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.
Keywords
Tatun Volcano GroupHydrothermal systemResistivityVapor-dominant regionPressure sourcesGas and groundwater geochemistry
1
Background
The Tatun Volcano Group (TVG) covers an area of approximately 300 km 2 on the northern tip of the island of Taiwan, only about 10 km north of the capital city of Taipei. The group is composed of over 20 andesitic volcanic composites, cones, and domes (Chen and Wu [1971]; Wang and Chen [1990]), enclosed by NE-SW trending faults such as the Chinshan and Kanchiao faults, as shown in Figure 1. The magmatism of the TVG is considered to have taken place in an extensional stress field, which was associated with postcollisional processes between the Philippine Sea Plate and East Asian continent, and with the opening of the southwestern end of the Okinawa Trough (Wang et al. [1999]; Chang et al. [2003]; Shyu et al. [2005]; Chen et al. [2010]). A look at historical volcanic eruptions has suggested that volcanism has been extinct since the last major activity that occurred from 0.8 to 0.2 Ma BP (e.g., Juang [1993]; Tsao [1994]). However, recent studies offer suggestions that the potential for volcanic activity exists in the area: extensive hydrothermal activity is discharging a large amount of heat (e.g., Chen [1970]); there are strongly acidic hot springs (pH approximately 1 to 3) (e.g., Liu et al. [2011]; Ohsawa et al. [2013]); magmatic contributions are found in fumarolic gases (e.g., Yang et al. [1999], [2003]; Lee et al. [2005]; Ohba et al. [2010]); relatively young ejecta can be observed (<< 20 ka, Chen and Lin [2002]; 6 ka, Belousov et al. [2010]), and the presence of clustered seismicity and shallow pressure sources suggest fluid flows (Lin et al. [2005]; Konstantinou et al. [2007], [2009]; Murase et al. [2013]). Based on the above studies, hazard assessments and monitoring projects are being conducted (e.g., Lee et al. [2008]; Wu et al. [2009]; Tsai et al. [2010]; Lin et al. [2012]; Rontogianni et al. [2012]).
Figure 1
Location of the Tatun Volcano Group, northern Taiwan. Open circles represent the AMT observation points. Sites 001, 002, 004, 005, 006, and 007 were observed in 2011 by Utsugi et al. ([2012]), while sites 008, 104, 105, 108, 109, 110, and 111 were observed in 2012 for this study. Double circles represent the locations of pressure sources obtained from precise leveling surveys by Murase et al. ([2013]). Squares and diamonds represent the wells drilled by MRSO ([1969], [1970], [1971], [1973]), and CGS ([2009]), respectively.
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. [1998], [2002]; Waxman and Smits [1968]). 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. [1998]; Kanda et al. [2008]; Aizawa et al. [2009]; Komori et al. [2010], [2013a]; Revil et al. [2011]). 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
Methods and Results
2.1 AMT surveys
2.1.1 Electromagnetic studies at the TVG
The magnetotellurics (MT) principle (e.g., Cagniard [1953]; Vozoff [1991]; Simpson and Bahr [2005]) 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. ([1998]) and Chen [2009] in the TVG to provide preliminary 1-D and 2-D structures, respectively. In addition, Kagiyama et al. ([2010]) 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. [2003]; Shyu et al. [2005]; Chen et al. [2010]). Utsugi et al. ([2012]) 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. ([2012]), 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 [1969], [1970], [1971], [1973]) 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. ([2012]), 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. [2013]; Wen et al. [2013]). 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 ([1979]) 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.
2.1.3 Dimensionality
To examine the regional dimensionality of this study area, impedance phase tensors and skew angles (β) were calculated using the method of Caldwell et al. ([2004]); this method has the merit of removing distortions from original impedances due to near-surface heterogeneities. Figure 2a shows the impedance phase tensors, skew angles, and induction arrows for representative frequencies.
Figure 2
Data for dimensionality and strike estimation.(a) Impedance phase tensors, skew angles β, and induction arrows for representative frequencies. Note that some data are missing due to their low quality. Also note that the larger induction vectors observed at sites 007, 105, and 108 are considered to be due to noise, as these sites are located near electrical cables and roadways. (b) Rose diagrams of tensor axes.
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. [2005]), 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. ([2004]), 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. [2010]). The TVG also has an E-W volcanic trend from Mt. Huangzuei to Mt. Tatunshan (Belousov et al. [2010]), 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. ([2005]). 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.
2.1.5 Soundings
Figure 3 shows the sounding curves of the apparent resistivity and phase, with open circles representing the TE mode and open rhombi for the TM mode, calculated from the impedance tensors as described above. The apparent resistivity and phase of the TM mode were calculated using electric fields perpendicular to the strike and magnetic fields parallel to the strike and the opposite for the TE-mode. For both modes, apparent resistivities have high values at high frequencies throughout and decrease with decreasing frequencies. In general, the apparent resistivity decreases with decreasing frequency for both modes.
Figure 3
Sounding curves of apparent resistivity and phase for both the TM and TE modes.(a) Chishinshan area. (b) MatsaoŰDa-you-keng area. Circles and diamonds represent the data for the TE mode and TM mode respectively, obtained from observations. Red and Blue lines represent the data for the TE mode and TM mode respectively, calculated using the best-fit model.
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 ([1996]). 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’.
Figure 4 shows the best-fit models obtained after 42 iterations for the Chishinshan area and 31 for the Matsao-Da-you-keng area, starting from an initial model with a uniform resistivity of 100 Ωm, with both RMS misfits of 1.02. Figure 3 shows the calculated soundings for the TE mode (red line) and TM mode (blue line). The inferred models reproduce most of the apparent resistivity and phase distributions. In the Chishinshan area, there seems to be no relation between the amount of static shift and the topographic change. The TE mode at site 004 has a relatively large static shift. Fumarolic activities do sporadically occur around site 004 in the area called Siao-you-keng. This is characterized by a surface resistivity less than 30 Ωm from the VLF-MT survey (Kagiyama et al. [2010]). This suggests that site 004 could have relatively strong 3-D heterogeneity near the surface, leading to the relatively large static shift. The Matsao-Da-you-keng area has a larger static shift than the Chishinshan area, presumably because most of its sites are situated amid sharp cliffs, resulting in a static shift due to the local topography (e.g., Jiracek [1990]).
Figure 4
Best-fit models obtained from 2-D analysis. Solid inverted triangles represent observation points. Site numbers are indicated above black triangles. X1 to X4 and Y represent regions used for the sensitivity tests.
2.1.7 Sensitivity tests
Before making any interpretations on the basis of our analyses, we performed the following series of sensitivity tests:
(i)
Linear sensitivity analyses based on the method of Schwalenberg et al. ([2002]). According to that study’s authors, model sensitivity can be described as:
(1)
where Sj is the sensitivity of grid element j of size Δj, fi(m) is the forward solution of model m, mj is the resistivity change of grid element j, σi 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.
Figure 5a shows the resultant model sensitivity, which decreases with depth, corresponding to the limit of the sounding frequency. The high-resistivity body situated below 1 to 1.5 km beneath sites 001 and 002 in the Chishinshan area has a variety of sensitivities ranging from 10−3 to 10−6, as do the resistive bodies situated below 1 km beneath sites 111, 105, 108, and 109 in the Matsao–Da-you-keng area. The MT method is generally less sensitive to resistive bodies because of the properties of electromagnetic waves, which can be easily absorbed by a conductor (e.g., Cagniard [1953]; Vozoff [1991]; Simpson and Bahr [2005]). For this reason, evaluating the reliability of the resistive body was necessary.
Figure 5
Sensitivity tests.(a) Results of linear sensitivity analysis. Site numbers are indicated above black triangles. (b) Variation in RMS misfits by further sensitivity analyses for each case. (c) Sensitivities of the TM phase at sites 001 and 111 by further sensitivity analysis for the cases where blocks X1 and Y are replaced. (d) Sensitivities of the TM phase at site 102 by further sensitivity analysis for the case where block X2 is replaced.
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.
In order to confirm these regions with reliable sensitivity, the deeper resistive or conductive bodies shown by regions X1 to X4 and Y in Figures 4 and 5a were submitted to the following further sensitivity analysis.
(ii)
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
Figure 6 shows the resistivity structures of the Chishinshan area (line A-A’) and the Matsao–Da-you-keng area (line B-B’) after removing the low-sensitivity regions defined in the previous section.
Figure 6
Resistivity structures along lines A-A’ and B-B’, after removal of the low-sensitivity part. Site numbers are indicated above black triangles. Locations of pressure sources (Murase et al. [2013]) and spasmodic bursts (Konstantinou et al. [2007]) are shown respectively as stars and ellipses in the structure along lines A-A’ and B-B’. The solid lines represent the trajectories of boreholes E202 and E203 drilled by MRSO ([1970]).
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 ([1969], [1970], [1971], [1973]) and VLF-MT surveys by Kagiyama et al. ([2010]). 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 ([1969], [1970], [1971], [1973]).
Figure 7a shows the resistivities along borehole E203, shown in Figure 6, one of the MRSO drilling sites ([1970]). Red lines represent the resistivities obtained in the present study, while black represent those from well logging (MRSO [1970]). The latter shows resistivities of a few Ωm at depths from 200 to 670 m with some fluctuations, increasing to several tens of ohm meters at depths of 670 to 1,000 m. The inferred resistivities around the borehole can reproduce the low resistivities from well logging quite well, although the inferred values for the resistive section of 670 to 1,000 m in depth are slightly lower than those from well logging. From these results, we determined that our method produces a reliable resistivity structure for the Chishinshan area from the surface to a depth of approximately 1 km.
Figure 7
Comparison between inverted results and in-situ measurement.(a) Resistivities along borehole E203, shown in Figure 6. Red and black lines represent the resistivities obtained by this study and by well logging (MRSO [1970]), respectively. (b) Geologic section along sites 102, 005, 006, and 007 at the foot of Mt. Chishinshan (MRSO [1973]). Red lines represent the isotherm obtained from temperature logging of the boreholes (MRSO [1973]). The locations of the boreholes are shown by the squares in Figure 1.
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 ([1969], [1970], [1971], [1973]). Thus, by comparing the inferred results with previous work, the resistivity structure obtained along line B-B’ is likewise believed to be reliable.
3
Discussion
This section attempts to interpret the resistivity structures obtained in this study, based mainly on reports from geothermal drillings by the MRSO ([1969], [1970], [1971], [1973]) and evidence from geochemistry (Ohba et al. [2010]; Ohsawa et al. [2013]), seismology (Konstantinou et al. [2007]), and leveling (Murase et al. [2013]). 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 [1973]). 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 [1973]). In general, smectite is stable at temperatures less than 180°C to 200°C (e.g., Pytte and Reynolds [1989]; Anderson et al. [2000]; Komori et al. [2013b]). This significantly decreases both the resistivity and permeability of rock matrices (e.g., Ogawa et al. [1998]; Revil and Cathles [1999]; Revil et al. [2002]; 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. ([2007]) and a pressure source inferred by Murase et al. ([2013])’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. [1998]; Nurhasan et al. [2006]; Komori et al. [2013a]). In addition, the MRSO ([1973]) 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 [2009]). 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 [1970]; CGS [2009]). MRSO ([1970]) 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 [1969]) 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. [2011]), 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 [2009]; Lee et al. [2005], [2008]). 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 [2009]). 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. ([2013]). 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. [2007]). According to Ohba et al. ([2010]), 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. ([2010]).
3.3 Matsao area
In the Matsao area, hot spring water with a temperature of 30°C to 50°C discharges CGS [2009]; Ohsawa et al. [2013]), 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. [2013]), 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. ([2013]), 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 discussed the relation between the resistivity structure and other geophysical and geochemical data above. On basis of the insights thus obtained, in this section, we propose a better description of the hydrothermal system of the TVG, as shown in Figure 8. Beneath Mt. Chishinshan, vapor-rich hydrothermal fluids are supplied from the deeper part. The fluids are maintained below the clay-rich, low-permeability cap, extending horizontally beneath the foot of Mt. Chishinshan. Some vapors are discharged through breaks or along the end of the clay-rich layer, developing fumarolic areas like Siao-you-keng. Further on, the vapor mixes with groundwater at the shallow subsurface, forming so-called ‘steam-heated thermal waters’, which develop the shallow flow system of hydrothermal fluids in the Matsao area. The fumaroles at Da-you-keng area, on the other hand, may be supplied from the deeper part beneath Cing-tian-gang and vapor-rich fluids maintained in the region, covered by a clay-rich cap.
Figure 8
Conceptual model of the hydrothermal system of the Tatun Volcano Group. As inferred by interpretation of the resistivity structure and other geochemical and geophysical evidence.
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 [1997]; Nakada et al. [1999]). A phreatic eruption actually occurred as the latest activity at Mt. Chishinshan circa 6,000 years ago (Belousov et al. [2010]). 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. [2012]), changes in precise leveling surveys (Murase et al. [2013]), 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. ([2007]), 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. [2013]).
4
Conclusions
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.
Declarations
Acknowledgments
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 [1998]).
Authors’ Affiliations
(1)
Institute of Earth Sciences, Academia Sinica
(2)
Aso Volcanological Laboratory, Kyoto University
(3)
Institute of Oceanography, National Taiwan University
(4)
Research Center for Earthquake Prediction, Disaster Prevention Research Institute, Kyoto University
(5)
Volcanic Fluid Research Center, Tokyo Institute of Technology
(6)
Geological Survey of Japan (GSJ), AIST
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