Indonesian Journal on Geoscience Vol. 7 No. 1 April 2020: 41-49
INDONESIAN JOURNAL ON GEOSCIENCE Geological Agency Ministry of Energy and Mineral Resources
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Locating Tremor Source with Polarization and Semblance Methods During the 2014 Crisis Period of Raung Volcano
Vico Luthfi Ipmawan1, Kirbani Sri Brotopuspito2, and Hetty Triastuty3
1Departement of Physics, Institut Teknologi Sumatera Jln. Terusan Ryacudu Way Hui, Lampung, Indonesia 2Departement of Physics, Universitas Gadjah Mada Jln. Sekip Utara Bulaksumur, Yogyakarta, Indonesia 3Centre for Volcanology and Geological Hazard Mitigation, Geological Agency Jln. Diponegoro No. 57 Bandung, Indonesia
Corresponding author: [email protected] Manuscript received: June, 4, 2018; revised: July, 4, 2019; approved: November, 19, 2019; available online: February, 24, 2020
Abstract - Raung is a basaltic-andesitic volcano with strombolian-type eruptive activity located in East Java Province, Indonesia. The seismic activity of this volcano increased on 11th November 2014 which was dominated by tremors. Due to the difficulty to distinguish the onset of body waves of tremor waveform, polarization and semblance methods were proposed and applied to locate the tremor source. The tremors recorded during November to December 2014 were analyzed. The results showed that the back-azimuth values obtained by the polarization method were around N 288o - 324o E in accordance with the direction of Raung summit, while the incidence angle ranged around N 81o - 89.3o E. The semblance method was performed on 2 x 2 km area around the summit. The result of the tremor source showed the distribution of epicentre extending N52o E to the northeast direction about ±2.1 km away from the Raung summit. Keywords: Raung, back-azimuth, incidence angle, volcanic earthquake © IJOG - 2020. All right reserved How to cite this article: Ipmawan, V.L., Brotopuspito, K.S., and Triastuty, H., 2020. Locating Tremor Source with Polarization and Semblance Methods During the 2014 Crisis Period of Raung Volcano. Indonesian Journal on Geoscience, 7 (1), p.41-49. DOI: 10.17014/ijog.7.1.41-49
Introduction surrounding rivers, Stail and Klatak Rivers. At that time, more than 1,000 people were killed by Raung, a basaltic-andesitic volcano, is located the flood and lahar. Another calamity eruptions in East Java Province. It is one of the most active occurred in 1597, 1730, and 1817. volcanoes in Indonesia. The characteristic eruption On the late October 2012, the status of Raung of this volcano is explosiveIJOG of which most have Volcano raised to level 2 alert after volcanic trem- been categorized as moderate explosions (Volca- ors were recorded. The exclusion zone was then nic Explosivity Index/VEI = 2), while in 1593 the placed with radius 3 km around the crater. Then, explosion was categorized as very large (VEI=5). a large eruption occurred on 8th November 2012 Raung has erupted at least fifty-seven times since where ash emission reached a height of ± 9 km. 1593, and one notorious eruption occurred in 1638. Strombolian eruptions were observed with 200 The eruption generated and poured lahar into the m in height above the crater.
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In 2014, a crisis period of Raung Volcano Raung is shown in Figure 1. Tremor is a volcanic started from November 2014, which then the earthquake that occurs in a long period, lasting eruption took place on 29th June 2015. The from several minutes to several days, preceding seismic activity of the volcano was fluctuated and/or accompanying most volcanic eruptions from November 2014 to June 2015. Volcanic (Konstantinou and Schlindwein, 2002). Physical tremors had been recorded since the initial crisis processes generating volcanic tremor involve period of this volcano on 11th November 2014, complex interactions of magmatic fluids with after which the seismic activity was dominated the surrounding rocks (Zobin, 2017). Tremor by tremors. Some tremors occurring on 12th is a powerful tool for better understanding the November 2014 had been recognized as quasi- physical processes controlling explosive erup- harmonic tremors (Ipmawan et al., 2018a). By tions. There are good agreements between tremor the end of November 2014, tremors became and eruption activities. In particular, a shift of continuous where the dominant frequency of dominant frequencies towards lower values was this volcano had the range of 0.95 ± 0.15 Hz noted which corresponds to increasing explosive (Ipmawan, 2018b). activity (Cannata et al., 2007). Raung Volcano is monitored by the Centre for Generally, an epicentre of earthquake can be Volcanology and Geological Hazard Mitigation obtained using P-wave and S-wave arrival time. (CVGHM) using four seismic stations, namely: In contrast, both P-and S waves of tremor interfere RAUN, MLTN, KBUR, and MLLR. All the sta- each other, which makes their arrival time be dif- tions were equipped with L-4C 1 Hz 1-component ficult to distinguish (Hofstetter and Malone, 1986). seismometers, except MLLR station that was Polarization is a method to obtain the epicentre of equipped with a L-22D 2 Hz 3-channel seis- tremor that was introduced by Jurkevics (1988). mometer. The distribution of seismic stations in This method does not require identification onset
114o0'0"E 114o5'0"E 114o10'0"E 5'0"S 5'0"S o o 8 8 2500 1000 2000 2500
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114o0'0"E 114o5'0"E 114o10'0"E km 0 1 2 4 6 8
Figure 1. Distribution of seismic stations at Raung Volcano.Green solid circles and red solid triangle denote seismic stations and the peak of Raung, respectively.
42 Locating Tremor Source with Polarization and Semblance Methods During the 2014 Crisis Period of Raung Volcano (V.L. Ipmawan et al. ) of body wave arrival time. Sugianto (2014) ap- blance methods were combined for determining plied this method to analyze the seismic source a better tremor location. location of Bledug Kuwu mud volcano in Central Java, Indonesia. The method requires at least three Spectral Coherence 3-components seismometers which are located Spectral coherence is a statistic method used for in different quadrants. The parameters obtained testing the degree of linearity between two random through this method are the back azimuth and the signals (Koopmans, 1995; Priestley, 1981). This incidence angle of the source. method can also be used to identify the similarity The semblance method can also locate source of signal content in frequency domain. locations of tremor without any information of By considering two random signals V(t) and the onset of body waves. This method is used for W (t), then Y (t) is defined as: locating the epicentre and hypocentre of tremor T (Kawakatsu et al., 2000; Andinisari et al., 2013) Yt ( ) = [V()tW ()t ] ...... (1) and the migration of tremor source (Takagi et al., 2006). The Discrete Fourier Transform of X (t) is: This study located tremors originating at Raung Volcano using polarization and semblance meth- N TY()ω = (t)eitω ...... (2) ods. The result is compared with another seismic ∑ t=1 activity during the crisis period of the volcano. There are many studies that discuss about Raung Then function φ(ω) is defined as: activity, but not many discussing the position of 1 the source of volcanic tremors in detail. φω()= YY()ωωT ()...... (3) N
φω() φω() Methods and Materials WW WV ...... (4) φω()= * φωVW () φωVV () Some stages were applied to tremors for ob- taining the tremor source location. First, tremor Thus, complex coherence can be written as data were analyzed with spectral coherence (Stoicaand Moses, 1997): method to know the bandpass filter range for the polarization method. The results are important to φω() C = WV ...... (5) understand whether the signal at this frequency WV 12 . []φωWW ()φωVV () originating from the same source, assumed by
Raung activity, or not. Second, the polarization Cwv is complex coherence and |Cwv| is spectral method was applied to tremor data to obtain back coherence. azimuth and incidence angle. These suggest the The value of spectral coherence is between estimation of epicentre and hypocentre of Raung 0≤|Cwv|≤1. tremor, respectively. Third, the semblance method was performed of which the output was the dis- The minimum value means that both signals tribution of semblanceIJOG location with 2 x 2 km have no similarity. The maximum value means area based on semblance coefficient. This method that both signals are perfectly similar. was chosen due to most tremor waveforms had an emergent onset to the extent that the picking Polarization of the first arrival was almost impossible and the Matrix X= |xij| is defined as a set of sample travel-time location method used for earthquakes data from 3-component seismometer with i = 1, could not be applied. The polarization and sem- 2, 3 and j = 1, 2, … ,M. The i index refers to the
43 Indonesian Journal on Geoscience, Vol. 7 No. 1 April 2020: 41-49 component of seismometer, for i=1=Z, i=2=N, The sign function is introduced to resolve the and i=3=E. 180 o ambiguity by taking the positive vertical
A polarization can be analyzed from the cova- component of u1. Similarly, the apparent inci- riance matrix S of data (Jurkevics, 1988): dence angle of rectilinear motion, as measured from vertical, may be obtained from the vertical T N XX 1 direction cosine of u . == 1 Sik ∑ xxij jk ...... (6) MM j=1 −1 ...... (10) T means tranpose from a matrix. The covari- Pi−=nc cos u11 ance matrix S is 3x3, real and symmetric. Semblance Method Semblance is the measure of the similarity SSZZ ZN SZE of multichannel data defined as (Almendros and S = SSS ...... (7) ZN NN NE Chouet, 2003): SSZE NE SEE 2 M N ∑∑Ujii()τ +∆t Explicitly, the terms of S are the auto- and j=1 i=1 S = ...... (11) cross-variances of the three components of mo- o M N ()τ +∆ tion. NU∑∑ ii jt j=1 i=1 The eigen value and the eigen vector of matrix S can be obtained by: Where: Δt denotes the interval of sampling, (S-λ2I)u = 0 ...... (8) τi is the origin time of the window sampling of the ith channel,
Where: Uii()τ +∆ jt is the jth time sample of the signal I is 3x3 identity matrix and U recorded on the ith channel, and 0 is a column vector of zeros. M and N represent the number of samples in the
The eigen vectors u1,u2, and u3 are orthogonal. window and number of channels, respectively.
The length of eigen vector ui = uzii123ˆ ++ unˆˆ ue i So is a number measuring the similarity of either is arbitrary, but it can be normalized to be unit waveform and amplitude. vector. The eigen vector components uij are the length of eigen vector projection in Z, N, and E In this research, only the similarity of wave- axes. form is interesting, so equation (1) can be modi- fied as (Almendros and Chouet, 2003):
Geometrically, the eigen value λi and the eigen 2 vector u shape an ellipsoid. Once the principal M N i ' 1 Ujii()τ +∆t axes of the polarization ellipsoid are estimated, So = 2 ∑∑ ...... (12) MN j=1 i=1 σ i the particle motion in the data window is deter- mined. Information describing the characteristics of ground motion is extractedIJOG using attributes 1 M στ=+Uj()∆t 2 computed from the principal axes. The azimuth where: ii∑ i is the rms M j=1 of P-wave propagation can be estimated as: (root-mean-square) velocity of the signal within the selected time window sampling the ith channel. −1 usignu() P- back-azimut Pt= an 31 11 .. (9) The value of semblance coefficient that is us21 ignu()11 higher than 90% of all semblance coefficient
44 Locating Tremor Source with Polarization and Semblance Methods During the 2014 Crisis Period of Raung Volcano (V.L. Ipmawan et al. ) value produced can be considered as the epicentre The tremors with approximately 3.0 to 5.5 of tremor (Almendros and Chouet, 2003). minutes in duration were analyzed using the polarization method. The length of window Seismic Waveform is 30 seconds with 50% overlaping for the Seismic data used in this study were obtained window shift. Before the polarization method from seismic stations at the Raung Volcano was performed, bandpass filter around 1.17 operated by the Centre for Volcanology and Hz (1.1 to 1.24 Hz) was applied to each signal. Geological Hazard Mitigation (CVGHM). The filter frequency range was obtained by There are five seismometers at Raung Volcano, the spectral coherence between KBUR-MLLR namely: KBUR (located 4 km from the summit and KBUR-RAUN waveforms. Both spectral crater), MLLR (6 kmaway), RAUN (6 km away), coherence showed the same results at 1.17 Hz MLTN (6 km away), and POSR (14 kmaway). with spectral coherence coefficients of 0.7 and Unfortunately, MLTN seismometer was damaged 0.5 Hz, respectively (Figure 2). due to a technical reason. The polarization method Polarization parameters, such as back-azimuth can only be applied on waveform recorded at and incidence angle, from various dates were 3-component seismometer. Thus, the sesimic obtained. The source location could be interpreted data recorded at MLLR seismic station was used from these parameters.The result showed that to analyze using the polarization method.The back-azimuth had dominant of 288o to 324o in spectral coherence method was applied to KBUR- direction (Figure 3). Meanwhile, the incidence RAUN and KBUR-MLLR, in order to know angle obtained using polarization method showed the band pass filter range for the polarization 81o to 89.3o in direction (Table 2). The consistency method. The POSR seismic station is used as the of incidence angle value was also showed on reference to distinguish between volcanic and Raung tremor. tectonic earthquake waveforms since the station All those parameters were relatively constant is located quite far from the summit. Furthermore, during the various activities on November - the semblance method was applied to tremors December 2014. recorded at KBUR, MLLR, and RAUN. The semblance method was applied to KBUR, MLLR-Z, and RAUN recordings with the duration of 30 seconds in 19th November 2014. Result and Analysis The length is adequate to obtain information about particle motion of the tremors. Grid of 2 x The waveforms recorded at MLLR on 12th, 2 km was applied near Raung caldera for locating 19th, 30th November 2014 and 12th, 25th December the distribution of epicentre. The area was divided 2014 were used for the polarization analysis. into 100 m which produced 41 x 41 nodes, and These dates were chosen due to some significant assuming homogenous isotropic medium. activities recorded at Raung Volcano as seen in The result showed that the distribution of Table 1. tremor epicentre was extended in the northeast Table 1. Activities of RaungIJOG Volcano on 2014 Crisis Period No Date and Time Raung Activity 1. 12th November 2014 01:00:00 Quasi-harmonic tremor occurred 2. 19th November 2014 20:00:00 White plume emmitted approximately 50 m high above the summit 3. 30th November 2014 13:40:00 White plume emmitted approximately 500 m high above the summit 4. 12th December 2014 02:10:00 Rumbling was frequently heard at the observation post 5. 25th December 2014 20:00:00 Incandescence was seen at the crater
45 Indonesian Journal on Geoscience, Vol. 7 No. 1 April 2020: 41-49
x106 x106 10 10 a PSD KBUR d PSD KBUR
5 5
0 0 0 2 4 6 8 10 0 2 4 6 8 10 x105 x105 4 4 b PSD MLLR e PSD RAUN
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0 0 0 2 4 6 8 10 0 2 4 6 8 10 0.8 0.8 c SPECTRAL COHORENCE f SPECTRAL COHORENCE KBUR-MLLR KBUR-RAUN 0.6 0.6
0.4 0.4
0.2 0.2
0 0 0 2 4 6 8 10 0 2 4 6 8 10 Frequency (Hz) Frequency (Hz)
Figure 2. Spectral coherence between KBUR-MLLR and KBUR-RAUN waveforms. Both have spectral coherence frequency dominant at 1.17 Hz. (a) Power Spectral Density (PSD) of KBUR, (b) PSD of MLLR, (c) spectral coherence between KBUR-MLLR, (d) PSD of KBUR, (e) PSD of RAUN, (f) spectral coherence between KBUR-RAUN.
0 0 0 330 30 330 30 330 30
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(a) 0 (b) 0 (c) 330 30 330 30
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210 150 210 150 180 180 IJOG (d) (e) Figure 3. Back-azimuth of Raung tremors in various dates having dominant values around 288o to 324o. (a). Back-azimuth of 12th November 2014; (b). 19th November 2014; (c). 30th November 2014; (d). 12th December 2014; and (e). 25th December 2014. direction. By assuming tremor velocity was of epicentre was obtained based on the highest
2,000 m/s and constant due to the wave travels value of semblance coefficient (S'o) having dark- in homogenous isotropic medium, the prediction red colour in Figure 4.
46 Locating Tremor Source with Polarization and Semblance Methods During the 2014 Crisis Period of Raung Volcano (V.L. Ipmawan et al. )
Table 2. Incidence Angle of RaungTremors in Various Dates On 12th and 19th November 2014, the back- azimuth as seen on Figure 3 directed not only to No Date Incidence Angle the summit of Raung Volcano, but also to around 1. 12th November 2014 83.6o - 89.3o o o 2. 19th November 2014 80.3o - 88.2o 18 to 54 . This direction may be associated 3. 30th November 2014 80.6o - 88.9o with Ijen Volcano complex located close to 4. 12th Desember 2014 81.0o - 89.3o RaungVolcano. It could be the seismic signals 5. 25th Desember 2014 82.0o - 89.3o that came from Ijen Volcano, since sometimes Raung tremors were also recorded at Ijen seismic
2.0 stations. The distance between Raung MLLR seismic station and Ijen summit is about 17 km. 1.5 The incidence angle of tremor obtained o 1.0 through polarization method ranges about 81 to 89.3o (Table 2). It can be interpreted that the 0.5 source of tremor is relatively shallow to medium
0
km in depth. By assuming homogeneous isotropic medium, the source depth could be obtained -0.5 with a simple Pythagoras formula. Based on -1.0 the semblance and polarization methods, the epicentre of tremor was located at 6.2 km away -1.5 from MLLR station, and the depth could be -2.0 -2.0 -1.5 -1.0 -0.5 0 0.5 1.0 1.5 2.0 obtained at about 0.07 to 1.03 km. km The epicentre distribution of the tremor source Figure 4. Result of semblance location with 2 x 2 km area. elongated to the northeast direction (Figure 3).It The dark-red coloured boxes are the epicentre predictions. could be due to the small number of seismometers and their distribution does not cover all azimuth Discussion directions. KBUR seismometer is located on the third quadrant, whereas MLLR and RAUN are Spectral coherence from two pairs of tremors on the fourth quadrant. For a good constraint, at shows the same frequency at 1.17 Hz. This least, five seismometers should be deployed in consistency of dominant frequency at 1.17 Hz three different quadrants. reveals that the tremors has similarities to each The polarization method obtained only the other at frequency 1.17 Hz (Figure 2). It can also direction of back-azimuth without knowing be intrepreted that the signal at this frequency exactly the distance of the epicentre from is originated from the same source, and the MLLR 3-component seismometer. The exact frequency is derived from Raung activity. distance is preferably obtained by deploying at The back-azimuth has dominant values least three 3-component seismometers around around 288o to 324o (Figure 3a and 3b) for the volcano. The distance was obtained by the the whole tremor waveform recorded during intersection of the back-azimuth directions November - December 2014. These results are in from the polarization method applied to three accordance with theIJOG direction of the summit of RaungVolcano, which is located in the northwest 3-component seismometers. of MLLR seismic station (Figure 1). There is The assumed epicentre obtained by combining no significant temporal variation of polarization polarization and semblance methods can be seen parameter associated with various activities of in Figure 5. The epicentre of tremor source is ±2.1 o RaungVolcano between November and December km away and 52 NE direction from the Raung 2014. summit.
47 Indonesian Journal on Geoscience, Vol. 7 No. 1 April 2020: 41-49
114o0'0"E 114o5'0"E 114o10'0"E 5'0"S 5'0"S o o 8 8 1000 2000 2500
1500
1500
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1000 10'0"S 10'0"S o o 8 8
N
114o0'0"E 114o5'0"E 114o10'0"E
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Figure 5. A combination result of semblance and polarization methods. The solid red circle is the epicentre and the solid green circle is the location of MLLR station.
Conclusions data. The research is supported by The Ministry of Research, Technology, and Higher Education The back-azimuth of Raung tremors are of the Republic of Indonesia. around 288o - 324o in accordance with the di- rection of Raung summit. The incidence angle of Raung tremors is relatively constant at References around 81o - 89.3o. There is no relation between various activities on Raung and polarization Almendros, J. and Chouet, B., 2003. Performance parameters. of Radial Semblance Method for the Location The semblance method performed on 2 x 2 of Very Long Period Volcanic Signals. Bul- km area around the Raung summit shows the letin of Seismological Society of America, 93 extended distribution of the epicentre in the (5), p.1890-1903. DOI: 10.1785/0120020143 northeast direction. The epicentre of tremor Andinisari, R., Maryanto, S., and Nadhir, A., source obtained through the combination of 2013. Preliminary Study on the Determina- polarization and semblance methods is ±2.1 km tion of Volcanic Tremor Epicenter Using away and is based on 52o NE direction from the Semblance Method (Case Study of Sakurajima Raung summit. Volcano). Natural B, 2 (2), p.172-177. DOI: IJOG10.21776/ub.natural-b.2013.002.02.12 Cannata, A., Catania, A., Alparone, S., and Acknowledgements Gresta, S., 2008. Volcanic tremor at Mt. Etna: Inferences on magma dynamics during The authors would like to thank the Centre for effusive and explosive activity. Journal of Volcanology and Geological Hazard Mitigation Volcanology and Geothermal Research, 178 (CVGHM) for providing the Raung Volcano (1), 19. DOI: 10.1016/j. jvolgeores.2007.11.027.
48 Locating Tremor Source with Polarization and Semblance Methods During the 2014 Crisis Period of Raung Volcano (V.L. Ipmawan et al. )
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