal reservoir maintains vapor-rich fluids. Therefore, we consider R3 to be dominated by vapors, like region R1 of the Chishinshan area.
This study also shows that the Da-you-keng fumarolic area has a relatively thin conductive surface, compared to the Chishinshan area. As mentioned previously, smectite composing the conductive layer is stable at temperatures of less than 180°C to 200°C. The lack of a thick conductive layer is considered to be due to a high-temperature gradient, suggesting the presence of high-temperature fluids in the shallow subsurface of the fumarolic area. This is consistent with the dominance of vapor-rich fluids suggested by Ohba et al. ().
3.3 Matsao area
In the Matsao area, hot spring water with a temperature of 30°C to 50°C discharges CGS ; Ohsawa et al. ), and there is no fumarolic area around the AMT observation points. According to sulfur isotope analysis of hot spring water from the TVG (Ohsawa et al. ), hot springs in the Matsao area are formed by mixing meteoric water with vapors separated from deep magmatic hydrothermal fluids, which then flow at shallow depths from Mt. Chishinshan along its topography. The Matsao area has an upper region with resistivities of less than 10 Ωm at depths of 0 to 1 km, shown in C3, and an underlying high-resistivity region R4. Based on Ohsawa et al. (), region C3 could correspond to the shallow flow system of the Matsao area’s hydrothermal fluid. Region R4 could correspond to less-altered materials, such as sediments or solidified igneous rocks, as described in the previous section. This is supported by the lack of a significant Bouguer anomaly around this area (Hsieh et al. personal communication).
3.4 Inferred hydrothermal system of the TVG and its implication for potential volcanic hazards
We estimate that an extensive vapor-bearing region could be situated beneath the foot of Mt. Chishinshan, Da-you-keng, and Cing-tian-gang, suggesting the potential for future phreatic explosions caused by a rapid increases in the internal fluid pressure due to intense injection of volcanic fluids (e.g., Voight and Elsworth ; Nakada et al. ). A phreatic eruption actually occurred as the latest activity at Mt. Chishinshan circa 6,000 years ago (Belousov et al. ). The data also suggest that the vapor may have been maintained for several thousand years. These factors point to the need for future work to detect signals related to phreatic explosions. Precursors might be detected by the following ongoing observations: temporal variations of chemical and isotopic composition ([Lee et al. 2008]), microgravity changes (Hwang et al. ), changes in precise leveling surveys (Murase et al. ), and temporal changes in tiltmeter readings (Lin, personal communication).
This study, however, did not reveal magmas suggested by a deeply distributed aseismic region as in Konstantinou et al. (), and their interrelation with the two pressure sources, due to a lack of data with low-frequency ranges. In the future, broadband MT surveys will reveal the deeper structural features to further elucidate the conditions from the viewpoint of hydrothermal fluid flow (i.e., Aizawa et al. ).
This study revealed the resistivity structure associated with hydrothermal activity in the Tatun Volcano Group using AMT surveys to investigate the present state of this system. The structure obtained here can be consistently explained by hot spring water and fumarolic gas formation processes as indicated by geochemical work. Its association with seismicity and pressure sources supports the presence of paths of hydrothermal fluid flow. This study also inferred the presence of an extensive vapor-bearing region covered by a low-permeability cap beneath Mt. Chishinshan and Da-you-keng-Cing-tian-gang. This suggests the possibility of future phreatic explosions around the area. The results indicate that an integrated conceptual model for the hydrothermal system at the TVG can provide reliable constraints for its potential volcanic hazards.
We would like to thank Yangmingshan National Park for arranging the surveys and M. Murase (Nihon University) for providing data about leveling surveys. We also thank Y.H. Lee, R. Sih, G.S.K. Ma, C.C. Lin, W. Minju (Academia Sinica), P. Pong (National Taiwan University), S. Yoshikawa, T. Asano, and N. Tokumoto (Kyoto Univ.) for supporting the observations. We thank the Central Geological Survey for providing data about the thermal monitoring project. We appreciate T. Lee, T. F. Yui, D. C. Lee, K. L. Wang, Y Iizuka, C. Y. Chen, C. H. Lin, X. E. Lei (Academia Sinica), C. Hwang (National Chiao Tung University), T. F. Yang, S.R. Song (National Taiwan University), K. Takemura, S. Ohsawa, and K. Matsuo (Kyoto University) for their valuable discussions. We also appreciate G. Zellmer (Massey University) for valuable comments and for improving the manuscript. The manuscript was critically reviewed by two anonymous reviewers. We appreciate H. Shimizu for the editorial support. Some figures were made using the GMT program (Wessel and Smith ).
- Aizawa K, Ogawa Y, Ishido T: Groundwater flow and hydrothermal systems within volcanic edifices: delineation by electric self-potential and magnetotellurics. J Geophys Res 2009,114(B1):B01208. doi:10.1029/2008JB005910 View ArticleGoogle Scholar
- Aizawa K, Koyama T, Hase H, Uyeshima M, Kanda W, Utsugi M, Yoshimura R, Yamaya Y, Hashimoto T, Yamazaki K, Komatsu S, Watanabe A, Miyakawa K, Ogawa Y: Three-dimensional resistivity structure and magma plumbing system of the Kirishima Volcanoes as inferred from broadband magnetotelluric data. J Geophys Res 2013, 119: 198–215. doi:10.1002/2013JB010682 View ArticleGoogle Scholar
- Anderson, E, Crosby D, Ussher G (2000) Bull’s-eye!-simple resistivity imaging to reliably locate the geothermal reservoir. In: Proceedings of the world geothermal congress 2000.. Beppu-Morioka.Google Scholar
- Belousov A, Belousova M, Chen C-H, Zellmer GF: Deposits, character and timing of recent eruptions and gravitational collapses in Tatun Volcanic Group, Northern Taiwan: Hazard-related issues. J Volcanol Geotherm Res 2010, 191: 205–221. doi:10.1016/j.jvolgeores.2010.02.001 View ArticleGoogle Scholar
- Bibby HM, Caldwell TG, Brown C: Determinable and non-determinable parameters of galvanic distortion in magnetotellurics. Geophys J Int 2005, 163: 915–930. doi:10.1111/j.1365–246X.2005.02779.x View ArticleGoogle Scholar
- Cagniard L: Basic theory of the magnetotelluric method of geophysical prospecting. Geophysics 1953, 18: 605–635. doi:10.1190/1.1437915 View ArticleGoogle Scholar
- Caldwell TG, Bibby HM, Brown C: The magnetotelluric phase tensor. Geophys J Int 2004, 158: 457–469. doi:10.1111/j.1365–246X.2004.02281.x View ArticleGoogle Scholar
- 2nd period of investigation and monitoring of particular geological hazard at Taipei district: investigation and monitoring of geological hazard and volcanic activity (2/4). Central Geological Survey, Taipei (in Chinese); 2009.Google Scholar
- Chang C-P, Chang T-Y, Angelier J, Kao H, Lee J-C, Yu S-B: Strain and stress field in Taiwan oblique convergent system: constraints from GPS observation and tectonic data. Earth Planet Sci Lett 2003, 214: 115–127. doi:10.1016/S0012–821X(03)00360–1 View ArticleGoogle Scholar
- Chen C-H: Geology and geothermal power potential of the Tatun volcanic region. Geothermics 1970, 2: 1134–1143. [http://dx.doi.org/10.1016/0375–6505(70)90425–6] http://dx.doi.org/10.1016/0375–6505(70)90425–6 http://dx.doi.org/10.1016/0375-6505(70)90425-6 10.1016/0375-6505(70)90425-6View ArticleGoogle Scholar
- Chen C-S: Investigation of potential magma chambers beneath the Tatun volcanic area: preliminary results of magnetotelluric survey. Journal of National Park 2009, 19: 1–10. (in Chinese with English abstract) (in Chinese with English abstract)Google Scholar
- Chen C-H, Lin S-B: Eruptions younger than 20 ka of the Tatun Volcano Group as viewed from the sediments of the Sungshan Formation in Taipei Basin. West Pac Earth Sci 2002, 2: 191–204.Google Scholar
- Chen C-H, Wu Y-J: Volcanic geology of the Tatun geothermal area, northern Taiwan. Proc Geological Soc China 1971, 14: 5–20.Google Scholar
- Chen C-S, Chen C-C, Chou K: Deep electrical structure of Taiwan as inferred from magnetotelluric observations. Terr Atmos Ocean Sci 1998, 9: 51–68.Google Scholar
- Chen C-T, Lee J-C, Chan Y-C, Lu C-Y: Growth normal faulting at the western edge of the metropolitan Taipei basin since the Last Glacial Maximum, northern Taiwan. Terr Atmos Ocean Sci 2010, 21: 409–428. doi:10.3319/TAO.2009.11.13.01(TH) View ArticleGoogle Scholar
- Gamble TD, Goubau WM, Clarke J: Magnetotellurics with a remote magnetic reference. Geophysics 1979, 44: 53–68. doi:10.1190/1.1440923 View ArticleGoogle Scholar
- Hwang C, Chao B, Chen C-C, Lee C-W, Hsieh W-C, Huang J-F, Kao R: Static and time-varying gravity observations at the Tatun Volcano Group in northern Taiwan. In Abstracts of AOGS-AGU (WPGM) joint assembly. Resorts world convention centre, Sentosa Island; 2012.Google Scholar
- Jiracek GR: Near-surface and topographic distortions in electromagnetic induction. Surv Geophys 1990, 11: 163–203. 10.1007/BF01901659View ArticleGoogle Scholar
- Juang W-S: Diversity and origin of quaternary basaltic magma series in northern Taiwan. Bull Natl Museum Nat Sci 1993, 4: 125–165.Google Scholar
- Kagiyama T, Utsugi M, Chen C-H, Miyabuchi Y: Conductivity distribution of the surface layer around Tatun Volcanic group, Taiwan. In Abstracts of Japan geoscience union meeting 2010,. Makuhari Messe international conference hall, Chiba; 2010.Google Scholar
- Kanda W, Tanaka Y, Utsugi M, Takakura S, Hashimoto T, Inoue H: A preparation zone for volcanic explosions beneath Naka-dake crater, Aso volcano, as inferred from magnetotelluric surveys. J Volcanol Geotherm Res 2008,178(1):32–45. doi:10.1016/j.jvolgeores.2008.01.022 View ArticleGoogle Scholar
- Komori S, Kagiyama T, Hoshizumi H, Takakura S, Mimura M: Vertical mapping of hydrothermal fluids and alteration from bulk conductivity: simple interpretation on the USDP-1 site, Unzen Volcano, SW Japan. J Volcanol Geotherm Res 2010, 198: 339–347. doi:10.1016/j.jvolgeores.2010.09.019 View ArticleGoogle Scholar
- Komori S, Kagiyama T, Utsugi M, Inoue H, Azuhata I: Two-dimensional resistivity structure of Unzen Volcano by AMT and MT surveys. Earth Planets Space 2013a, 65: 759–766. doi:10.5047/eps.2012.10.005 View ArticleGoogle Scholar
- Komori S, Kagiyama T, Takakura S, Ohsawa S, Mimura M, Mogi T: Effect of the hydrothermal alteration on the surface conductivity of rock matrix: comparative study between relatively-high and low temperature hydrothermal systems. J Volcanol Geotherm Res 2013b, 264: 164–171. doi:10.1016/j.jvolgeores.2013.08.009 View ArticleGoogle Scholar
- Konstantinou KI, Lin C-H, Liang W-T: Seismicity characteristics of a potentially active quaternary volcano: The Tatun Volcano Group, northern Taiwan. J Volcanol Geotherm Res 2007, 160: 300–318. doi:10.1016/j.jvolgeores.2006.09.009 View ArticleGoogle Scholar
- Konstantinou KI, Lin C-H, Liang W-T, Chan Y-C: Seismogenic stress field beneath the Tatun Volcano Group, northern Taiwan. J Volcanol Geotherm Res 2009, 187: 261–271. doi:10.1016/j.jvolgeores.2009.09.011 View ArticleGoogle Scholar
- Lee H-F, Yang TF, Lan T-F, Song S-R, Tsao S: Fumarolic gas composition of the Tatun Volcano Group, northern Taiwan. Terr Atmos Ocean Sci 2005, 16: 843–864.Google Scholar
- Lee H-F, Yang TF, Lan T-F, Chen C-H, Song S-R, Tsao S: Temporal variations of gas compositions of fumaroles in the Tatun Volcano Group, northern Taiwan. J Volcanol Geotherm Res 2008, 178: 624–635. doi:10.1016/j.jvolgeores.2008.06.005 View ArticleGoogle Scholar
- Lin C-H, Konstantinou KI, Liang W-T, Pu H-C, Lin Y-M, You S-H, Huang Y-P: Preliminary analysis of volcanoseismic signals recorded at the Tatun Volcano Group, northern Taiwan. Geophys Res Lett 2005, 32: L10313. doi:10.1029/2005GL022861 View ArticleGoogle Scholar
- Lin C-H, Yang TF, Leu P-L, Chang W-Y: Establishment of Taiwan Volcano Observatory at Tatun. In Abstracts of AOGS-AGU (WPGM) joint assembly. Resorts world convention centre, Sentosa Island; 2012.Google Scholar
- Liu C-M, Song S-R, Chen Y-L, Tsao S: Characteristics and origins of hot springs in the Tatun Volcano Group in northern Taiwan. Terr Atmos Ocean Sci 2011, 22: 475–489. doi:10.3319/TAO.2011.05.25.01(TT) View ArticleGoogle Scholar
- MRSO Report 90: the geothermal exploration of the, Tatun Volcano Group (I). Mining Research and Service Organization, Taipei (in Chinese); 1969.Google Scholar
- MRSO Report 102: the geothermal exploration of the Tatun Volcano Group (II). Mining Research and Service Organization, Taipei (in Chinese); 1970.Google Scholar
- MRSO Report 111: the geothermal exploration of the, Tatun Volcano Group (III). Mining Research and Service Organization, Taipei (in Chinese); 1971.Google Scholar
- MRSO Report 126: the geothermal exploration of the, Tatun Volcano Group (IV). Mining Research and Service Organization, Taipei (in Chinese); 1973.Google Scholar
- Murase, M, Lin C-H, Kimata F, Mori H, Suzuki A (2013) Estimated pressure source and vertical deformation in Tatun volcano group, Taiwan, detected by precise leveling during 2006–2013. In: Abstracts of IAVCEI 2013 scientific assembly, Kagoshima prefectural citizens exchange center & Kagoshima citizens social support plaza, Kagoshima.Google Scholar
- Nakada S, Shimizu H, Ohta K: Overview of the 1990–1995 eruption at Unzen volcano. J Volcanol Geotherm Res 1999, 89: 1–22. [http://dx.doi.org/10.1016/S0377–0273(98)00118–8] http://dx.doi.org/10.1016/S0377–0273(98)00118–8. http://dx.doi.org/10.1016/S0377-0273(98)00118-8. 10.1016/S0377-0273(98)00118-8View ArticleGoogle Scholar
- Ogawa Y, Ujihara N, Tank SB, Honkura Y, Onizawa S, Mori T, Makino M: Two electrical conductors beneath Kusatsu-Shirane volcano, Japan, imaged by audiomagnetotellurics, and their implications for the hydrothermal system. Earth Planets Space 2006, 58: 1053–1059. 10.1186/BF03352610View ArticleGoogle Scholar
- Ogawa Y, Uchida T: A two-dimensional magnetotelluric inversion assuming Gaussian static shift. Geophys J Int 1996, 126: 69–76. doi:10.1111/j.1365–246X.1996.tb05267.x View ArticleGoogle Scholar
- Ogawa Y, Matsushima N, Oshima H, Takakura S, Utsugi M, Hirano K, Igarashi M, Doi T: A resistivity cross-section of Usu volcano, Hokkaido, Japan, by audiomagnetotellurics soundings. Earth Planets Space 1998, 50: 339–346. 10.1186/BF03352120View ArticleGoogle Scholar
- Ohba T, Sawa T, Taira N, Yang TF, Lee H-F, Lan T-F, Ohwada M, Morikawa N, Kazahaya K: Magmatic fluids of Tatun volcanic group, Taiwan. Appl Geochem 2010, 25: 513–523. [http://dx.doi.org/10.1016/j.apgeochem.2010.01.009] http://dx.doi.org/10.1016/j.apgeochem.2010.01.009. http://dx.doi.org/10.1016/j.apgeochem.2010.01.009. 10.1016/j.apgeochem.2010.01.009View ArticleGoogle Scholar
- Ohsawa S, Lee H-F, Liang B, Komori S, Chen C-H, Kagiyama T: Geochemical characteristics and origins of acid hot spring waters in Tatun Volcanic Group, Taiwan. J Hot Spring Sci 2013, 62: 282–293. (in Japanese with English abstract) (in Japanese with English abstract)Google Scholar
- Pytte AM, Reynolds RC: The thermal transformation of smectite to illite. In Thermal history of Sedimentary Basins: Methods and Case Histories. Edited by: Naeser ND, McCulloh TH. Springer-Verlag, New York; 1989:133–140. 10.1007/978-1-4612-3492-0_8View ArticleGoogle Scholar
- Revil A, Cathles III LM: Permeability of shaly sands. Water Resour Res 1999,35(3):651–662. doi:10.1029/98WR02700 View ArticleGoogle Scholar
- Revil A, Cathles III LM, Losh S: Electrical conductivity in shaly sands with geophysical applications. J Geophys Res 1998,103(B10):23925–23936. doi:10.1029/98JB02125 View ArticleGoogle Scholar
- Revil A, Hermitte D, Spangenberg E, Cochemé JJ: Electrical properties of zeolitized volcaniclastic materials. J Geophys Res 2002,107(B8):2168. doi:10.1029/2001JB000599 View ArticleGoogle Scholar
- Revil A, Finizola A, Ricci T, Delcher E, Peltier A, Barde-Cabusson S, Avard G, Bailly T, Bennati L, Byrdina S, Colonge J, Di Gangi F, Douillet G, Lupi M, Letort J, Tsang Hin Sun E: Hydrogeology of Stromboli volcano, Aeolian Islands (Italy) from the interpretation of resistivity tomograms, self-potential, soil temperature and soil CO 2 concentration measurements. Geophys J Int 2011, 186: 1078–1094. doi:10.1111/j.1365–246X.2011.05112.x doi:10.1111/j.1365-246X.2011.05112.x 10.1111/j.1365-246X.2011.05112.xView ArticleGoogle Scholar
- Rinaldi AP, Todesco M, Vandemeulebrouck J, Revil A, Bonafede M: Electrical conductivity, ground displacement, gravity changes, and gas flow at Solfatara crater (Campi Flegrei caldera, Italy): results from numerical modeling. J Volcanol Geotherm Res 2011, 207: 93–105. doi:10.1016/j.jvolgeores.2011.07.008 View ArticleGoogle Scholar
- Rontogianni S, Konstantinou KI, Lin C-H: Multi-parametric investigation of the volcano-hydrothermal system at Tatun Volcano Group, Northern Taiwan. Nat Hazards Earth Syst Sci 2012, 12: 2259–2270. doi:10.5194/nhess-12–2259–2012 View ArticleGoogle Scholar
- Schwalenberg K, Rath V, Haak V: Sensitivity studies applied to a two-dimensional resistivity model from the Central Andes. Geophys J Int 2002, 150: 673–686. doi:10.1046/j.1365–246X.2002.01734.x View ArticleGoogle Scholar
- Shyu JBH, Sieh K, Chen Y-G, Liu C-S: Neotectonic architecture of Taiwan and its implications for future large earthquakes. J Geophys Res 2005, 110: B08402. doi:10.1029/2004JB003251 View ArticleGoogle Scholar
- Simpson F, Bahr K: Practical magnetotellurics. Cambridge University Press, Cambridge; 2005.View ArticleGoogle Scholar
- Tsai Y-W, Song S-R, Chen H-F, Li S-F, Lo C-H, Lo W, Tsao S: Volcanic stratigraphy and potential hazards of the Chihsingshan volcano subgroup in the Tatun Volcano Group, northern Taiwan. Terr Atmos Ocean Sci 2010, 21: 587–598. doi:10.3319/TAO.2010.02.22.03(TH) View ArticleGoogle Scholar
- Tsao S: K-Ar age determination of volcanic rocks from the Tatun Volcano Group. Bull Central Geological Surv 1994, 9: 137–154. (in Chinese) (in Chinese)Google Scholar
- Utsugi, M, Kagiyama T, Chen C-H, Kanda W, Yoshimura R, Asano T, Tokumoto N, Inoue H, Yoshikawa S (2012) Audio frequency magneto-telluric survey on Tatun Volcanic Group, Taiwan In: Abstracts of Japan geoscience union meeting 2012, Makuhari Messe international conference hall, Chiba.Google Scholar
- Voight B, Elsworth D: Failure of volcano slopes. Géotechnique 1997, 47: 1–31. 10.1680/geot.19126.96.36.199View ArticleGoogle Scholar
- Vozoff, K (1991) The magnetotelluric method. In: Nabighian MN (ed)Electromagnetic Methods in Applied Geophysics, Society of Exploration Geophysicists, 641–711, Oklahoma. Vozoff, K (1991) The magnetotelluric method. In: Nabighian MN (ed)Electromagnetic Methods in Applied Geophysics, Society of Exploration Geophysicists, 641–711, Oklahoma.Google Scholar
- Waxman MH, Smits LJM: Electrical conductivities in oil-bearing shaly sands. Soc Pet Eng J 1968, 8: 107–122. 10.2118/1863-AView ArticleGoogle Scholar
- Wang W-H, Chen C-H: The volcanology and fission track age dating of pyroclastic deposits in Tatun Volcano Group, northern Taiwan. Acta Geological Taiwan 1990, 28: 1–30.Google Scholar
- Wang K-L, Chung S-L, Chen C-H, Shinjo R, Yang TF, Chen C-H: Post-collisional magmatism around northern Taiwan and its relation with opening of the Okinawa Trough. Tectonophysics 1999, 308: 363–376. 10.1016/S0040-1951(99)00111-0View ArticleGoogle Scholar
- Wen, H-Y, Yang TF, Lan T-F, Lee H-F, Lin C-H (2013) Spatial and temporal variations of soil CO2 flux in geothermal areas of the Tatun Volcano Group, Northern Taiwan. In: Abstracts of IAVCEI 2013 scientific assembly, Kagoshima prefectural citizens exchange center & Kagoshima citizens social support plaza, Kagoshima.Google Scholar
- Wessel P, Smith WHF: New, improved version of generic mapping tools released. Eos Trans AGU 1998,79(47):579. 10.1029/98EO00426View ArticleGoogle Scholar
- Wu C-C, Cheng C-S, Lee M-Y, Hong C-H: Numerical simulation of volcanic ash dispersal and fallout from Datun volcano and Kuei-shan-tao by using PUFF model. Meteorol Bull 2009, 48: 83–99. (in Chinese with English abstract) (in Chinese with English abstract)Google Scholar
- Yang TF, Sano Y, Song S-R: 3 He/ 4 He ratios of fumaroles and bubbling gases of hot springs in Tatun Volcano Group, North Taiwan. Il Nuovo Cimento C 1999, 22: 281–286.Google Scholar
- Yang TF, Chen C-H, Tien R-L, Song S-R, Liu T-K: Remnant magmatic activity in the Coastal Range of East Taiwan after arc-continent collision: fission-track data and 3 He/ 4 He ratio evidence. Radiation Measurements 2003, 36: 343–349. 10.1016/S1350-4487(03)00149-5View ArticleGoogle Scholar
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