Magnitude–frequency distribution of volcanic explosion earthquakes
- Takeshi Nishimura^{1}Email author,
- Masato Iguchi^{2},
- Mohammad Hendrasto^{3},
- Hiroshi Aoyama^{4},
- Taishi Yamada^{4},
- Maurizio Ripepe^{5} and
- Riccardo Genco^{5}
Received: 28 March 2016
Accepted: 6 July 2016
Published: 20 July 2016
Abstract
Magnitude–frequency distributions of volcanic explosion earthquakes that are associated with occurrences of vulcanian and strombolian eruptions, or gas burst activity, are examined at six active volcanoes. The magnitude–frequency distribution at Suwanosejima volcano, Japan, shows a power-law distribution, which implies self-similarity in the system, as is often observed in statistical characteristics of tectonic and volcanic earthquakes. On the other hand, the magnitude–frequency distributions at five other volcanoes, Sakurajima and Tokachi-dake in Japan, Semeru and Lokon in Indonesia, and Stromboli in Italy, are well explained by exponential distributions. The statistical features are considered to reflect source size, as characterized by a volcanic conduit or chamber. Earthquake generation processes associated with vulcanian, strombolian and gas burst events are different from those of eruptions ejecting large amounts of pyroclasts, since the magnitude–frequency distribution of the volcanic explosivity index is generally explained by the power law.
Keywords
Magnitude Exponential distribution Power law ExplosionIntroduction
Volcanic explosion earthquakes (hereafter termed EXs) are earthquakes that are observed in vulcanian and strombolian eruptions, or gas bursts, which often accompany strong air shocks or infrasonic signals. A pioneer study by Minakami (1960) first defined EXs, classifying volcanic earthquakes into four types: A-, B-type, explosion earthquake, and tremor. He indicated that EXs at Sakurajima, Japan, follow Ishimoto–Iida’s formula of n(A) = kA ^{−m }, where n(A) represents the number of earthquakes with a maximum amplitude of A, m is the coefficient called Ishimoto–Iida’s m value, and k is a proportional coefficient (Ishimoto and Iida 1939). This relationship is linked to the Gutenberg–Richter equation (G–R eq.) that explains the magnitude–frequency distribution of earthquakes in general, and the m value is related to the b value in the G–R eq. as m = b + 1 (Asada et al. 1950; Suzuki 1953). These observed magnitude–frequency distributions are often termed power laws, which are interpreted to be related to fractal properties and self-similar systems.
Since Minakami’s pioneering work in 1960, magnitude–frequency distributions have been investigated at active volcanoes (e.g., Tanaka 1967; Shimozuru et al. 1971; Tanaka et al. 1972; Del Pezzo et al. 1974; Rowe et al. 2000). These previous studies often plotted the number of EXs versus amplitude in double-logarithmic graphs to estimate m values. However, most of the figures presented seem not to be well matched with the Ishimoto–Iida’s formula (power law). For example, Tanaka (1967) pointed out a break in the Ishimoto-Iida’s formula at large amplitudes for EXs at Sakurajima and interpreted the break as related to crater size. Magnitude–frequency distributions of EXs associated with strombolian eruptions at Akita-Komagatake, Japan, were explained by combinations of two power laws using two m values (Tanaka et al. 1972). Rowe et al. (2000) examined the magnitude–frequency distribution of EXs associated with frequent strombolian explosions within the summit crater lake at Erebus volcano, Antarctica. They showed that the distribution follows an approximate power law with b value of about 1.7 and pointed out that an inflection in the cumulative distribution curve may be due to low detection level of small events, distinct source populations or a preferred median bubble size. These previous studies indicate that EXs do not follow a simple relation as represented by the Ishimoto–Iida’s formula or G–R eq. Such divergence of the magnitude–frequency distribution is also found for volcanic tremors. Benoit and McNutt (2003) analyzed duration times and amplitudes of volcanic tremors and followed exponential rather than power-law scaling.
Although magnitude–frequency distributions provide some of the most basic and important information to understanding explosive eruption processes, investigations of the statistical characteristics of EXs are limited in number. In the present study, therefore, we examine the magnitude–frequency distribution characteristics of EXs at different volcanoes. The EXs we analyze are those associated with vulcanian and strombolian eruption styles and gas bursts at Sakurajima, Suwanosejima, and Tokachi-dake in Japan, Semeru and Lokon in Indonesia, and Stromboli in Italy. Note that Plinian style explosive eruptions are associated with eruption tremors (e.g., McNutt and Nishimura 2008) rather than EXs, and they are not the target of the present study. Since EXs are considered to be caused by rapid conduit pressure changes in volcanic explosions, magnitude–frequency distributions provide us with the basic statistical attributes of eruptions and clues to understanding eruption dynamics. We examine the magnitude–frequency distribution of EXs at the six volcanoes identified above and discuss their relationship to the volcanic systems.
Magnitude–frequency distributions
Vulcanian eruptions at volcanoes in Japan
Tokachi-dake volcano exhibited explosive activity from December 1988 to March 1989, and 23 explosive eruptions are listed in Table 1 of Okada et al. (1990) where date and time, amplitude of EXs as well as airwaves are summarized. We use half-amplitudes of EXs that are recorded at JMA-A (TVO) station 4.5 km NNW from the crater. The number of EXs occurring during this eruptive sequence is small, but we can see in Fig. 3b that the exponential distribution seems to explain the observed data well.
Vulcanian eruptions at volcanoes in Indonesia
Figure 1b shows the locations of Semeru and Lokon volcanoes in Indonesia. We analyze seismic data recorded during vulcanian explosive activity in March–April 2007 and gas burst activity in March–April 2009 at Semeru (Nishimura et al. 2013). Vulcanian explosions and gas bursts occurred continuously, every few minutes to tens of minutes in 2007 and 2009, respectively. Both kinds of explosions occurred within the same summit crater. Seismic signals were recorded by a broadband seismometer (STS-2, Streckeizen Ltd.) at a station 0.5 km north of the crater. Hence, most of large seismic events in the continuous records were associated with the repeated crater explosions. We numerically extract EXs based on when the vertical seismic amplitude exceeds a threshold level of 2 × 10^{−4} m/s, which is about 10–40 times the ambient noise level. We measure maximum amplitude in the raw broadband seismometer records for each EX. Tectonic earthquakes contamination in the records is eliminated by checking whether or not clear P- and S-waves are observed in the seismograms.
EXs at Lokon are manually selected from continuous records of a broadband seismometer (Trilium40, Nanometrics), installed 1.7 km from the active crater, for a period of 1 year from September 2012. We measure maximum amplitudes from the raw records. Figure 4c plots the cumulative number of EXs versus maximum seismic amplitude in double-logarithmic and semilogarithmic graphs. Like the Semeru volcanoes, an exponential distribution explains the observed data at Lokon well.
Strombolian eruptions at Stromboli volcano, Italy
It is noteworthy to mention that we only analyze data of standard activity of Stromboli volcano, as no major explosion or paroxysmal activity occurred during our observation period. It is necessary to analyze data over long observations time periods of more than 10 years to encompass the entire eruptive activity types of Stromboli.
Statistical tests on the magnitude–frequency distributions
So far, we have visually examined EX magnitude–frequency distributions in graphs and indicated that they are best explained by exponential relationships at all of the studied volcanoes, except Suwanosejima. In the present section, we statistically examine the observed magnitude–frequency distributions.
We first analyze correlation coefficients of the EX magnitude–frequency distributions on the double-logarithmic and semilogarithmic graphs (Figs. 2, 3, 4, 5). The correlation coefficients show high values of more than about 0.9 in both types of graph for all of the EXs. This suggests that both relationships explain the observed data well. However, it is clear that correlation coefficients for the semilogarithmic graphs are larger than the double-logarithmic ones for all of EXs except Suwanosejima. All of the semilogarithmic graph coefficients are larger than 0.89, and most are larger than 0.97.
Estimated parameters of explosion earthquakes at active volcanoes
Volcano (observation period) | Corr. coeff. | D _{max} | N _{b} | \(D_{\hbox{max} } \sqrt {N_{\text{b}} }\) | Δ (km) | Freq. (Hz) | D _{R} (cm^{3}) | a _{0} | Unit | A _{0} (mm) | M | |||
---|---|---|---|---|---|---|---|---|---|---|---|---|---|---|
D-log | s-log | D-log | s-log | D-log | s-log | |||||||||
Sakurajima Minami-dake (1963–1999) | 0.892 | 0.996 | 0.310 | 0.171 | 30 | 1.698 | 0.938 | 2.7 | 1.0 | 12,324 | 0.0750 | mm | 0.0750 | 1.8 |
Sakurajima Showa crater (2008–2011) | 0.948 | 0.989 | 0.170 | 0.055 | 21 | 0.777 | 0.253 | 3.0 | 1.0 | 4919 | 0.0284 | mm | 0.0284 | 1.4 |
Suwanosejima (January–June, 2011) | 0.998 | 0.891 | 0.040 | 0.206 | 27 | 0.207 | 1.070 | 0.5 | 2.0 | 1433 | 0.1800 | mm/s | 0.0143 | −0.2 |
Tokachi-dake (December 16, 1988–March 5, 1989) | 0.907 | 0.987 | 0.202 | 0.102 | 10 | 0.638 | 0.321 | 4.5 | 1.0 | 5049 | 0.0238 | mm | 0.0238 | 1.7 |
Semeru Vulcanian (March 18–April 10, 2007) | 0.967 | 0.995 | 0.044 | 0.043 | 52 | 0.318 | 0.312 | 0.5 | 1.0 | 13,286 | 1.1800 | mm/s | 0.1879 | 0.9 |
Semeru Gas bursts (March 17–April 10, 2011) | 0.955 | 0.997 | 0.054 | 0.043 | 36 | 0.323 | 0.257 | 0.5 | 1.0 | 7927 | 0.7040 | mm/s | 0.1121 | 0.7 |
Lokon (September 2012–September 2013) | 0.934 | 0.973 | 0.223 | 0.128 | 18 | 0.948 | 0.541 | 1.4 | 1.0 | 7744 | 0.4110 | mm/s | 0.0654 | 1.2 |
Stromboli 1–8 Hz (June 2014) | 0.940 | 0.989 | 0.073 | 0.058 | 39 | 0.454 | 0.360 | 0.4 | 4.0 | 49 | 0.0097 | mm/s | 0.0004 | −1.9 |
Stromboli 0.05–0.2 Hz (June 2014) | 0.965 | 0.996 | 0.078 | 0.024 | 33 | 0.446 | 0.135 | 0.4 | – | – | 0.2700 | m/s | – | – |
Based on these two statistical examinations, we conclude that exponential distributions well match the observed EX magnitude–frequency distributions. This strongly suggests the existence of a characteristic scale in the generation of explosions during each eruptive activity at these volcanoes.
Discussion
Results shown in the previous sections may be unreliable if low amplitude EXs were not correctly counted due to large noise amplitudes. For example, by removing the five lowest-amplitude bins from the Sakurajima EXs plotted on the double-logarithmic scale, correlation coefficients increase from 0.892 to 0974 for 1963–1999 data and from 0.948 to 0.996 for 2008–2011 data. However, EXs are some of the largest earthquakes occurring at Sakurajima and the signal amplitudes are well beyond the noise level. Hence, SVRC correctly detects EXs without interference from noise signals. At Semeru, EXs were selected by setting a high threshold level (10–40 times the noise level), and the magnitude–frequency distributions show a convex shape even in the high amplitude range (see Fig. 4). Similar convex shapes are recognized in full amplitude ranges of Stromboli volcano. These results suggest that low detection levels of EXs in the low amplitude range are not the main cause of the convex shape of the magnitude–frequency distributions, or of the low correlations for the power-law distributions.
We have fitted a straight line on the double-logarithmic scale magnitude–frequency distribution at each volcano. However, as Tanaka et al. (1972) explained in an investigation of data from Akita-Komagatake, Japan, the magnitude–frequency distribution at volcanoes such as Semeru, Stromboli, and Tokachi may be fitted by two straight lines on the double-logarithmic scale. For example, we can see inflections in the magnitude–frequency distribution at about −4.8 on the horizontal axis for Stromboli data, at about −2.8 and −3.1 for Semeru vulcanian and gas burst data, respectively, and −4.7 for Tokachi volcano. Fitting two straight lines to the data implies that the magnitude distribution follows two different power laws; we cannot statistically reject this possibility. Also, we are not able to objectively distinguish it from the exponential distribution, although the power laws are limited in narrow ranges of <1 order. If the distributions comprise two power laws, the inflection point may be related to a scale change in the magma system to generate explosions.
EXs are often explained by a single force acting at the shallow part of a volcano (e.g., Kanamori et al. 1984; Ohminato et al. 2006) or by pressure release of a magma chamber (Uhira and Takeo 1994). The amplitude of the single force is proportional to the product of the cross-sectional area of the vent and the pressure stored before explosion. The amplitude is related to the time derivative of the seismic moment that is defined by the volume of the chamber. These theoretical predictions indicate that the amplitudes of these sources distribute exponentially. Since EXs at each volcano repeatedly occurred from the same vent or crater, we infer that the characteristic scales are related to the size of conduit or chamber, and fluctuations of excess pressure stored before explosion may change for each explosion.
We have represented the observed exponential distributions by \(\log_{10} N = N_{0} \exp ( - a/a_{0} ),\) where N is the number of events at the maximum amplitude of a, N _{0} is the constant related to the total number of events. The parameter a _{0} is measured from the slope of the semilogarithmic graphs. To compare the characteristic scales of EXs at different volcanoes, we use the reduced displacement D _{R} that is an indication of the strength of the seismic source (Aki and Koyanagi 1981), although D _{R} is generally used to evaluate volcanic tremor sources. EXs generally excite large amplitude Rayleigh waves from a shallow depth in the conduit (Kanamori and Given 1983; Tameguri et al. 2002). Hence, we have assume that the dominant waves are surface waves and determine the reduced displacement, D _{R}, for the surface wave, which is expressed as \(D_{\text{R}} = A_{0} \sqrt {\lambda r/2}\) where r is the epicentral distance, A _{0} the maximum amplitude in displacement, and λ the wavelength. We assume a homogenous structure with a surface wave velocity of 1000 m/s, and the wavelength of the surface waves is calculated from the dominant frequencies f. When the observed maximum amplitude is in velocity, we obtain the displacement by using the equation \(A_{0} = a_{0} /2\pi f.\) Table 1 compares the reduced displacements for different EXs. Stromboli data at 0.05–0.2 Hz are excluded from the analysis, because the long-period waves are near-field and not surface waves. We also evaluate the seismic magnitude M using Tsuboi’s formula (Tsuboi 1954), where \(M = 1.73\log r + \log A_{0} - 0.83.\) Seismic magnitudes range from about −0.2 to 2. From the reduced displacements and seismic magnitudes obtained, the largest EXs are those of vulcanian eruptions at Sakurajima, followed by Tokachi, Semeru, Lokon and Suwanosejima volcanoes. Reduced displacement and seismic magnitude for the 1–8 Hz Stromboli EXs are much smaller than the others. If the excess pressure before explosion is almost constant, as suggested by Nishimura and Hamaguchi (1993) and Nishimura (1998), which shows a scaling relationship in the amplitude of single force and source duration time, the differences in reduced displacements and seismic magnitudes at these volcanoes may be attributed to vent radius. The differences could be examined in more detail if site amplification factors and attenuation structure, or more detailed waveform analyses using seismic waves, are incorporated in the analyses.
It is well known that the magnitude–frequency distribution of the volcanic explosivity index (VEI, Newhall and Self 1982), which is determined from the volume of ejecta or column height, is expressed by a power law for all volcanoes around the world (Simkin 1993). Recently, Nakada (2015) examined Sakurajima and Izu-Oshima, Japan, and Merapi in Indonesia and indicated that the magnitude–frequency distributions of VEI in the range of 2–6 obey a power law, even for individual volcanoes. Power-law distributions represent self-similar properties in the eruption system and suggest there is no characteristic scale, even in an individual volcano. This is different from the exponential distribution found for EXs and may be attributed to different scaling relations of eruption mechanisms. However, we are not able to discuss the inconsistency in the magnitude–frequency distributions between EXs and VEIs, because the amount of ejecta associated with each EX we analyzed is often too small to evaluate its VEI. Even for large vulcanian eruptions from Minami-dake at Sakurajima, column heights reach about 5000 m and their VEI is equivalent to 2. The EX magnitude–frequency distributions reflect the statistical characteristics of mechanical properties and may not be directly related to the amount of ejecta that determines the VEI. Further investigation on the volume of ejecta associated with vulcanian eruptions, for example, using ash collectors (e.g., Tajima et al. 2013), is necessary.
Finally, we discuss the possibility of airwave contamination of EX seismograms. At Sakurajima, maximum amplitudes are measured in the seismograms before the arrival of airwaves. We see ground-coupled airwaves in the seismograms at Semeru and Suwanosejima, but these signals are generally smaller than the maximum amplitude of ground motion. At Lokon, ground-coupled waves are not well recognized, probably because a hill located between the station and crater obstructs the propagation of airwaves. Hence, we simply measured the maximum amplitudes in the EX seismograms for these three volcanoes. There is no detailed description in Okada et al. (1990) on the amplitude measurements at Tokachi-dake. However, according to Ichihara et al. (2012), the amplitude of ground-coupled airwaves is estimated to be <about 20 % of that of maximum ground motion, based on observation at a nearby station. Hence, the data in Okada et al. (1990) can be reliably used for the examination of EX magnitude–frequency distributions. We analyzed very low-frequency seismic waves (0.05–0.2 Hz) only for Stromboli, as EXs at the other volcanoes are dominated by short-period waves around 1 Hz, and no significant low-frequency waves are recognized. Also, since impulsive airwaves are generated from vulcanian eruptions, low-pass-filtered seismograms may represent ground-coupled airwaves. Hence, we have not analyzed low-frequency bands for the other volcanoes.
Declarations
Authors’ contributions
TN carried out seismic data analyses and drafted the manuscript. MI conducted seismic observation at Sakurajima and Suwanosejima volcanoes and analyzed the Sakurajima data. MH designed seismic observations at Semeru and Lokon volcanoes. HA and TY carried out seismic observations at Lokon and Stromboli volcanoes and analyzed the data. MR and RG conducted volcano observations at Stromboli and analyzed the data. All authors read and approved the final manuscript.
Acknowledgements
We appreciate the careful comments of two anonymous reviewers and the editorial work of Benoit Taisne. This study was partly supported by the Ministry of Education, Culture, Sports, Science and Technology (MEXT) of Japan, under its Observation and Research Program for Prediction of Earthquakes and Volcanic Eruptions, SATREPS project “Multi-disciplinary Hazard Reduction from Earthquakes and Volcanoes in Indonesia” in collaboration with JST, JICA, RISTEK, and LIPI.JST-JICA project, and JSPS bilateral project on Stromboli volcano between Japan and Italy from 2013 to 2015.
Open AccessThis article is distributed under the terms of the Creative Commons Attribution 4.0 International License (http://creativecommons.org/licenses/by/4.0/), which permits unrestricted use, distribution, and reproduction in any medium, provided you give appropriate credit to the original author(s) and the source, provide a link to the Creative Commons license, and indicate if changes were made.
Authors’ Affiliations
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