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- Open Access
Ground motions around a semi-circular valley partially filled with an inclined alluvial layer under SH-polarized excitation
- Kao-Hao Chang^{1}Email author,
- Deng-How Tsaur^{2} and
- Jeen-Hwa Wang^{1}
https://doi.org/10.1186/1880-5981-66-53
© Chang et al.; licensee Springer. 2014
- Received: 4 September 2013
- Accepted: 7 March 2014
- Published: 12 June 2014
Abstract
A simplified mathematical model, composed of a semi-circular valley partially filled with an inclined alluvial layer under plane SH-wave incidence, is presented. To evaluate the site response theoretically, a rigorous series solution is derived via the region-matching technique. For angular wavefunctions constrained by an inclined free surface, the original form of Graf's addition formula is recast to arbitrarily shift the local coordinate system. The valley geometry, filling material, angle of incidence, and wave frequency are taken as significant parameters in exploring the site effect on ground motions. Also included are the frequency- and time-domain computations. Two canonical cases, the semi-circular vacant canyon and the fully filled semi-circular alluvial valley, with exact analytical solutions, and the partly horizontally filled case previously studied, are taken to be particular cases of the proposed general model. Steady-state results show that the peak amplitudes of motion may increase at low frequencies when the filling layer inclines to the illuminated region. At low-grazing incidence, the phenomenon of wave focusing becomes evident on the shadow side of the filling layer. Transient-state simulations elucidate how a sequence of surface waves travel on the topmost alluvium along opposite directions and interfere with multiple reflected waves within the filling layer.
Keywords
- Ground motions
- Scattering
- SH waves
- Partially filled valley
Background
From numerous simulations of destructive earthquakes, the seismological community has become increasingly aware of the significance of site response to seismic waves (e.g., Boore2004). It is generally accepted that valleys (or basins) with alluvial sediments (e.g., gravel, pebbles, clays, and volcanic ashes) can amplify and prolong ground motions dramatically (e.g., Koketsu and Kikuchi2000; Huang et al.2005,2007,2009). Near-surface geological and geometrical conditions at a specific site could be partly responsible for a strong modification of ground shaking on a regional scale (e.g., Ewald et al.2006). Unfortunately, many metropolitan (or industrial) areas are concentrated over such unfavorable sites (e.g., the Cascadia region of northwestern USA) so that they are much more prone to catastrophic seismic consequences such as loss of life, injury, economic damage, and environmental impact. Recent striking events are the 1999 M_{w} 7.6 Chelungpu, Taiwan earthquake (Wang2008), the 2010 M_{w} 8.8 Maule, Chile earthquake (Boroschek et al.2012), and the 2011 M_{w} 9.0 Tohoku, Japan earthquake (Ghofrani et al.2013). Consequently, we have learned that knowledge of valley- and basin-related site effects not only improves the prediction of ground motions but also contributes to feasible seismic hazard assessments for seismically active areas (e.g., Frischknecht et al.2005; Wang2006).
Since the early 1970s, a number of canonical models have been constructed to approximate the cross-sectional profiles of natural sediment-filled valleys. Among these idealized simplified models, the most popularly adopted ones are those of the fully filled type, especially those in trapezoid shapes (e.g., Bard and Bouchon1980; Kawase and Aki1989; Takenaka et al.1996; Makra et al.2005; Kham et al.2006; Gelagoti et al.2010). Various numerical approximation methods were devised to evaluate the dynamic site response (e.g., Aki and Larner1970; Boore et al.1971; Dravinski et al.1991; Clements and Larsson1994; Fu and Bouchon2004; Dravinski2007; Ávila-Carrera and Sánchez-Sesma2013). Nowadays, tremendous progress in parallel processing and faster processors has boosted the growth of mesh discretization techniques. For a large-scale domain with actual subsurface velocity structures, several sophisticated numerical schemes are, no doubt, the most powerful tools to carry out the ground-motion modelling pertinent to specific earthquakes and event scenarios. Representatives of modern schemes are the finite-difference, finite-element, spectral-element, and boundary-element methods (e.g., Komatitsch and Vilotte1998; Bielak et al.2005; Ma et al.2007; Moczo et al.2007; Lee et al.2009; Kristek et al.2010; Pelties et al.2010; Delépine and Semblat2012; Virieux et al.2012; Kham et al.2013). Although these effective approaches are flexible, the reliability and accuracy of the numerical results from these codes have to be strictly verified via the existing benchmark solutions.
In contrast to the fully filled alluvial valleys, the partially filled valleys seem to be of little interest. However, such types of valleys are common geological/geomorphological features. Examples are the Chusal valley in the Garm region of the former USSR (see Figure five in Tucker and King1984), the Nera River valley in the Perugia region of Italy (see Figure three in Lenti et al.2009), and the Aterno River valley in the Abruzzo region of central Italy (see Figure nine in De Luca et al.2005). Furthermore, the top surfaces of alluvial deposits are sometimes mildly inclined (see Figure two in Bordoni et al.2011). These cross-sectional geometries capture the authors' attention and thereby motivate this study.
In a paper by Tsaur and Chang (2008a), the partially filled semi-circular alluvial valley served as a simplified model for the exploration of site response and wave-scattering effects. Subsequently, the conceptual model was extended by Tsaur and Hsu (2013) to study alluvial valleys with semi-elliptic cross sections. Thus, this article continues along this path, looking closely at the spatial and temporal fluctuations in ground motions near a semi-circular valley partially filled with an inclined alluvial layer. To the authors' knowledge, relevant topics in the literature are very rare to date, especially those approaching the subject from a theoretical perspective. On the other hand, the present model with an inclined filling layer can degenerate into the simpler model with a horizontal filling layer. However, the latter is infeasible for the former. For these reasons, the model proposed herein is important per se. Recently, Wang (2010) treated an analogous problem on the basis of Tsaur and Chang (2008a). However, Wang (2010) only dealt with the steady states limited to a fairly narrow band of low frequencies.
For the problem under consideration, the method of solution hinges on the application of the region-matching technique (RMT), which is an effective way of overcoming the intrinsic difficulty in exploiting the method of separation of variables. From a mathematical point of view, such a promising technique is beneficial in pursuing theoretical solutions to problems involving geometric cross sections incompletely coinciding with any one of the separable coordinate systems (e.g., Tsaur and Chang2008b,2009; Chang2009; Tsaur et al.2010; Tsaur2011; Chang et al.2013). In this study, a rigorous series solution is derived via the RMT for the plane SH-wave incidence. Suitable wavefunctions are utilized to characterize the antiplane displacements both inside and outside the valley. The enforcement of matching conditions on the soil-bedrock interface leads to the determination of unknown expansion coefficients. A parametric analysis with systematic variations in the associated parameters (angle of incidence, wave frequency, valley geometry, and filling material) is carried out to assess the influence of these parameters on the peak amplitudes of motions.
In order to shift the coordinate origins of scalar cylindrical wavefunctions, the use of Graf's addition formula (e.g., Watson1966) is helpful to solve the multiple-scattering problems in several branches of wave physics such as elastic, electromagnetic, sound, and water waves (e.g., Varadan et al.1978; Bostock and Kennett1992; Martin2006). When the angular components of the wavefunctions are not expected to meet any constraints, Graf's addition formula can be utilized straightforwardly. For full-plane problems in the context of elastodynamics, this addition formula is usually applied in a half truncated form if the expressions with sine/cosine functions are preferred over those with exponential functions (e.g., Equations 33 to 36 in Avilés and Sánchez‒Sesma1983). For half-plane cavity/inclusion problems, this formula is commonly combined with the method of images (e.g., Smerzini et al.2009; Tsaur and Chang2012). When the angular wavefunctions are constrained by the zero-stress condition on a horizontal free surface, the original form of Graf's addition formula should be appropriately rewritten for specific arrangements of coordinate systems (e.g., Equations 15 and 16 in Tsaur and Chang2008a). Herein, for angular wavefunctions constrained by an inclined free surface, a novel form of Graf's addition formula is derived. Such a recast version is devoted to ‘arbitrary’ offsets so that it is more general than those given in the literature for offsets along the vertical direction (e.g., Tsaur and Chang2008a; Chang2009).
The main simplifications in the adopted model lie in the two-dimensional geometric profile, excitation source, and physical properties of the media. For the valley partially filled with inclined strata, these idealizations are perhaps the most significant ones in proposing a simple model. This indeed allows theoretical manipulation to yield the displacement/stress fields throughout the entire domain. So far, the element-based methods have been well established and developed with plenty of in-house/commercial codes. However, these methods cannot bypass the need for frequency-dependent discretizations. When the wavelength of the incident wave is smaller than the characteristic length scale of the region of interest, a rapidly growing number of degrees of freedom are indispensable to maintain accuracy. In standard discretized algorithms, adaptive mesh refinement and multi-grid preconditioning operations may have to be incorporated to capture the phenomena of interest while keeping the cost of a simulation tractable on the current hardware. Nevertheless, above a certain threshold frequency, the size of the discretized model may be too large (or impractical) so that the associated computational cost may become prohibitive. For the high-frequency case, the use of traditional domain/boundary discretization schemes may generate oscillatory solutions (see Engquist et al.2009). By contrast, the semi-analytical nature of the present series solution makes the high-frequency computation very easy and efficient. With increasing frequency, only one simple manipulation is needed in the present series-based code, namely, raising the number of wavefunction expansions. The key reason for this is that by making good use of the RMT, well-defined expressions can be obtained for the wavefield components. The field solution of each individual subregion is well behaved because the governing equation and all the boundary conditions (except for those at the soil-bedrock interface and circular-arc free surface) are fulfilled innately.
The RMT proposed herein can be conveniently applied to deal with more SH-wave problems involving other types of partially filled models consisting purely of circular-arc lines or those made up of both curves and straight lines. As to P- and SV-wave incidence, the RMT may be applicable if the explicit expressions of wavefunctions in specific coordinate systems are available. However, such wavefunctions in the open region have to inherently satisfy the zero-stress condition on the horizontal ground surface, while those in the enclosed region have to intrinsically fulfill the traction-free condition at the surface of the alluvium. This is a fundamental requirement for extension of the applicability of the RMT to in-plane wave propagation.
The model profile assumed in this paper might be the most obvious one in a first investigation for an inclined alluvial layer partially filling the valley. Because our interest focuses on the site-amplification effect, the potential applications of the current model may cover a wide range of geophysical, environmental, and engineering disciplines. It is known that during strong ground motions, site amplification is one of the root causes responsible for the instability of steep rocky slopes, the loss of cohesion, the imbalance of stress-strength state, the reduction of frictional resistance of the substrate, and the mobilization of superficial loose materials (e.g., Keefer et al.2006; Chigira et al.2010; Hovius and Meunier2012). Thus, the current analysis lays a solid foundation for related studies. Typical examples are those concerning the earthquake-induced slope failures, landslides, and debris flows. However, their dynamic processes involve a succession of granular materials, ranging in size from silts and clays to gravel, pebbles, and even boulders. Opportunities for these situations may be provided by using the individual-based approaches such as the off-lattice method, the discrete (or distinct) element method, the material point method, and the particle method (see Jing and Stephansson2007; Andersen and Andersen2010; Marketos and O’Sullivan2013; Takekawa et al.2013).
Methods
Theoretical formulations
Derivation for the general case
where ∇^{2} is the 2-D Laplacian and k_{ j } = ω/c_{ j } is the shear wavenumber. Throughout this work, the time-harmonic factor exp (iωt) is assumed and suppressed.
where ε_{ n } is the Neumann factor (equal to 1 if n = 0 and 2 if n ≥ 1) and J_{ n }( ⋅ ) denotes the n th order Bessel function of the first kind. Note that Equation 6 inherently satisfies the traction-free condition on the horizontal ground surface (Equation 2).
in which the primes stand for differentiation with respect to the arguments of the corresponding functions.
in which the complex expansion coefficients A_{ n } and B_{ n } are unknown.
where the complex expansion coefficients C_{ n } will be determined.
where the functions${F}_{m,n}^{C}$ and${F}_{m,n}^{S}$ are given in Appendix 1 (see Equations 39 and 40). Note that Equation 15 in Tsaur and Chang (2008a) is just the special case of Equation 14. Because the coordinate-transformation formula adopted herein is more compact than that in Wang (2010), the following solution enables a more effective computational performance, notably for high frequencies.
and detailed expressions are given in Appendix 1 (see Equations 39 to 43).
where the pertinent functions used are shown in Appendix 2 for conciseness (see Equations 44 to 47).
After truncating the infinite series in Equations 25 and 26 properly, the expansion coefficients C_{ n } can be evaluated by standard matrix techniques. For numerical computations, it is necessary to truncate the infinite summation to a finite number of terms. Summation indices n and weighting indices q in Equations 25 and 26 are truncated after 2N - 1 and N - 1 terms, respectively. Therefore, Equations 25 and 26 constitute a system of 2 N equations with 2 N unknowns. Once the coefficients C_{ n } are found, the expansion coefficients A_{ n } and B_{ n } can be evaluated straightforwardly via Equations 18 and 19.
where Re(·) and Im(·) denote the real and imaginary parts of complex expressions, respectively. Note that for the computed results given below, the free wavefield u^{F} is directly evaluated from Equation 5.
Degeneration for limiting cases
Vacant canyon
When the filling layer in the valley is absent (i.e., β_{1} = β_{2} = 0), the model is merely the semi-circular vacant canyon. Hence, the expansion coefficients are A_{ n } = 0, B_{ n } = 0, and C_{ n } = 0. This gives u^{S2} = 0, and only u^{S0} exists. Thus, the series solution derived for such a limiting case is the exact analytical solution derived by Trifunac (1973).
Fully filled alluvial valley
Equations 31 to 34 are the solutions of simultaneous equations derived by Trifunac (1971) for the fully filled semi-circular alluvial valleys.
Horizontal free surface
When the filling materials in regions 1 and 2 have the same mechanical properties (i.e., ρ_{1} = ρ_{2} and c_{1} = c_{2}, and thus μ_{1} = μ_{2} and k_{1} = k_{2}), a fully filled alluvial valley becomes a horizontal free surface without any surficial discontinuities. Clearly, in such a condition,${\widehat{\mathit{A}}}_{\mathit{n}}$ and${\widehat{\mathit{B}}}_{\mathit{n}}$ in Equations 33 and 34 are zero because W_{ n } in Equation 35 becomes zero. This signifies that all the scattered waves vanish in the absence of alluvium. By applying the Wronskian relation (Lebedev1965) to simplify the denominators of Equations 31 and 32, and then utilizing Equations 28 to 30, the wavefields in region 2 recover the free wavefields shown in Equation 6.
Results and discussion
The displacement amplitude of the incident waves is taken to be one unit. All the following simulations are done using a desktop computer with a 3.40 GHz Intel® Core™ i7-3770 CPU (Intel, Santa Clara, CA, USA) and 8.00 GB RAM under Windows 7 64-bit OS and MATHEMATICA programming environment (Wolfram, Champaign, IL, USA).
Convergence test
At the initial stage of calculations, a number of convergence tests are performed. The inner series with indices m (see Equations 48 and 49 in Appendix 2) are truncated and bounded from 0 to M - 1 terms. These internal sums should be accurately calculated via numerical testing for their convergence, thereby leaving only one parameter (i.e., the summation index n) to remove the problem of relative convergence.
Values of pertinent parameters for different inner truncation indices
M | Low-frequency case (η = 1) | ||
---|---|---|---|
P _{1} | P _{2} | P _{3} | |
22 | 1.190294289687 | 3.494137369096 | 3.951746767643 |
24 | 1.190267947613 | 3.494149108380 | 3.951352255433 |
26 | 1.190267465292 | 3.494149365072 | 3.951351221806 |
28 | 1.190267458947 | 3.494149368736 | 3.951351210176 |
30 | 1.190267458962 | 3.494149368728 | 3.951351210224 |
32 | 1.190267458962 | 3.494149368728 | 3.951351210224 |
34 | 1.190267458962 | 3.494149368728 | 3.951351210224 |
High-frequency case ( η = 10) | |||
105 | 3.852549926081 | 3.798895709292 | 1.426239484464 |
110 | 3.852670425350 | 3.798897978157 | 1.425983729509 |
115 | 3.852672532000 | 3.798897841089 | 1.425996636539 |
120 | 3.852672269462 | 3.798898139431 | 1.425999548587 |
125 | 3.852672241997 | 3.798898064628 | 1.425997735750 |
130 | 3.852672217055 | 3.798898082794 | 1.425997818638 |
135 | 3.852672217334 | 3.798898082637 | 1.425997818635 |
140 | 3.852672217334 | 3.798898082637 | 1.425997818635 |
Low-frequency case ( η = 1) | |||
P _{ 4 } | P _{ 5 } | Error | |
22 | 0.500030672653 | 0.891741857615 | 75.0368864083 |
24 | 0.499811004983 | 0.891382133938 | 0.187004610300 |
26 | 0.499810783582 | 0.891381807308 | 4.47556145287 × 10^{-4} |
28 | 0.499810781914 | 0.891381803982 | 3.63315136472 × 10^{-6} |
30 | 0.499810781927 | 0.891381804004 | 1.61204492590 × 10^{-8} |
32 | 0.499810781927 | 0.891381804004 | 3.13190321119 × 10^{-9} |
34 | 0.499810781927 | 0.891381804004 | <10^{-10} |
High-frequency case ( η = 10) | |||
105 | 0.293334113173 | 0.421453729093 | 3.09171329268 |
110 | 0.293284625937 | 0.421398985186 | 1.79321185135 × 10^{-2} |
115 | 0.293286828405 | 0.421402108231 | 9.05131671893 × 10^{-4} |
120 | 0.293286952154 | 0.421402250130 | 2.04211367705 × 10^{-4} |
125 | 0.293286901718 | 0.421402154841 | 1.27127443954 × 10^{-4} |
130 | 0.293286913103 | 0.421402167992 | 5.81262142562 × 10^{-6} |
135 | 0.293286912958 | 0.421402167820 | 4.96550950368 × 10^{-8} |
140 | 0.293286912958 | 0.421402167820 | <10^{-10} |
Values of pertinent parameters for different outer truncation indices
N | Low-frequency case (η = 0.5) | ||
---|---|---|---|
Error | Elapsed time | Memory | |
6 | 2.27 | 0.85 | 11.11 |
8 | 0.63 | 1.20 | 12.19 |
12 | 0.29 | 1.32 | 14.06 |
16 | 0.017 | 1.63 | 15.62 |
28 | 0.0026 | 3.23 | 20.70 |
High-frequency case ( η = 12) | |||
70 | 26.64 | 23.89 | 44.46 |
78 | 13.95 | 25.49 | 46.61 |
88 | 2.93 | 29.87 | 52.79 |
100 | 1.41 | 36.04 | 59.74 |
120 | 0.51 | 46.46 | 72.13 |
126 | 0.12 | 49.89 | 78.04 |
138 | 0.07 | 57.51 | 86.07 |
148 | 0.0086 | 64.44 | 93.09 |
Validation for the completely empty case
Validation for the fully filled case
In contrast, when the upper surface of the alluvial layer approaches the ground level, the computed results can approximate those for the fully filled valley. The exact analytical solution to SH-wave scattering induced by a semi-circular alluvial valley obtained by Trifunac (1971) serves as the benchmark. The analytical solutions are displayed by open circles in Figure 2b. Results for η = 0.5 at α = 30° when β_{1} = - 87°, - 89°, and - 89.999° with β_{2} = 80°, 86°, and 89°, respectively, are shown in Figure 2b. The values of ρ_{2}/ρ_{1} and c_{2}/c_{1} are 0.6667 and 0.5, respectively. Figure 2b exhibits good consistency between the present results and those of Trifunac (1971) when the filling level of alluvial layer rises gradually towards the top of the valley. Figure 2b thus suggests that the present model is valid.
Surface motions in the frequency domain
Mechanical properties for the three materials adopted
ρ_{2}/ρ_{1} | c_{2}/c_{1} | μ_{2}/μ_{1} | |
---|---|---|---|
Material 1 | 0.88 | 0.8 | 0.5632 |
Material 2 | 0.85 | 0.6 | 0.3060 |
Material 3 | 0.82 | 0.4 | 0.1312 |
The computed results revealing the effect of the filling level of soft alluvial layer (i.e., material 3) on the displacement amplitudes are shown in Figure 3b,c,d,e,f for α = 0°, 45°, 90°, - 45°, and - 90°, respectively, and when η = 1. Owing to the valley asymmetry, asymmetric motions under symmetric excitation can be found in Figure 3b. For obliquely incident cases in Figure 3c,e, the peak amplitudes of motions increase with the filling level. In Figure 3b,c,d,e,f, the number of local maximum amplitudes increases when the filling level of the alluvial layer rises.
Overall, the surface motions within and around the valley are dependent not only on the filling level and mechanical properties of alluvial layers but also on the frequency and incident angle of input waves.
Surface and subsurface motions in the time domain
where f_{c} is the characteristic frequency and is set to be 2 Hz. Computations are made at discrete frequencies ranging from 0 to 8 Hz with an interval of 0.0625 Hz. The half-width of the valley top and the outer shear-wave velocity are 1 km and 1 km/s, respectively. The reference point for t = 0 when the plane waves pass by is specified at the position (x_{1}, y_{1})=(0 km, 4 km) for vertical incidence and at (x_{1}, y_{1})=(–4 km, 0 km) for grazing incidence.
Figure 10a shows that the incident pulse is partly reflected and partly transmitted at the soil-bedrock interface. The waves entering the deposits slow down and bend downwards because the input signal moves from a high-velocity layer to a low-velocity one. Figure 10b shows that two scattered waves (marked by white crosses) are generated when the incident pulse passes through the lower corners of the valley. The geometric spreading of reflected waves from the valley bottom (displayed with white asterisks in Figure 10a,b,c,d,e,f,g) reaches the horizontal ground surface and couples with scattered waves L 1 and R 1 generated from the upper corners of the valley (see Figure 10c,d,e,f,g). Reflected waves from the inclined surface of the valley (displayed with white hollow triangles in Figure 10b,c,d,e) cross through the soil-bedrock interface, then interact with scattered waves from the lower corners of the valley, and finally trigger scattered waves R 2 and L 2 from the upper corners of the valley (see Figure 10f,g,h,i,j). The amplitudes of scattered waves induced by reflected waves from the horizontal ground surface (see those displayed with yellow arrows in Figure 10e,f,g,h,i) are much weaker than those from the valley corners. Hence, it is not easy to recognize the scattered waves from valley corners in Figure 9a. The scattered waves R 3, L 3, R 4, and L 4 (see Figure 10h,i,j) can be generated from the waves transmitted from the lower corners of the valley. Overall, the upper and lower corners of the valley behave as new sources to generate waves.Figure 10c,d,e,f,g,h,i,j reveals that the surface waves emerge from the lower corners of the valley and travel along the topmost alluvial layer in opposite directions. The reflected waves continue to bounce back and forth between the bimaterial interface and the inclined zero-stress surface. This traps energy within the low-velocity filling layer. Interaction and interference between surface waves and multiple reflected waves are responsible for a long duration of ground shaking, amplified ground motions, and complicated waveforms in the alluvial region.
Conclusions
Herein, the problem of SH-wave scattering, induced by a semi-circular valley partially filled with an inclined alluvial layer, has been tackled and solved theoretically. The use of the robust RMT has given rise to a rigorous series solution. A novel form of Graf's addition formula is derived for angular wavefunctions constrained by an inclined free surface so that it is more general than those given in the literature for a horizontal free surface. With the aid of such a newly derived version of Graf's addition formula, the coordinate transformation for Bessel functions between two arbitrarily located polar coordinate systems can be performed conveniently. Disturbances in antiplane displacement fields have been evaluated and analyzed in both the frequency and time domains. Approximations of the extremely lowly filled valleys are consistent with the completely empty canyons, and approximations of the extremely highly filled valleys with the fully filled valleys. The frequency-domain results indicate that the peak amplitudes of motions may increase at low frequencies when the top surface of the filling layer steepens towards the illuminated region (i.e., the region facing the incident waves). If the incident angle bends towards the horizontal ground surface, the phenomenon of wave focusing is found to be significant, and spectral amplifications might reach up to approximately 8. The time-domain results show that the dynamic response of the valley is closely related to the interaction and interference between the surface waves and multiple reflected waves within the alluvial layer. The computed results presented herein can serve as a benchmark to validate mesh-based numerical simulations.
Appendix 1
Pertinent functions in Equations 14, 20, and 21
Appendix 2
Pertinent functions in Equations 25 and 26
Declarations
Acknowledgements
The authors are much obliged to the editor, Dr. Tatsuhiko Hara, and two reviewers for their encouragement and insightful and valuable suggestions and comments that have improved this paper. Additionally, the first and third authors are sincerely grateful for the financial support granted by the Ministry of Science and Technology, former National Science Council, Taiwan, Republic of China (Project Nos. NSC 102-2811-M-001-060 and NSC 102-2116-M-001-021, respectively).
Authors’ Affiliations
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