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Seismo-traveling ionospheric disturbances of ionograms observed during the 2011 Mw 9.0 Tohoku Earthquake
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2011
Received: 7 April 2011
Accepted: 18 May 2011
Published: 27 September 2011
In this paper, sequences of ionograms recorded by 4 ionosondes in Japan and 1 in Taiwan are employed to examine seismo traveling ionospheric disturbances (STIDs) triggered by the 11 March, 2011, M 9.0 Tohoku Earthquake. The circle method, a standard/traditional technique of seismologists for locating an earthquake, is used to find the origin and compute the propagation speed of the triggered STID. Results show that the STID speeds induced by Rayleigh waves, acoustic gravity waves mainly traveling in the ionosphere, and tsunami waves of the Tohoku Earthquake are 2100–3200 m/s (2.1–3.2 km/s), 900 m/s, and 200 m/s (720 km/hr), respectively. The origins derived by the circle method near the epicenter confirm that the observed STIDs were triggered by the seismic waves and tsunami waves of the Tohoku Earthquake.
During earthquake occurrences, vertical motions of the Earth’s surface create mechanical disturbances (acoustic gravity waves; AGWs) in the neutral atmosphere, which propagate into the ionosphere and interact with the ionized gas (hereafter, seismo traveling ionospheric disturbance; STID) (Davies, 1990). An ionosonde is the most traditional instrument for probing the ionosphere, which has been routinely (every 15 minutes) recording ionograms to monitor the vertical distribution of the electron density from 90 km altitude to the ionospheric F2 peak (about 250–350 km altitude) since the early 1930s (Hansucker, 1991). Leonard and Barnes (1965) first observed ionospheric disturbances induced by the 27 March, 1964, M 9.2 Alaskan earthquake using data at four sites of ionosondes in Alaska and California. Although fluctuated traces in the ionograms of the ionosondes were observed after the Alaskan earthquake, the origin and the propagation of the STIDs were not studied in detail.
The method of intersecting circles (hereafter, the circle method) might be the first used for locating the hypocen-ter (source, or epicenter) of an earthquake (Lay and Wallace, 1995). Seismologists calculate the possible circular distance (zone) to the source of seismic waves from each station, which is equal to the product of the propagation speed and the traveling time. When circular zones of three or more stations intersect at the same location, we then consider the source as being located. The short-coming of this method is that the onset time of the earthquake and the propagation speed of the seismic waves should be approximately known and/or estimated in advanced.
2. Observation and Results
Locations, distances to the epicenter and traveling times of the ionosonde. The distance is computed by the spherical coordinate with the Earth’s radius of 6371 km.
WAK (45.2°N, 141.8°E)
KOK (35.7°N, 139.5°E)
YAM (31.2°N, 130.6°E)
OKI (26.7°N, 128.2°E)
CHL (25.0°N, 121.2°E)
Following the 1st and 2nd STID signatures, remarkably sinusoidal/wavy uplift STIDs appeared at WAK at 0730 UT, YAM at 08:00 UT, OKI at 08:30 UT and CHL at 0905 UT. Note that no clear feature can be found at KOK. Again, applying the circle method with horizontal speeds in the range 100–300 m/s with a step of 50 m/s, we find that for a horizontal speed of 200 m/s (or 720 km/hr), 4 circular zones intersect at one location, which is near the tsunami origin and/or the Tohoku epicenter.
3. Discussion and Conclusions
Many studies report STIDs triggered by the 11 March, 2011, M 9.0 Tohoku Earthquake by means of TEC (total electron content) derived from ground-based GPS receivers of GEONET (Maruyama et al., 2011; Rolland et al., 2011; Tsai et al., 2011) and ionograms of ionosondes (Maruyama et al., 2011). Three different STIDs are observed by the 5 ionosondes after the earthquake. The 1st STIDs with rather small disturbed amplitudes but very high propagation speeds of 2100–3200 m/s (2.1–3.2 km/s) which is in agreement with 3 km/s by Rolland et al. (2011) and 2.3 km/s by Tsai et al. (2011). The high speed waves might be induced by vertical motions of the solid Earth’s surface of Rayleigh waves of the earthquake. Due to the high speed of 2–4 km/s and relatively short duration of several seconds/minutes, it requires some coincidence for ionosondes to observe STIDs triggered by the Rayleigh waves.
However, large vertical motions around the epicenter can generate acoustic (pressure) waves and gravity (buoyancy) waves (i.e. AGWs) in the neutral atmosphere, which can further propagate into the ionosphere and interact with the ionized gas. The highly-fluctuated features indicate these waves with various amplitudes, frequencies, and speeds confoundedly/concurrently reaching the ionosphere. The AGW speed is a function of the ratio of specific heat, temperature, molecular weight, wind speed, etc. For those traveling below the mesopause of 90 km altitude, the average AGW speeds are about 300–400 m/s (Liu et al., 2006), while for those departing with relatively high elevation angles and mainly traveling in the ionosphere (or thermo-sphere) above 100 km altitude, the associated average AGW speeds could be up to 700–1100 m/s (cf. Artru et al., 2004; Heki and Ping, 2005; Liu et al., 2010). Therefore, the speed of 900 m/s suggests the 2nd STID being related to AGWs mainly traveling in the ionosphere of about 200 km altitude, which is close to the value of 1032–1045 m/s given by Liu et al. (2011) and the 1 km/s (1000 m/s) given by Rolland et al. (2011).
On the other hand, the sinusoidal traces in the ionograms of WAK, YAM, OKI, and CHL suggest that the triggering source has a relatively long period. A study of the 5-min time resolution ionograms shows that the period of the 3rd STID is in the range 15–20 minutes and the associated speed is 200 m/s (or 720 km/hr) which is close to 225 m/s by Rolland et al. (2011) and 210 m/s by Tsai et al. (2011). The agreements suggest that the 3rd STID is induced locally by the tsunami wave right under it.
For simplicity, we assume that the STIDs take 4 minutes traveling vertically from the Earth’s surface to the ionosphere of 200 km altitude and examine the horizontal propagations of the origins of the STIDs accordingly. It is essential to find whether this assumption is reasonable and appropriate. Liu et al. (2011) report that STIDs of the GPS TEC first appear near the epicenter about 7 minutes after the Tohoku Earthquake onset, while Tsai et al. (2011) find that the STIDs in the GPS TEC triggered by the Rayleigh waves appear 7–8 minutes after the earthquake occurrence. Maruyama et al. (2011) further cross-compare concurrent/co-located GPS TECs and ionograms recorded by the 4 ionosondes in Japan during the Tohoku Earthquake. They find the earlier onset of the disturbance in the iono-gram than the commencement of the propagating TEC perturbation. Since fluctuations in TEC are sensitive to the disturbance near the F2 peak (about 350 km altitude), while the observed ionosonde STIDs are at the reflection height of about 200 km altitude, the 4-minute time lag should be reasonable for the STIDs directly and/or locally triggered by Rayleigh and tsunami waves under them (i.e. the 1st and 3rd STIDs). However, it might take longer than 4 minutes for the internal AGWs, such as the 2nd STID. Nevertheless, due to the ionosonde sampling rate of every 15 minutes, the 4-minute assumption, or even slightly longer, is reasonable and appropriate.
In conclusion, the STIDs induced by the Rayleigh waves, ionospheric AGWs, and tsunami waves have been observed by ionograms recorded by the 5 ionosondes near the earthquake. The circle method can be used to locate origins and enable the determination of the propagation speed of STIDs triggered by seismic waves and tsunami waves of large earthquakes.
Ionsonde ionograms were retrieved from the National Institute of Information and Communications Technology (NICT) in Japan, http://wdc.nict.go.jp/IONO/HP2009/ISDJ/index-E.html, and the National Communications commission (NCC) in Taiwan http://iono.ncc.tw/Ionosphere/Introcht.aspx. This research was partially supported by the National Science Council Grant, NSC 98-2116-M-008-006-MY3 and NSC 98-2111-M-008-008-MY3 to National Central University.
- Artru, J., T. Farges, and P. Lognonné, Acoustic waves generated from seismic surface waves: Propagation properties determined from Doppler sounding observations and normal-mode modeling, Geophys. J. Int.,158, 1067–1077, 2004.View ArticleGoogle Scholar
- Davies, K., Ionospheric Radio, 580 pp, Peter Peregrinus Ltd., London, U.K., 1990.View ArticleGoogle Scholar
- Hansucker, R. D., Radio Techniques for Probing the Terrestrial Ionosphere, 293 pp, Springer-Verlag, Berlin Heidelberg, 1991.View ArticleGoogle Scholar
- Heki, K. and J. Ping, Directivity and apparent velocity of the cosemic ionospheric disturbances observed with a dense GPS array, Earth Planet. Sci. Lett.,236, 845–855, 2005.View ArticleGoogle Scholar
- Lay, T. and T. C. Wallace, Modern Global Seismology, 512 pp, Academic Press, New York, 1995.Google Scholar
- Leonard, R. S. and R. A. Barnes, Observations of ionospheric disturbances following the Alaska earthquake, J. Geophys. Res.,70, 1250–1253, 1965.View ArticleGoogle Scholar
- Liu, J. Y., Y. B. Tsai, S. W. Chen, C. P. Lee, Y. C. Chen, H. Y. Yen, W. Y. Chang, and C. Liu, Giant ionospheric disturbances excited by the M9.3 Sumatra earthquake of 26 December 2004, Geophys. Res. Lett.,33, L02103, doi:10.1029/2005GL023963, 2006.Google Scholar
- Liu, J. Y, H. F. Tsai, C. H. Lin, M. Kamogawa, Y I. Chen, C. H. Lin, B. S. Huang, S. B. Yu, and Y H. Yeh, Coseismic ionospheric disturbances triggered by the Chi-Chi earthquake, J. Geophys. Res.,115, A08303, doi: 10.1029/2009JA014943, 2010.Google Scholar
- Liu, J. Y, C. H. Chen, C. H. Lin, H. F. Tsai, C. H. Chen, and M. Kamogawa, Ionospheric disturbances triggered by the 11 March 2011 M9.0 Tohoku Earthquake, J. Geophys. Res.,116, A06319, doi:10.1029/2011JA016761, 2011.Google Scholar
- Maruyama, T., T. Tsugawa, H. Kato, A. Saito, Y. Otsuka, and M. Nishioka, Ionospheric multiple stratifications and irregularities induced by the 2011 off the Pacific coast of Tohoku Earthquake, Earth Planets Space,63, this issue, 869–873, 2011.View ArticleGoogle Scholar
- Rolland, L. M., P. Lognonné, E. Astafyeva, E. A. Kherani, N. Kobayashi, M. Mann, and H. Munekane, The resonant response of the ionosphere imaged after the 2011 off the Pacific coast of Tohoku Earthquake, Earth Planets Space,63, this issue, 853–857, 2011.View ArticleGoogle Scholar
- Smith, A., Focal mechanism of the 2011 off the Pacific coast of Tohoku Earthquake, Earth Planets Space, 2011 (submitted).Google Scholar
- Titheridge, J. E., Ionogram analysis with the generalized program POLAN, World Data Center A for Solar-Terrestrial Physics Report UAG-93, 1985.Google Scholar
- Tsai, H.-F., J.-Y. Liu, C.-H. Lin, and C.-H. Chen, Tracking the epicenter and the tsunami origin with GPS ionosphere observation, Earth Planets Space,63, this issue, 859–862, 2011.View ArticleGoogle Scholar