Electromagnetic Emissions Recorded by a Borehole TOA Installment before Four Huge Destructive MS ≥ 8.0 Earthquakes in Asia

In this paper, electromagnetic emissions recorded by a borehole TOA installment with three observing channels of CH1 (0.01 0.1 Hz), CH2 (0.1 1.0 Hz) and CH3 (1 9 kHz) before four large earthquakes with magnitudes more than 8.0 have been depicted. These abnormities present different fluctuating processes from one another. For the Wenchuan MS 8.0 earthquake on 12 May 2008, the nearest one among these four events and only 660 km from the TOA station, electromagnetic information appeared at least 5 months ago in two low frequency bands of CH1 and CH2 and it was subjected to an obvious fluctuating process with several developing stages: initial information, intensive anomaly and large amplitude signals. The typical pulse-like emissions in CH2 happened group by group with large various magnitudes, which can be of 10 mV in the climax period. While during this period, compatible wave-like information with little magnitudes also happened in CH1 channel and a few pulses in CH3. Anomalous emissions occurred about 4 months prior to the 25 April 2015 Nepal MS 8.1 event, 1560 km away from the TOA station. The abnormal information in CH2 also appeared group by group but with small various magnitudes, more than 2 mV during their climax. This process is also effective for the Sumatra MS 8.9 earthquake on 26 December 2004, 2500 km from the borehole TOA, only with a different duration of 2 months and less magnitudes of 0.1 mV in CH1 and 1 mV in CH2 in this case. However, there is no obvious fluctuation and only small constant amplitude signals being ~0.15 mV appeared during 2 weeks before the Japan MS 9.0 earthquake on 11 March 2011. It is the farthest one among these four events and beyond 4000 km from the observing station. So, we can make a conclusion that there is a near relationship between the properties of the abnormiHow to cite this paper: Li, M., Yu, C., Zhang, Y., Zhao, H.X., Zhang, X.H., Li, W.X., Zhang, P. and Zhang, L. (2020) Electromagnetic Emissions Recorded by a Borehole TOA Installment before Four Huge Destructive MS ≥ 8.0 Earthquakes in Asia. Open Journal of Earthquake Research, 9, 50-68. https://doi.org/10.4236/ojer.2020.92004 Received: November 24, 2019 Accepted: March 7, 2020 Published: March 10, 2020 Copyright © 2020 by author(s) and Scientific Research Publishing Inc. This work is licensed under the Creative Commons Attribution International License (CC BY 4.0). http://creativecommons.org/licenses/by/4.0/


Introduction
At present, short-term earthquake (EQ) prediction is still one of the most challenging targets worldwide [1]. Electromagnetic observation is one effective way to pursue precursors associated with seismic activities during the last several decades. Ground-based electromagnetic observation is broadly utilized and effective precursory data have been attained before many strong seismic events.
The ULF band is of particular interest because only EM signals in the ULF range and at lower frequencies can be effectively recorded at the Earth's surface without significant attenuation compared with "high" frequency band because most of the epicenter depths are at more than 10 km, even several hundreds of kilometers beneath the Earth's surface. Unusual ULF (0.01 -10 Hz) magnetic signals were observed about two weeks before the Loma Prieta M S 7.1 EQ on 17 October 1989 [2] [3]; Anomalous electromagnetic emissions were also observed about one month and a few days before the 8 August 1993 M S 8.0 Guam EQ (f = 0.02 -0.05 Hz) [4] [5] and before the great M S 8.2 Biak EQ in Indonesia, on February 17, 1996 (f = 0.005 -0.03 Hz) [6]. Li et al. [7] have reported that obvious ULF (f = 0.1 -10 Hz) electromagnetic abnormity had been observed for several months prior to the large Wenchuan M S 8.0 EQ on May 12, 2008 at Gaobeidian station, 1400 km away from the Wenchuan epicenter.
As the development of ionosphere-Earth integration observation, satellite-Earth observation has gradually displayed its application potential in fields of earthquake local mechanism investigation, earthquake monitoring and prediction, and defensive and rescue of seismic disasters because of its advantages on fast speed, large scale and high resolution, especially for areas with harsh natural conditions. Electromagnetic emissions associated with seismic activities have also been recorded by satellite-borne receivers [8]- [14]. The concept of lithosphere-atmosphere-ionosphere (LAI) coupling among the three involved layers of the Earth system has been proposed due to the transfer of energy among these three layers during some last stages of the long-term process of preparation. At present, the coupling mechanism and coupling model in these three layers have been gained more and more attention [15]- [22].
Furthermore, as a segment of ionosphere-Earth stereoscopic observation system, the sub-surface measurements of electric and magnetic field emissions at frequencies between ULF and VLF (very low frequency) have also played an important role during some strong seismic activities due to its freedom of part disturbances outside of the Earth. VLF electromagnetic signals have been respectively recorded by borehole antennas before the M S 5.8 east Yamanashi Prefecture EQ [23] and the Chamoli M S 6.6 EQ on 29 March 1999 in India [24].
In this paper, a borehole electromagnetic observing installment named TOA is firstly introduced in Section 1. Then, in Section 2, the fluctuating processes of electrical emissions related to four huge EQs in Asia will be depicted in detail.
Discussion and conclusions are in Section 3 and Section 4, respectively.

Experimental System
Benefitted from a cooperation with Japan Meteorology Agency (JMA), TOA electromagnetic measurement was put into service in November 1992 in Dali city in China. The observing system includes a sensor, a channel filter, a channel attenuator and a recorder. The sensor is comprised of a copper circle with 15 m radius, which is buried 1 m sub-surface, and an 800 m perpendicular borehole antenna in the casing pipes in an observing well (No. dian21), with a location of the geographical coordinates (100.2˚E, 25.7˚N). The depth of the observing well is 800.5 m and casing pipes with different diameters reach to 800 m underground ( Figure 1(a)).
The system measures a potential difference between the borehole antenna and the copper circle and includes three observing channels: two ULF bands CH1 (0.01 -0.1 Hz) and CH2 (0.1 -1.0 Hz) and one VLF band CH3 (1 -9 kHz). But the system is with a narrow channel bandwidth: 0.05 Hz, 0.5 Hz and 5 kHz for CH1, CH2 and CH3 when calibrated or there will be no output.
The measured potential difference is outputted by a drum recorder (see mV. What we need to notice is that there are different magnification coefficients for three channels CH1, CH2 and CH3 when a signal is output by the recorder; that is, it is 1 mV, 10 mV and 50 mV respectively for CH1 (0.01 -0.1 Hz), CH2 (0.1 -1 Hz) and CH3 (1 -9 kHz) if the amplitude of a signal is full of all lattices of the recording paper (100 lattices in total). For example, Figure 1(c) shows a signal recorded by CH2 (0.1 -1 Hz), which is labeled by a black arrow. This signal covers about 5 lattices in the recording paper and its amplitude is ~0.5 mV.
In fact, the system is still not free of all effects outside and it is affected mainly Open Journal of Earthquake Research by thunder and lighting, strong magnetic storm when Kp > 7, AC/DC (AC, alternating current; DC, direct current) conversion, radio communication in measurement area and automobile engine. While the signals caused by these factors are short-period and single-shape transient pulses or discrete pulses. These emissions are of significant difference from relative long time, continuous and various-shape signals with big amplitudes during seismic activities [25]. More details about signal properties of disturbances outside the TOA measurement can be found in [26].
At the same time, Li et al. [25] have made an important statistical work on this TOA electromagnetic observation and summarized variation characters of electromagnetic emissions associated with 29 M S ≥ 5.0 EQs recorded in the ensuing decade after the installment coming into service. More details can also be found in [26]. Open Journal of Earthquake Research

Electromagnetic Emissions Recorded by the Borehole TOA during Large EQs
Almost Fortunately, these EQs had also been recorded effectively by the TOA and electrical emissions recorded prior to or during these events will be described in the following parts.

Sumatra MS 8.9 EQ on 26 December 2004
A huge EQ with a magnitude M S 8.9 occurred at 00:58:53 universal time (UT) on 26 December 2004 in Sumatra-Andaman Islands, with a location of the geographical coordinates (3.31˚N, 95.95˚E) (see Figure 2) and a depth of 30 km. It has been the fourth largest EQ in the world since 1900 and it is the largest since the 1964 Prince William Sound, Alaska EQ [27]. The electromagnetic emissions started at the beginning of November 2004 mainly in two low frequency CH1 (0.01 -0.1 Hz) and CH2 (0.1 -1.0 Hz) recording channels. The signals in CH1 are like waves with small amplitude pulses. Comparatively, signals in CH2 are continuous pulses with relative large magnitudes. Figure 3(a) shows part of real-time analog recordings on November 8 2004 and the magnitude of the signals is more than 2 mV sometimes (see Figure  3(a)). This condition was going on in the following days but with a little difference. The anomalous signals did not appear continuously but group by group  There seems to be a long run for the TOA station that recorded electromagnetic signals but the total developing process of these abnormalities can be divided into three stages. At the first stage, weak information started in October 2007. But the emissions became obvious in January 2008, more than five months prior to the Wenchuan EQ on May 12 2008. Figure 4  pulses and various amplitudes. The amplitudes of some signals can be up to full lattices (~10 mV) of the recording paper occasionally. While there were also discrete signals happening in CH1 and CH3 channels during this period and their magnitudes were relatively small (see Figure 4(a)). However, during the second stage, the condition seems to change with a big difference when it came into the mid of March 2008. The emissions intensively appeared group by group in two low frequency channels CH1 and CH2 but with smaller magnitudes than before and each group of emissions last more than 3 hours. This phenomenon rarely happened in this TOA borehole observing history. Figure 4 Then, the abnormities appeared less than ever till the Wenchuan M S 8.0 EQ took place on 12 May, when coseismic responses occurred at the same time both in CH1 and CH2 channels and decayed quickly (see Figure 4(d)). The distance between the Wenchuan epicenter and the TOA station is 660 km, the nearest one among these four events described in this paper.

Japan M 9.0 EQ on 11 March 2011
A disastrous EQ occurred in Japan on 11 March 2011, with an epicenter located at 142.6˚E and 38.1˚N and a depth of 32 km. This M S 9.0 Tohoku-Oki EQ is officially referred to as the off the Pacific coast of Tohoku EQ by the JMA (Figure  2), which is the largest EQ in Japan since the start of instrumental observation in the late 19th century and the fifth one following the last Sumatra M S 8.9 EQ on 26 December 2004.
The anomalous information recorded this time at TOA station began from 26 February 2011, and it is characterized by discrete signals appeared group by group and with equal magnitudes in two low frequency bands of CH1 and CH2.  Figure 5(d)). One point must be noted is that this EQ is beyond 4000 km away from the observing TOA station in Dali, Yunnan province, China.

Nepal MS 8.1 EQ on 25 April 2015
The Nepal M S 8.1 EQ occurred on 25 April 2015 lies in the juncture of Nepal and Open Journal of Earthquake Research China and with a location of the geographical coordinates (28.1˚N, 84.7˚E) and a depth of 15 km (see Figure 2).
The electromagnetic variations started from the beginning of January 2015 and lasted more than four months till the occurrence of the Nipal event. During this period, it shows typical signal properties in each recording channel CH1, CH2 or CH3. Emissions in CH1 are wave-like with weak equal amplitude signals; emissions in CH2 were of group continous pules with various amplitudes, which tended to increase but generally less than 2 mV during last stage of the total process; relative long period wave appearred occasionally in CH3. Like the other three events illustrated above, coseismic responses had also been recorded in CH1 and CH2 but CH3 when the Nepal M S 8.1 EQ occurred on 25 April 2015,

Discussion
In this paper, electromagnetic emissions recorded by TOA before four large EQs with magnitudes more than 8.0 have been presented. These abnormities present different fluctuating process from one another. While, one interesting point here is that the epicentral distances from 660 km to 4000 km for these four events are larger than usual, which are defined that the borehole TOA electromagnetic system can effectively record M S > 5.0 EQs within 200 km, M S > 6.0 events within 300 km, and M S > 7.0 events within 500 km [25]. However, Li et al. [7] have reported that ULF (0.1 -10 Hz) electromagnetic emissions was recorded at 1400 km Gaobeidian station in north China before the Wenchuan EQ. Ohta et al. [27] have also reported that the seismogenic ULF emissions propagated from the Sumatra M 8.9 EQ epicentre over about 5500 km.
The radius of seismic area where changes can be expected can be estimated using the Dobrovolsky formula R = 10 0.43M , where R is the radius of the EQ preparation zone, and M is the EQ magnitude [28]. It gives that the radius for the M S 8.0 event preparation zone is more than 2700 km and 7400 km for the M S 9.0 event. In order to estimate the magnetic field intensity expected on the ground, different mechanisms were proposed. When the seismogenic emissions are generated in the Earth's crust, electromagnetic emissions will be effectively recorded in the near distance used the empirical law by Hayakawa and Hattori [29]. However, the seismogenic ULF emissions might be generated near the Earth's surface or in the atmosphere when the depth of an EQ is very small (i.e., 10 km). In this case, they seem to be able to propagate in the Earth-ionosphere waveguide over great distances as the quasi-TEM mode of propagation [30]. At the same time, in order to interpret a 1.3 mV·m −1 electrical field recorded at 1400 km Gaobeidian station, Li et al. [31] have attained that the same value of 1.3 mV·m −1 can be recorded at a 5800 km propagating distance in the Earth-ionosphere waveguide when the ionospheric influence is considered. However, a borehole antenna can still display its advantageous potential during EQ monitoring. On together with seismic waves. These results were consistent with those of Karake-lian et al. [33], who observed that coseismic ULF signals exist on all components of the magnetic and electric fields and begin with the arrival of seismic waves.
Mogi et al. [34] found coseismic changes in the electric field and inferred that these changes began at the arrival time of a seismic wave by examining the relationship between variations in the electric field and EQs in Sumatra, Indonesia.
Similar results has also been attained by Nagao et al. [35], which concluded that electric field changes started at the arrival times of seismic waves, rather than the original times of EQs, and claimed that the generation mechanism of changes was related to the electrokinetic effect. On the other hand, Iyemori et al. [36] reported a possible mechanism associated with coseismic geomagnetic variations of an induction effect due to crustal dynamo mechanism. However, Matsushima et al. [37] considered that such an electromagnetic variation should propagate faster than the seismic wave itself. They also proposed seismo-dynamo effect of electromagnetic induction in the electrically conducting Earth caused by ground motion in the Earth's magnetic field [38]. However, it is not easy to distinguish the initial time of the coseismic response for each event because of different adjustments of three recording pens in different period and TOA instrument aging. However, we still consider that these coseismic signals arrived together with seismic waves based on the description by Li et al. [25].

Conclusions
In this paper, a borehole TOA electromagnetic experiment system from Japan has been introduced firstly. The system includes three observing channels: two ULF bands CH1 (0.01 -0.1 Hz) and CH2 (0.1 -1.0 Hz) and one VLF band CH3 For the Wenchuan M S 8.0 EQ on 12 May 2008, 660 km from the TOA station, electromagnetic information appeared more than 5 months ago in two low frequency bands of CH1 and CH2 channels and it displayed an obvious fluctuating process with several developing stages: initial information, intensive anomaly and large amplitude signals. The typical pulse-like emissions in CH2 appeared group by group with a maximum magnitude of 10 mV and compatible wave-like information with equal little magnitudes also happened in CH1 channel.
Anomalous emissions occurred about 4 months prior to the Nepal M S 8.1 event, 1560 km away from the TOA station. The abnormal emissions in CH2 appeared in groups but with small various magnitudes, more than 2 mV during their climax, and equal little magnitude appeared in CH1 during this period.
However, there is no obvious fluctuation and only small constant amplitude signals being ~0.15 mV in CH2 appeared during 2 weeks before the Japan M S 9.0 EQ on 11 March 2011, which is beyond 4000 km from the borehole station.
Though the abnormities of these four events present different fluctuating processes from one another, on one hand, almost electromagnetic emissions were collected in two low frequency bands of CH2 and CH1 channels instead of VLF band of CH3 channel. At the same time, it seems that CH2 band is more sensitive to the seismic events at TOA station. On the other hand, for all these large EQs, both CH1 and CH2 bands had recorded obvious coseismic responses, which are thought to be induced by the arrival of seismic waves.
However, if these four huge EQs are considered in the light of their epicentral distances, we can conclude that there is a near relationship between the properties of the abnormities, such as amplitudes, duration and signal types, and the distances from TOA station: on one hand, the amplitude and duration decreases as the distance increases; on the other hand, there is an evolution for emission properties from complex various magnitude signals to single equal magnitude ones as the distance changes to be far.