JP3404229B2 - Apparatus and method for generating alarm just before earthquake disaster prevention - Google Patents

Description

Detailed Description of the Invention

[0001]

BACKGROUND OF THE INVENTION The present invention is, space electromagnetic field sensor
The precursors of Seismic accurately observed as an electric signal, on Earthquake Disaster immediately before alarm generation apparatus and method capable of trigger an earthquake just before alarm before the occurrence of the main shock using.

[0002]

2. Description of the Related Art The conventional method of observing earthquakes is mainly "observation of crustal movements " such as seismographs and volumetric strain gauges. Basically, warnings and warnings are issued just before the main shock. It was not an observation system that could do. In addition, when estimating the seismic intensity of the epicenter, the main system is a system that transmits the data from multiple observation points to the arithmetic and control unit by communication means and performs arithmetic processing, which is due to the occurrence of a huge earthquake. It was not a system that could estimate the seismic intensity of the epicenter when communication was lost.

This basic defect was revealed by the Hyogo-ken Nanbu Earthquake (Great Hanshin Earthquake) that occurred on January 17, 1995, and due to rescue in some areas, delay in disaster prevention activities, etc., many precious human lives,
It was lost. As is well known, earthquake research institutes such as universities were established in Kansai from early on, and are still actively engaged in research activities. However, even these public research institutes, which are in an environment that is financially and financially endowed, are not able to obtain M7.
The failure to predict a 0-class giant earthquake indicates that the conventional seismic observation method is not a very effective method for catching the precursor of an earthquake. That is, the acceleration recording waveform and the displacement recording waveform such as earthquake motion are recorded as phenomena and become "past data" at the time when they are recorded in the seismograph. In general, in order to understand the seismograph records as a precursory phenomenon before the main shock, it is indispensable to accurately measure the amount of crustal movement and the stress accumulated inside the crust. , Is currently underway in Tokai area. However, a big earthquake cycle
It was difficult to get an accurate grasp because it lasted at least 100 years.

[0004] In addition, no matter how, even if can accurately grasp the crust inside of stress, in the evaluation method of "material mechanical" such as distortion and deformation, it is not possible to accurately determine the occurrence time of the main shock. This is because the rocks that make up the crust are made of brittle materials, and the fracture and reliability of the materials are evaluated mainly by statistical methods.
For example, when a strength test is performed on a metal, which is a representative of artificial materials, the breaking strength often appears with variations around a certain fixed value. When the strength is to be calculated from these test data, the strength is calculated by adding statistical processing to the test data.

Among the artificial materials, even the metal, which is the most uniform material, has a varying breaking strength,
It is not difficult to imagine that the fracture strength of natural rocks varies widely even at the laboratory level. Therefore, it can be considered that it is impossible to satisfy the prediction principle only with the seismic observation methods that have been used to date. This is because the seismic observation method itself has a large reason that it is performed by a material mechanics method such as “strain”, “deformation”, and “fracture surface generation”.

Then, how can we predict the occurrence of an earthquake? In general, many natural phenomena have statistical properties. The point is that the handling of the observed phenomenon depends on how much the observed phenomenon depends on the statistics. In other words, the fact that no matter what physical phenomenon is observed cannot be predicted, it is a common problem when dealing with natural phenomena. However, on the contrary, when a precursory phenomenon appears in such a natural phenomenon with a high probability with respect to the occurrence of the observed object, by performing the observation of the precursory phenomenon in parallel, the time when the observed object occurs can be considerably increased. It can be predicted with good accuracy.

If this is limited to earthquake prediction, it means that it is possible to observe the precursory phenomenon that precedes the main shock and accurately predict the time of occurrence of the main shock. It goes without saying that, as a matter of course, the method that does not rely on the material mechanics method as described above is the main principle for observing the precursory phenomenon. Therefore, as a result of investigating various methods related to earthquake prediction, it was found that precursory observation was performed by measuring earth current, geomagnetism, and electric field. In addition, some of these methods have been reported by Mr. Oike and Mr. Fujinawa of Kyoto University who observed the precursor of the Hyogo-ken Nanbu Earthquake that occurred on January 17, 1995 with electromagnetic waves, and observed electrical phenomena. Is considered to be one of the effective methods (for details, see the Institute of Electrical Engineers, September 1995 issue, Vol. 115).

[0008] In addition, according to various reports after the occurrence of the previous Hyogoken Nanbu Earthquake, many people have witnessed that white light emission occurred for several minutes immediately before the earthquake. This white luminescence was a very weak light that shimmered, just like a fluorescent lamp that was about to break, and the main shock occurred after this luminescence. Immediately before the earthquake (a few seconds before), a brighter orange emission was observed in the Rokko area. In addition, no such luminescence was seen during the shaking of the main shock. What is worrisome here is that, as often seen in the electromagnetic precursory phenomenon, a sign appears in the form of a light emission phenomenon or anomalous ground current immediately before the occurrence of the main shock, but the main shock occurs. At times, these phenomena are not seen.

Regarding this point, Mr. Enomoto of the Institute of Industrial Science,
The following theory is stated in the above journal of the Institute of Electrical Engineers of Japan. According to Enomoto's theory, when stress accumulates in the rock and fracture begins, the electrons (exoelectrons) that jump out from the lattice defects on the fracture surface are
Charge the gas and water vapor contained in the bedrock. Eventually, in the state just before the earthquake when the cracks on the top, bottom, left, and right of the rock begin to meet, a sudden gas flow is induced and discharge occurs. This discharge is observed as an electromagnetic change immediately before the earthquake, and this theory is in good agreement with the fact that no electromagnetic phenomenon is observed during the main shock. That is, at the time of the main shock, the cracks inside the bedrock have already completely met, the discharge path is extended, and the discharge ends. In this way, the high voltage generated by the discharge ionized gas on the surface of the earth and in the atmosphere to emit light immediately before the earthquake, and many people witnessed this.

[0010]

However, most of the conventional earthquake prediction methods based on the observation of the earth current described above have not been put into practical use. The main reason is that the earth current itself is susceptible to external noise such as lightning and artificial electromagnetic fields. In addition, all measurement systems used for measurement are composed of electronic circuit systems such as antennas and amplifiers, and in many cases, these can be observed in relation to impedance and circuit resonance frequency. Another reason is that the frequency band and the amplification factor have a finite relationship, so that it may not be possible to measure an electrical signal as a key precursory phenomenon.

According to the lessons learned from the Great Hanshin Earthquake, the gravity pendulum (1 m in length) at the inventor's home was excited about 2 days before the occurrence of the earthquake, and the vibration did not stop.
I have been vibrating for nearly 10 hours in a long time. The main shock is
The vibration of the gravity pendulum occurred the day after it stopped. In addition, prior to that, pulse-like noise began to enter the photomultiplier tube (R928 made by Hamamatsu Photonics) of the spectroscope used by the inventor, and around November 1994, the photoelectron noise was so great that photon counting could not be performed. Although the number increased sharply, pulse noise was hardly observed around February 1995 after the earthquake. The present invention considers these phenomena that occurred before the Great Hanshin Earthquake as precursory phenomena,
We also consider and propose an observation method with high measurement accuracy. An object of the present invention is to provide a space electromagnetic field sensor for observing an electromagnetic field using an electron tube or the like capable of generating electrons, paying attention to the property that electrons are easily bent by a magnetic field or an electric field. Without being affected by the impedance and resonance of the electronic circuit using this sensor,
It is possible to effectively observe the precursory phenomenon that precedes the above-mentioned earthquake, determine that it is an earthquake precursory phenomenon from the peculiarity of the electrical signal, and issue a warning immediately before the earthquake (a warning immediately before and not a prediction) with relatively high accuracy. An object of the present invention is to provide a device for generating an alarm immediately before an earthquake disaster that can be generated and a method thereof. Moreover, it is to introduce an analysis method that can obtain the estimated seismic intensity of the epicenter, which was conventionally obtained from data of three or more points, from the seismic waveform data of only one point.

[0012]

In order to achieve the above-mentioned object, the present invention aims to generate electricity by changing the trajectory of electrons flying in space.
Spatial electromagnetic field generated by an electron tube that detects the generation of a magnetic field
The sensor and the space electromagnetic field sensor
It is used by exposing it to an electromagnetic field including a magnetic field.
Seismic observation and electrical characteristics detection means for measuring signals from sensors
Seismic measurement means using seismometers and
Electromagnetic generated just before the earthquake by using the signal from the output means
For observing electromagnetic precursory phenomena
And the seismic measuring means and the electromagnetic precursory phenomenon observer
After the observation of the electromagnetic precursory phenomenon,
Even if a certain time or more has elapsed, seismic waves will be
Noise discriminating means for discriminating noise when no noise is observed
And within a predetermined time after the observation of the electromagnetic precursory phenomenon
When the seismic wave was observed by the seismic measurement means,
The vibration duration of the seismic waveform is increased, and
When the signal strength of the electromagnetic precursory phenomenon increases, the signal
Earthquake when signal intensity peaked and then decreased slightly
Pre-earthquake alarms that generate last-minute alarms
Analyze the earthquake waveform observed by the measuring means
Source distance from at least one observation data at the time of life
Calculate the epicenter distance according to the formula and calculate the magnitude.
Seismic wave
According to the distance attenuation formula, which shows the property that
A hypocenter analyzer that estimates the seismic intensity of the epicenter and the depth of the epicenter
An alarm just before an earthquake disaster that features a step
It is a device. In the above, an earth ammeter that measures earth current
Further, the electrical characteristic detection means, the artificial electromagnetic field or
The spatial electromagnetic field exposed to an electromagnetic field including a spatial electromagnetic field.
While measuring the signal from the sensor,
The ground noise is measured and the noise discrimination means
The change of the earth current by the ammeter changes the output of the space electromagnetic field sensor.
If it is not correlated with
Alternatively, it may be determined to be noise. Also, above
In the above, the space electromagnetic field sensor is a photomultiplier tube.
Electron beam generator with built-in electron tube or electron gun
It may be. In addition, the present invention reduces the fluctuation of the electromagnetic field in space.
Spatial electromagnetics detected as electrical signals using flying electrons
Pulse or voltage average of the signal from the field sensor
The absolute value of the amount of change such as a value increases, and the amount of change decreases.
Electrical characteristic detection step of detecting the electrical characteristics until
A seismometer that measures seismic waves by performing seismic observations with seismometers
Detection by the measuring step and the electrical characteristic detecting step
This electrical characteristic is regarded as an electromagnetic precursory phenomenon, and
Within a predetermined time from the detection of atmospheric characteristics, the earthquake measurement step
When an earthquake is not measured in
If an elephant is identified as noise and an earthquake is measured within a predetermined time,
Noise discrimination step to be regarded as electromagnetic precursory phenomenon
According to the noise discrimination step, the electromagnetic precursory phenomenon
The electrical characteristics and the earthquake measurement step determined as
Treat the measured earthquake as an observation unit, and repeat it multiple times
And the step of observing the electromagnetic precursory phenomenon,
Observed at the electromagnetic precursory observation step
The signal strength of the electromagnetic precursory phenomenon or the number of observed pulses
And the number of observations increases, and the earthquake measurement step
Duration of seismic waves measured in
When an earthquake is observed, there are few electromagnetic precursory phenomena.
Both the signal strength is reduced from the peak point based on the signal strength.
An earthquake that outputs a previous warning by defining the point just after it as the previous warning point
An immediately preceding alarm generation step,
This is a method of issuing an alarm immediately before earthquake disaster prevention. Also, in the above,
In the alarm generation step immediately before the earthquake, the average
A value that is more than twice the observed level is set as a warning and
If the increase amount decreases in multiple observations, it is set as an alarm and
Note: When the number of alarms decreases below the set point after multiple observations, immediately
It may be set as a pre-warning.

[0013]

BEST MODE FOR CARRYING OUT THE INVENTION An embodiment of an immediately-before-earthquake warning device to which an immediately-before-earthquake-disaster-prevention warning generation method of the present invention is applied will be described below. FIG. 1 is a block diagram of an immediately before-earthquake warning device according to the first embodiment, and FIG. 2 is a block diagram of an immediately-before-earthquake warning device according to a more full-scale second embodiment. First, the first embodiment shown in FIG. 1 will be described. This apparatus uses an electron beam generation detection means (spatial electromagnetic field sensor) which detects a deviation of an electron trajectory of an electron beam flying in a vacuum and detects the generation of an electromagnetic field while being exposed to the electromagnetic field. As this electron beam generation detection means, an electron tube 1 made of a photomultiplier tube (also called a photomultiplier) or the like is used, and a recorder 2 is used as a means for detecting the electron beam pattern or other electric characteristics of the detection signal. To use. The electron tube 1 is driven by the photomultiplier driver 3 in a predetermined manner. Further, the present device uses the seismic pendulum sensor 4 that measures seismic motion. The seismic pendulum sensor 4 is driven by the seismic pendulum sensor driver 5, and the recorder 2 is used as a means for performing the measurement.
The data input to the recorder 2 is transmitted to the computer 6, where the determination process such as the alarm immediately before the earthquake is performed. The embodiment of FIG. 3 will be described later.

The operating principle of the device will now be described. Figure 3
Indicates the general nature of electrons due to electromagnetic fields. The electrons flying in a vacuum have the property that their trajectories are easily bent by an electric field or a magnetic field. Therefore, when an electric field is applied, the activation of electrons is deviated as shown in FIG.
Current and its current waveform change. When a magnetic field is applied to the electron tube 1, the orbits of the electrons are also bent as shown in FIG. 3 (b). In either case, electron tube 1
The electric characteristics such as the energizing current of the electron beam change, and the pattern of the electron beam also changes. A well-known example is that the bright lines of an oscilloscope, TV, etc. may shift due to the effect of geomagnetism.

In this embodiment, a photomultiplier tube (for example, R928 manufactured by Hamamatsu Photonics) is used as the electron tube 1 which is most susceptible to the influence of geomagnetism. It is also possible to adopt an applied product of an electron beam generator incorporating an electron gun, which is incorporated in other electron tubes, cathode ray tubes, electron microscopes and the like. Since the photomultiplier tube is basically a kind of phototube, it has a conceptual structure as shown in FIG. The basic operation principle is that when light 8 is incident on the cathode 9 from the outside of the container 7 made of glass or the like that can transmit light, electrons 10 are generated, which are generated by the high voltage power supply 11 on the anode 12. Collected. Here, only one stage of the anode 12 is shown for the sake of simplicity, but a plurality of anodes 12 are included in the actual photomultiplier tube.
(Called a dynode) that multiplies and amplifies a small number of photoelectrons.

By measuring the signal with an ammeter or the like, the light intensity or the like can be measured. As mentioned above, electrons
Since the orbit is easily bent by the electromagnetic field, the cathode 9
From the time it reaches the anode 12, the orbit shifts due to the influence of the earth's magnetic field. Therefore, the first-stage anode 12
If there is a surface distribution on the surface, or if electrons collide with a place other than the anode 12, the output current changes. As can be seen from this description, the most susceptible electrons are the electrons that fly between the cathode 9 and the first anode. Therefore,
A photomultiplier tube having a long distance between the first anode (first dynode) and the cathode 9 and a photomultiplier tube having a distribution in the geometric shape of the first anode are particularly affected by electromagnetic fields. It is said to be easy. If it is selected for the purpose of the present invention, it means that the head-on type is more suitable than the side-on type among the photomultiplier tubes having a large tube diameter.

FIG. 5 is a schematic view of a cathode tube (electron tube) used as an electromagnetic field sensor. FIG. 6 is a diagram showing a configuration example of an electromagnetic field sensor 1A (electron beam generation detection means) using the electron tube 1 formed of a photomultiplier tube. The electron beam generation detection means 1A is made of a material that can transmit an electromagnetic field. Configured container 7
The electron tube 1 operates by irradiating the electron tube 1 with stabilized light from the light source 1a such as an LED through the filter 1b and the lens 1c. FIG. 7 is a configuration diagram of the electron gun type electromagnetic field sensor 1B (electron beam generation detection means), in which the electrons ejected from the electron gun 1f are targets 1g.
When the CCD camera 1h catches a change in the light emission pattern, the sensing is performed. When an electromagnetic field is applied to the sensor, the trajectory of the electron beam changes, and the position of the bright spot colliding with the target 1g also shifts. This change in position is captured by the CCD camera 1h. Although the current of the electron beam may change or the brightness may change, it can be easily detected by performing image processing using the CCD camera 1h.

Further, in the photomultiplier tube, in order to remove the influence of electromagnetic waves, the electromagnetic shield normally used is removed,
I tried to positively utilize the property that is easily affected by the electromagnetic field. It is desirable to use an electron beam generator including the above-mentioned electron gun, an electron tube such as a Braun tube, or the like so as to be able to detect the influence of an electromagnetic field and electrons. Further, in order to make it more resistant to noise, two electron tubes 1 are prepared and their outputs are compared with each other. If they are different from each other, it may be determined that they are noise. .

In the apparatus shown in FIG. 1, the output of the electron tube 1 having the above-mentioned properties is output to the recording paper by the recorder 2, and at the same time, the detection data by the seismic pendulum sensor 4 is also output. The seismic pendulum sensor 4 is installed for the purpose of easily detecting the occurrence of an earthquake of a magnitude that cannot be detected by the human body, such as an insensitive earthquake, and the weight 14 having an appropriate weight is attached to the optical fiber 15. It is hung and used as a pendulum. Earthquake pendulum sensor driver 5
Supplies a stabilized power to the light source 16 such as a light emitting diode to light it, and the light emitted from the light source 16 propagates through the optical fiber 15 and enters the optical sensor 17. The signal of the optical sensor 17 is amplified by the amplifier incorporated in the seismic pendulum sensor driver 5, and the output change is recorded on the recording paper of the recorder 2. Therefore, the earthquake pendulum sensor 4 is used to detect not only a sensitive earthquake but also a teleseismic earthquake or an insensitive earthquake. Instead of this sensor 4,
A seismograph or earth current detection sensor may be used. The device of the first embodiment can output a warning immediately before the earthquake, and the details of its operation will be described later.

FIG. 2 shows a second embodiment. The device of this embodiment is capable of outputting an alarm immediately before an earthquake and automatically or manually obtaining the estimated seismic intensity of the epicenter from the earthquake observation data. Further, the electron tube 1 and other measuring device are used together to improve the measurement accuracy. In FIG. 2, a ground current measuring instrument 22 to which an electrode 21 for detecting a ground current is connected is added to the basic configuration of the electron tube 1 and the recorder 2 which form the electron beam generation detecting means of FIG. Instead of the seismic pendulum sensor 4, a highly accurate seismograph 23 is installed. Further, the recorder portion of the earth current measuring device 22 is a continuous recording sheet, and the output of the electron tube 1 is recorded in the same row on this recording sheet. Normally, the change in the earth current is correlated with the change in the electron tube 1, but when the change in the earth current is a lightning strike or radio noise, the output of the electron tube 1 often does not change. In many cases, the recorder records the output changes of the electron tube 1 and the earth current measuring device 23 earlier than the seismic wave detection by the seismograph 23 and the seismic pendulum sensor 4. A seismograph 24 is connected to the seismograph 23. The output of the electron tube 1 and the output of the earth current measuring device 22 are given to the voltmeter 25, and further, those outputs and the seismograph 2
The output of 3 is input to the computer 6 via the communication line 26. In addition, from a plurality of measurement data described later, the seismic detection distance in the device configuration of FIG. 1 is a radius of 60 km, the warning range just before the effective is a radius of 40 km, and the seismic detection distance in the device configuration of FIG. It can be said that the radius of 200 km and the immediately-before-effective warning range have the performance of a radius of 80 km.

Next, a method of determining the immediately preceding alarm in the devices shown in the first and second embodiments will be described. The output changes of the electron tube 1 and the earth current measuring device 22 recorded by the recorder 2 and the computer 6 to which the recorder 2 is connected are generally as shown in FIG. Even if you directly read the output of the measured value,
This is also the case when counting the number of pulses for each fixed time. This is because changes in the earth's current and changes in the earth's magnetic field often change in a pulsed manner. Basically, the same observations are made only with the difference in whether they are observed as an average value or as a pulse. There is one reason. The vertical axis of FIG. 8 is the intensity (absolute value) of the measured value, and the horizontal axis is the time (hr). Normally, the signal intensity is at the level of A, but this value begins to increase and reaches the point B. To reach. At this stage, there is still a possibility of noise, so it is necessary to carefully observe the behavior of the seismic pendulum sensor 4 and the seismograph 23. Eventually, the measured value reaches the peak C point, decreases from that point, and becomes the E point, which is at the same level as before.

When the measured value is not noise, in many cases, the seismic pendulum sensor 4 and the seismograph 23 within 24 hours.
The tremor without P wave begins to be recorded. This is because the epicenter is far away or the magnitude of the earthquake is extremely small, so the P wave is attenuated and cannot be measured. By accumulating these measurements, it is possible to get a rough idea of the relationship between the magnitude of the earthquake, the epicenter distance, and the signal strength in FIG. These data cannot be unequivocally stated because the values vary considerably when the measurement system changes, but the magnitude is M
When observing the precursory phenomenon of more than 6 huge earthquakes, C
The height of the peak value of the point is more than twice the normal measurement level A point. Therefore, when continuous observation is performed, C
If the peak of the point gradually increases and the vibration duration of the seismic pendulum sensor 4 and the seismograph 23 gradually increases in units of 5 minutes to 10 minutes, it is presumed to be a sign of a huge earthquake. To be done. When an earthquake is predicted to occur through such observations, alarm points from points A to E defined in FIG. 8 are set.

For example, when an observation value that is twice as high as the average observation level A point is obtained, it is set as point B and a "warning" is issued. Whether or not this measured value is noisy is confirmed by the seismic pendulum sensor 4, the seismograph 23, or the like, or by comparing the outputs of the earth current measuring device 22 and the electron tube 1 as shown in FIG. If it is determined that this value is not noise,
When the point C is reached, an "alarm" is given. It is easier to determine the C point, which is the peak point, by taking the difference between the measured values at each sampling time and determining the C point when this value turns negative 10 times or more, rather than differentiating the measured value. Therefore, the peak point C can be determined. As for the alarm just before the earthquake, it is considered that the "immediate alarm" should be issued according to Enomoto's theory when the value of this point C becomes about 63%.
Since it seems to be related to the mechanism of earthquake occurrence,
The actual figures need to be carefully examined. Depending on the area and the case, it may be sufficient to use point C as the immediately preceding alarm point. When such a precursory phenomenon is measured, in many cases, it is considered highly likely that a huge earthquake of M6 or more will occur within 24 hours.

Next, a method of observation immediately before an earthquake and a procedure for determining an immediately preceding alarm according to the first and second embodiments will be described. Figure 9
Shows a plurality of observation time charts, and FIG. 10 shows a flowchart of the immediately preceding observation method and the determination of the immediately preceding alarm. (1) It is detected that the absolute value of the amount of change such as the pulse of the signal from the electron beam detection means or the average voltage value increases (#
1). (2) Observation is performed until the result as shown in FIG. 8 is obtained. (3) Eventually, the seismic pendulum sensor 4 and seismograph 23
Vibrations will be recorded. With this seismic record,
FIG. 9 shows an observation time chart of the plurality of observations in which the record of (2) is examined and the observation is performed a plurality of times. FIG. 9 shows an example of a time chart until a damaging earthquake arrives. The time when the observation started is t0, and the time when the earthquake occurred is t1. Since the precursory observation needs to perform the preceding phenomenon and the earthquake as one unit, these observation units are accumulated as data as shown in FIG. It can be understood from this figure that even if the electromagnetic precursory phenomenon is captured, if it is not accompanied by an earthquake, it can be treated as noise as described later. In this way, the precursory phenomena of earthquakes are empirically understood by accumulating observation records during normal times and during small-scale earthquakes. Generally, after observing the electromagnetic precursory phenomenon, 24-
If the seismic wave is not observed even after 72 hours or more, it is determined to be noise, and its signal strength, appearance time zone, and other common patterns are examined at this stage. Further, as in the second embodiment, when used in combination with the earth current measuring device 22 and the like , as the observed value of the electron tube 1 increases,
Since the observed value of the earth current measuring device 22 also increases, it can be distinguished from noise. In many cases, the electron tube 1 does not observe noise unless the geomagnetism fluctuates on a large scale. Further, unlike earth current, it is not affected by factories, power stations, electric railways, etc. Therefore, noise can be determined by comparing the values of both.

(4) As shown in FIG. 9, when the absolute value of the signal strength, the number of observations and the number of observation pulses of the electromagnetic precursory phenomenon increase, and the number of microearthquakes increases accordingly. Judges that it is a sign of a damaged earthquake. In this case, continue the observation, especially seismic pendulum sensor 4 and seismograph 2
When the vibration continuation time ta of No. 3 is examined and the vibration continuation time gradually becomes longer in units of 5 to 10 minutes, it is often a precursor of a huge earthquake which is the main shock (# 2, # 3). In addition, the absolute value of the signal intensity obtained in (1) in particular increases with each observation, so an alarm point is set when the following conditions are satisfied.・ When the vibration duration of the seismic pendulum sensor or seismograph is around 20 minutes, or when the preceding electromagnetic sign does not decrease, such as the baseline point A in Fig. 8 rising (# 4). ).・ Vibration duration of earthquake pendulum sensor and seismograph is 5-10
When it becomes longer in minutes or swarm earthquakes increase in the vicinity, and the signal strength of the electromagnetic precursor does not decline. As shown in FIG. 9, the duration of earthquake motion increases with each observation. The relation is ta1 <ta2, and it should be noted that the main shock is near when the time starts shaking for about 20 minutes. (5) If it is judged in the procedure of (4) that it is just before the earthquake, an alarm point is set as shown in FIG. (6) From FIG. 8, if a value more than twice the average observation level is observed, the warning point B is determined. The alarm at point C is set as a peak point when the amount of increase in the observed value decreases in multiple observations (# 5). The point D, which is the immediately preceding alarm point, is determined when the observed value decreases from the alarm point C (# 6). (7) There is a high possibility that an earthquake will occur within 24-72 hours from point D of the last warning.

By issuing this "immediate warning", it is possible to take measures such as evacuating residents and evacuating dangerous materials. However, it can be said that the warning just before the earthquake (prediction) functions as a disaster prevention system. Absent. Rather, disaster relief activities after the main shock will have an important meaning. Therefore, after the occurrence of the main shock, it is necessary to estimate the seismic intensity of the epicenter from the seismic waveform record of the seismograph 23 or the like installed to determine the rescue level.

After the occurrence of the main shock, the seismic intensity estimation related to the earthquake damage is performed by analyzing the seismic waveform according to the procedure shown in FIG. (8) If the seismic intensity of the epicenter is considered to be 5 or more, or if considerable damage is expected, judge at this stage. In addition, the direction of the epicenter and the disaster area cannot be obtained from the data of only one location, so information will be collected at this stage. However, be careful of the abnormal seismic region when performing a hypocenter evaluation. This point will be described later. (9) To predict the occurrence of large-scale aftershocks and induced earthquakes, continue the previous warning observation at this stage. As for the aftershock pattern after the main shock, the maximum aftershock may occur after the rest period in many cases, so pay attention to the seismograph data. If a judgment is made in the above procedure, disaster prevention activities can be carried out quickly. Also, since the maximum aftershock can be predicted by this method / judgment method, there is an effect that disaster relief activities can be carried out without worrying about the occurrence of aftershocks.

FIG. 11 is a flow chart showing how to obtain the estimated seismic intensity of the epicenter. The earthquake formula used for the hypocenter analysis program is as follows.

[Equation 1]

[Equation 2]

[Equation 3]

[Equation 4]

[Equation 5]

[Equation 6]

The method of estimating the seismic intensity of the epicenter (FIG. 11) is as follows. (1) The propagation velocity difference Vk between the P wave and the S wave is obtained as a constant (preliminarily investigated or obtained from observation data) (# 11). (2) Obtain the SP time difference τ from the waveform data (# 1
2). (3) The focal distance R is calculated using the first equation (# 13). (4) If the epicenter distance R is R ≧ 100 km, an abnormal seismic area may have appeared, so damage investigation and information collection will be conducted. (5) Obtain the maximum value of S wave and the maximum value of P wave (# 14). At this time, the maximum value of the S wave is obtained as √ (X ² + Y ² ) (vector value). (6) The magnitude M is calculated using the third and fourth equations (# 15). In order to use the acceleration value obtained from the seismograph in the third formula, it is necessary to perform waveform analysis by Fourier transform to convert the acceleration waveform into a displacement waveform, and the calculation error cannot be ignored. As a result of examination by the actual seismic waveform analysis, as shown in Tables 1 and 2, even if the magnitude is evaluated using the formula 4, the radius is 50k.
For earthquakes within m, relatively good approximations are obtained. Therefore, it is better to use the fourth formula for calculating the magnitude. (7) The Mercari seismic intensity at the observation point is calculated using the sixth equation (# 16). (8) The Mercari seismic intensity (including the decimal point) of the epicenter is estimated using Equation 5-1 (# 17). (9) Substituting the estimated Mercari seismic intensity of the epicenter into Equation 6-1 to estimate the seismic intensity of the epicenter (# 18). (10) Substituting the estimated Mercari seismic intensity of the epicenter into Equation 8,
Estimate the epicenter depth (# 19).

FIGS. 15 to 18 show the actually recorded seismic waveforms, and the analysis results are shown in Tables 1 and 2 below. The first to eighth equations were used for the analysis. Seismic waves
Since it has the property of decaying with distance, if the magnitude and depth of the earthquake can be estimated, the seismic intensity of the epicenter can be easily estimated. The seismic wave generated on the earth is attenuated by friction in the atmosphere and rocks, and its equation is expressed by an exponential function. Therefore, if the exponential function is fitted so as to follow the measured data, the fifth formula can be inferred. Since this fifth equation is not obtained by seismological consideration, it is considered necessary to introduce an improved formula later.

The actual propagation of seismic waves is very complicated due to the fact that the earth is a sphere with a liquid part inside and the existence of bedrock and structure lines, but it is necessary to arrive to rescue within one hour. In the range of distances in which is possible, this equation can be sufficiently approximated at present. This was actually confirmed by the past four seismic wave measurements. That is, when the equation 5 was verified with an actual seismic waveform, it was found that it could be used without any problem in the distance range and the radius 50 km range. At this point, it should be noted that the abnormal seismic region occurs. The abnormal seismic region can be easily discarded by obtaining the distance from the seismic waveform data to the epicenter. Normally, if the data is observed at a distance of 100 km or more and the epicenter has a depth of 100 km or more, even if the observation point analysis result shows a large value, the observation point will be an abnormal earthquake. It is likely to be included in the area. If you encounter such an example in the analysis result of the seismic waveform,
We should focus on collecting information. If it is absolutely necessary to make a judgment at the field level, it is better to judge that a damaged earthquake occurs when the communication network, railway, or lifeline is cut off.Therefore, substations, railways, road corporations and gas It is better to contact the company or water department to confirm the damage.

Next, the applicable range and installation guidelines of the present invention will be described. An earthquake has regional characteristics, and it is necessary to investigate the activity history of the earthquake for each place where the device of the present invention is installed. Moreover, it may be difficult to catch the electromagnetic precursory phenomenon depending on the mechanism of the earthquake. Therefore, here, the range of application of the present invention and the method of obtaining the distance attenuation formula in consideration of regional characteristics will be described. (1) Relationship between epicenter distance and earthquake damage Figure 12 shows the relationship between the observation points and the epicenter. Let r be the measurement limit distance from the observation point and R be the epicenter distance R. It is safe to think that the distance = radius,
The true distance to the epicenter is x, but when actually trying to find x, data for multiple observation points are needed, and the procedure for epicenter determination is slightly complicated. This is because the earth is an ellipsoid, so the coordinate axes are represented by the spherical triangle theory, but in the range of use of the present invention,
Since R is 100 km or less, the seismic waves do not propagate to the extent that the earth can be treated as an ellipsoid, so it is possible to estimate the epicenter with only one observation data. In the present invention, the direction of the epicenter cannot be estimated, and data of a plurality of observation points is required to estimate the direction. Regarding the accuracy of the present invention, Tables 1 and 2 show the results of analysis of actual seismic waveforms, and the seismic waveforms are shown in FIGS. The Mercalli intensity scale shown in Table 2 is shown in real number format for the purpose of hypocenter estimation, but originally it is an integer value. From the results of Table 2 which performed hypocenter estimation, it can be seen that hypocenter estimation is possible with relatively good accuracy. Judging from the observation data, it can be understood that the method of the present invention can be applied within a radius of about 50 km.

Further, immediately above the epicenter, the relationship is as shown in FIG. That is, even if the earthquake has a large M, if the epicenter is deep, the seismic acceleration at the epicenter becomes small. However, that is also a matter of magnitude, and in the case of an earthquake in which M is 4 or greater, the seismic acceleration of seismic intensity 4 is obtained just above the epicenter.
It can be easily estimated from FIG. 13 that many people are surprised by the earthquake, and if the damaging earthquake is M4.5 or more, the earthquake damage starts immediately above the epicenter. Here, it should be noted that the magnitude of seismic acceleration may not be directly related to earthquake damage. For details, I will leave the explanation to a specialized document, but at present, the JMA has improved the evaluation method of seismic intensity display,
The seismic intensity is announced so that the gap between the actual seismic intensity and the damage is reduced, and in the present invention, the seismic intensity is evaluated.
It is clear that the JMA formula should be introduced, but here, in order to give a qualitative explanation of the earthquake, we will focus on the discussion on seismic acceleration and examine it. From FIG. 13, M =
The graph of 3.0 shows that no matter how shallow the epicenter is, it does not reach the acceleration corresponding to seismic intensity 4. This is
In the case of earthquakes with M = 3.0 or less, it suggests that the earthquake is not a damaging earthquake, which is consistent with the observation results in many cases.
It also provides a theoretical basis for M being independent of seismic intensity.

[0034] Next, the relationship between the seismic source and epicenter distance,
It shows in FIG. In FIG. 14, interesting results can be seen for the damaged earthquake. Both earthquakes are 980 gal immediately above the epicenter, but the inclination of the seismic acceleration decay curve becomes gentle as the earthquake M increases. This indicates that the seismic wave is less likely to be attenuated as M (magnitude) increases, and it can be easily understood by looking at the graph that the larger the M, the larger the damaged area. In addition, it is shown in the graph that within the effective range of the present invention within 50 km of the epicenter distance, any earthquake is close to the acceleration level of seismic intensity 5, and it is possible to use an observation device with an effective radius of 50 km or more. Therefore, it can be understood that it can be used for the purpose of earthquake disaster prevention. In this way, the applicable range of the present invention can be obtained using a diagram.

In order to create this diagram, the equations 5 to 8 can be easily solved by solving them simultaneously. By the way, I doubt that there will be an earthquake equivalent to the acceleration of gravity, but in the Great Hanshin Earthquake (Southern Hyogo Prefecture Earthquake), 830g in Kobe
The seismic acceleration of al units is recorded. Therefore, in Takatori, the stopped train derailed, and due to the large vertical motion, underground structures that were said to be safe were destroyed by the earthquake. Many of the reinforced concrete structures that had suffered serious damage such as total destruction were caused by the collapse of the basement. Conventionally, it has been said that damage to underground structures occurs from around 1 G regardless of horizontal or vertical motion, so this indicates the possibility of seismic acceleration of 900 gal level. It is believed that there is. The fact that the underground structure collapsed suggests that an earthquake acceleration of about 1 G may exist depending on the depth of the epicenter and the size of M, and it gives an important lesson in considering urban disaster prevention. It was

(2) Presence / absence of electromagnetic precursory phenomenon due to difference in mechanism of earthquake Here, the electromagnetic precursory phenomenon, which is the gist of the present invention, will be considered. As mentioned above, the electromagnetic precursory phenomenon is closely related to the mechanism of earthquake occurrence. Therefore, due to the difference in the mechanism of earthquake occurrence, it is sufficiently conceivable that an electromagnetic precursory phenomenon is not observed or the time lag is short. Earthquakes have regional characteristics, and as will be described later, the cause and the frequency of occurrence also vary depending on the area. Here, in some cases, the cause of the earthquake,
I would like to think about the correspondence with the electromagnetic precursory phenomenon.
As described above, the gist of the present invention is released when the bedrock is destroyed. It is assumed that the generation of electrons will trigger the electromagnetic precursory phenomenon. In addition, due to the characteristics of the sensor used to detect the occurrence, the fluctuations in the earth's magnetic field are likely to be noise, and in order to remove this noise, a seismometer or seismic sensor is used together to minimize the effects of fluctuations in the earth's magnetic field. , Small. In the results observed in the present invention, the fluctuation of the earth's magnetic field can be sufficiently eliminated, so that the observation of the electromagnetic precursory phenomenon can be captured in correlation with the earthquake.

Therefore, the regional characteristics of earthquakes to be considered are classified as follows. (A) When the bedrock is fatigue-damaged by fault motion (intraplate earthquake), (b) earthquake due to groundwater or dam storage, (c) earthquake due to volcanic activity,
(D) Earthquake due to plate motion, (e) due to abnormal seismic zone, (f) Atomic bomb explosion and asteroid collision, rock fall, mine pile, and induced earthquake due to oil field excavation.

The matters described in the operation and effect of the present invention are applied to the earthquake of the type (a) including the type directly under the metropolitan area.
Most of these earthquakes are inland earthquakes, and 80% of the damaging earthquakes other than the tsunami in Japan fall into this category. An earthquake of type (a) has a shallow epicenter and does not have the cause of the earthquake inside the crust, so electromagnetic phenomena appear at the same time as the earthquake, or the time lag is short,
Alternatively, the epicenter is too shallow and there is no electromagnetic phenomenon. In addition, some earthquakes of this type are artificial, such as pumping water into the groundwater vein. Since damages due to this type of earthquake have not been reported in conventional observation records, they may be excluded from the scope of the present invention. (C) type of earthquake,
Although similar to (a), in many cases, the magma is magnetic, as seen in the magnetic lava of the Fuji volcanic zone, and thus the present invention can be applied. In this case, electromagnetic precursors and swarms may be observed almost at the same time, and whether or not an eruption has occurred and evacuation is possible based on the seismometer waveform data in the device configuration of the second embodiment. It is necessary to judge the sex (the earth ammeter may be omitted). When the present invention is applied, it becomes possible to predict "when full-scale volcanic activity will occur" rather than earthquake prediction, and it is possible to prevent sudden volcanic disasters. Earthquakes of type (d) account for most of the earthquakes observed in Japan, but not many are damaging earthquakes. Rather, because of the distribution of epicenters centered on the trench, the damage caused by the tsunami will be greater than the damage caused by the earthquake. Also, this type of earthquake
It is easily misunderstood as the type (A) type earthquake, but it is important to note that the epicenter is deep along the plate boundary,
The depth of epicenters is distributed up to around 400 km (deep earthquakes occur within a depth of 650 km).

Earthquakes which are the main targets of the present invention are as follows:
An earthquake that occurs inside the crust. The thickness of the crust is 3 on average
It is said to be 5 km, and in the Japanese archipelago, it is partially about 40
There is a thickness of km (75 km in the continental area, 5-7 k in the ocean)
It is considered to be the thickness of m). Also, 150 km to 20
The cause of an earthquake that occurs at a depth of 0 km or more is
It is considered to be due to the phase transition of the crustal constituents, and if these are taken into consideration, it is considered that there are earthquakes in which electromagnetic precursory phenomena can be observed and other earthquakes. At present, there are few earthquakes that occur at a depth of 70 to 100 km or more and are damaging earthquakes. Considering the thickness of the crust, the effective range of the present invention is a radius of 50 km-
It is considered to be a hemispherical shape of 80 km, and a depth of 10 km to 6
It is estimated that about half of the plate boundary type earthquakes occurring up to 50 km cannot be observed. Since the epicenter of the type (e) earthquake is extremely distant, it is difficult to catch the electromagnetic precursory phenomenon. The cause of this abnormal seismic region can be explained if the Q values of the island arcs that make up the Japanese archipelago are distributed in the depth direction, but details are explained in the references. Give up. Anomalous seismic regions can only be seen in distant and deep earthquakes, so they can be discarded if the focal distance is calculated. This method is as described above. Since the (f) type earthquake does not have a cause of occurrence in the crust, it is difficult to observe the electromagnetic precursory phenomenon, which is outside the scope of the present invention. Inferring from the data observed up to now, there is almost no possibility that it will lead to a damaging earthquake, and there is no problem even if it is outside the scope of the present invention (Reference: Tokuharu Utsu, seismology, Kyoritsu Zensho 216 , Kyoritsu Publishing).

(3) Consideration on seismic wave distance attenuation formula It is a well-known fact that seismic waves attenuate by distance.
Several evaluation formulas have been conventionally proposed. The formulas are shown in Formulas 9 to 12. [Distance attenuation formula derived from seismic method]

## EQU00007 ## I = exp (-. Omega.x / 2Qc) (9) I: amplitude Q: Q value c: velocity of seismic wave .omega .: circular frequency x: distance [distance attenuation formula by statistical method]

## EQU00008 ## Distance attenuation of maximum velocity amplitude log ₁₀ V _max = 0.61 M- (1.66 + 3.6 / X) log ₁₀ X- (0.631 + 1.83 / X) (10) M: Magnitude X: Distance V: Velocity amplitude

Equation 9] - maximum acceleration attenuation log ₁₀ of _{A max = 0.41M S -log 10 (} R + 0.032 · 10 0.41Ms) -0.0034R + 1.30 (11) log 10 A max = 0.51M J - log ₁₀ (R + 0.006 · 10 ^0.51Mj ) −0.0034R + 0.59 (12) MS: Surface wave magnitude R: Distance MJ: Meteorological Agency magnitude A: Acceleration amplitude

The above evaluation formula is synonymous with the fifth formula used in the present invention. Due to differences in the ground, etc., depending on the area, it is necessary to exercise caution when applying it, but this is given here because it is a commonly used evaluation formula. When the fifth formula cannot be used due to a regional difference or the like, it is preferable to create the evaluation formula by modifying the eleventh formula and the twelfth formula. Here, the fifth
The points to be noted in calculating the formula are shown below. Equation 9 shows the damping equation obtained by the seismic method. As mentioned above, magnitude and depth are important parameters for earthquake evaluation, but in the ninth equation, these parameters are standardized by the Q value and ω, which are coefficients of swayability. ing. Therefore, it cannot be used as it is. Therefore, it is possible to use the 11th and 12th formulas obtained by the statistical method.
Due to the geological structure, seismic wave attenuation is directional, and detailed examination revealed that it could not be used in some areas. The observed seismic waveform used to explain the present invention is
Both were observed in Tennoji Ward, Osaka City. A closer look at FIGS. 15 to 18 reveals the uniqueness of Osaka City. To explain this, FIG. 20 shows the geological structure around Osaka City, and FIG. 19 shows the peculiarities of seismic waves.

FIG. 19 is a diagram showing the difference in displacement waveform of the 1961 Kita-Mino earthquake of M7.0 observed at the Kobe Meteorological Observatory and the Osaka Meteorological Observatory. In this way, the displacement waveforms of Kobe and Osaka are not so different, but the displacement waveforms show a large difference. This is because the sedimentary layer called the Osaka Group, surrounded by hard rock, was excited by the seismic waves and acted as a waveguide. The difference in the geological structure also appeared in the 1995 Great Hanshin Earthquake (Nanbu Earthquake of Hyogo) in the form of strips of areas affected by the earthquake, such as Kobe, Ashiya, and Nishinomiya. This peculiarity appeared when the reflected wave was superimposed on the seismic waveform. For example, when looking closely at FIGS. 15 and 17, it can be seen that the Z-direction waveform (P wave) is divided into the first wave and the second wave. In either case, the time difference is about 4 seconds. Since the time difference between both waveforms is constant, it can be easily inferred that it is a reflected wave from a fixed object.Based on these data, considering the distance from the observation point, the Rokko Mountains system It is estimated to be a reflected wave. This is in good agreement with the fact that the observation point of the Osaka District Meteorological Observatory shown in FIG. 20 is 15 km from Mt. Rokko.

The observation point is located about 2 km south of the observation point of the Osaka District Meteorological Observatory and about 17 km from Mt. Rokko. The propagation velocity of the P wave is 4.5 km / se including the portion decelerated by the deposition layer in the surface layer portion around a depth of 10 km.
Since it is assumed to be around c to 7 km / sec, when considered in this velocity range, the results given from the observed seismic waveform are consistent. For these reasons, it can be seen that in the Osaka area, it is somewhat difficult to apply the distance attenuation formula as shown in general formulas 11 and 12. So, we had to calculate a new evaluation formula,
Since it is not possible to blindly calculate the evaluation formula, the following points were noted and the data were collected and evaluated. here,
Since we mainly conducted a survey on the felt damaging earthquakes that occurred in the past based on newspaper information, we could not perform statistical regression analysis. In addition,
As the basic equation, the 9th equation obtained by the seismological method was selected in consideration of the physical characteristics of the earthquake. That is, the ninth
The fitting curve was created from the equation and the fifth equation was obtained by the method of obtaining the coefficient.

Further, the Vk value can be obtained from the observed seismic waveforms of FIGS. 15 to 18 by the same method. Originally, regression analysis is the best choice, but in order to perform regression analysis, it is necessary to have an environment in which a certain amount of observed seismic waveforms can be browsed. Although regression analysis cannot be used in the present invention, the present invention may be implemented in an environment in which regression analysis can be used. Therefore, points to be noted when determining analysis parameters for earthquakes will be described below. . The basic data of the analysis is based on the observed seismic waveform record that can clarify the distance to the epicenter. At this time, the observed earthquake
It goes without saying that the waveform must be classified into an acceleration waveform, a velocity waveform, or a displacement waveform. Generally, a seismometer for disaster prevention is a strong seismometer, and acceleration and velocity seismometers are often used. Among them, it is necessary to select the objective variables and explanatory variables, keeping in mind that the accelerometer-type seismometer is the mainstream.

Usually, as the explanatory variables, epicenter parameters,
The characteristic parameters of the propagation path and the observation point are used. If the variables are independent of each other, the statistical analysis will lead to correct results, but the analysis of the seismic motion cannot always completely separate the contributions of the explanatory variables, and the coefficients will be correlated. For example, a magnitude parameter (M) is generally used as the epicenter parameter, but the value of this M is determined based on the maximum amplitude of a seismograph having a certain characteristic, so it may have a dependent relationship with the objective variable. is there. As for the propagation path parameter, in Japan, plate boundary type earthquakes are common, and since these earthquakes are far from the observation point, the earth was considered to be a sphere.
The epicenter distance and the epicenter distance are used. Also, in the US and other countries, inland earthquakes often have clear fault locations,
The distance from the fault is often used. In the present invention,
Since the inland earthquakes that occur near large cities are assumed, the American method is adopted for the epicenter distance. The parameters of the observation points are generally classified by ground type and ground velocity.

When the regression equation is obtained by combining the parameters described above, it is common to use the form of linear combination. The function of magnitude is a first-order system of M, and the general form of the function of distance is represented by −b · log (R + h) −dR, and the geometric damping term is d = 1 for a body wave and d = for a surface wave.
0.5 (d = 0 in some cases). If these analyzes are successful, formula 11 and formula 1
It is possible to obtain an evaluation formula having a form close to the two formulas. For details, please refer to the reference document. In the present invention, the fifth formula was selected as the evaluation formula in consideration of the property of the basic analysis data (reference document: Masatetsu Izumi, Seismology, Kashima Press). ).

Further, FIG. 21 shows an example of observation data when an earthquake sensor having the same properties as the earthquake pendulum sensor 4 is used in the apparatus of the first embodiment. This data shows the output signals of the electromagnetic field sensor and the seismic sensor using the electron tube 1, and the recorder 2 is a pen recorder (LR4 manufactured by Yokogawa Electric).
220), which captures the electromagnetic precursory phenomenon of the earthquake observed on October 14, 1995. The waveform due to the earthquake is as shown in FIG.
Approximately 4 hours before the earthquake occurred, about 4 hours before, an electromagnetic field sensor was used to capture fluctuations considered to be precursors. The earthquake occurred at 2:04 am, and the signal from the earthquake sensor fluctuated almost at the same time. From this data as well, it can be understood that the time point at which the signal of the electromagnetic field sensor reaches a peak and then slightly decreases may be determined as the immediately preceding alarm issuance. Note that the data observation was not reliable for continuous use of the high-voltage power supply part of the device, and the seismic sensor was magnetic line type, so intermittent operation was performed. That is, the electromagnetic field sensor detects the electron tube 1 (R92) at 20:00.
8) High voltage ON (to ensure stability of circuits etc.), light source driver ON, light source OFF, light source ON at 21:00, electron tube 1 at 05:00 the next day.
FF. Bias OFF at 20:00 on seismograph
(Observation start), Bias ON at 05:00 the next day (Observation end). If the seismic pendulum sensor 4 is used instead of the seismic sensor, it is not necessary to rest the device.

Next, details of various constituent elements used in the above embodiment will be described. FIG. 22 is a sectional view of the earthquake pendulum sensor 4. Although the weight 14 is suspended by the optical fiber 15, the weight 14 may have a structure in which the optical fiber is along a kite string or a piano wire. Light from a light source 16 such as an LED or a laser is guided to the optical fiber 15, and this light is transmitted to an optical sensor 17 such as a photodiode.
Be guided to. When there is an earthquake, the weight 14 starts to sway, whereby the optical axes of the optical fiber 15 and the optical sensor 17 are deviated, and light enters the optical sensor 17 or does not enter. As a result, the electric output of the optical sensor 17 fluctuates, and if it is recorded by a pen recorder or the like, it functions as an earthquake sensor.

FIG. 23 is a diagram showing the installation situation of the seismograph. As the seismograph 23, a strong motion seismometer is selected for installation for disaster prevention purposes, and mainly velocity type and acceleration type are widely used. In addition, there are displacement-type seismometers, but this type of seismometer is often installed underground for high academic sensitivity and can detect quite small vibrations, mainly for academic purposes. It is designed so that P waves of small magnitude earthquakes and distant earthquakes can be reliably captured. It is also known that installing a seismograph in the basement is effective because it can cut out the vibrations of cars, railways, etc. that propagate from the ground. FIG. 23 shows the installation configuration of the seismograph 23 that observes the seismic waveforms of FIGS. For the purpose of disaster reduction, it is sufficient in this level of equipment, when the vibration prone and noise around occurs, it is better to equipment in the basement goes without saying. It is necessary to pay attention to not only the vibration environment around the seismograph but also the vibration of the reinforced concrete to be careful when installing it. Reinforced concrete is surprisingly easy to transmit vibrations, and even vibrations when walking by humans propagate to a wide range with considerable strength.

The seismograph 23 is installed with these points in mind, and a marble 31 as a vibration absorbing / dissipating material is placed on the ground floor of the earth floor where no reinforcing bars are present. It was fixed with a material, and used as a countermeasure against miscellaneous vibration (noise) of the seismograph 24 which is the sensor part of the seismograph 23. When burying or fixing the marble 31 with resin, care must be taken so that the foundation of the building does not hit the foundation of the marble 31. The detection signal of the seismic sensor 24 is input to the display unit that constitutes the observation section. In addition, like the seismograph, the seismic pendulum sensor 4 requires caution when installing. Since the seismic pendulum sensor 4 is not as accurate as the seismograph, it rarely malfunctions even in a fairly rough installation, but it is necessary to pay attention to the vibration environment of the installation site.

FIG. 24 is a diagram showing a procedure for installing an electromagnetic field sensor using an electron tube. The electromagnetic field sensor may be installed anywhere if there is no particularly strong vibration, but due to its operating characteristics, it may be in a place where a large current is present, a place where a magnetic substance such as an electromagnet or reinforced concrete or a magnetic field line is generated, or a pseudo electromagnetic field. It is not desirable to use it in a shielded place, and if possible, it is ideal to make cabinets using non-magnetic materials such as plastic and brass and place them outdoors (even in a wooden house). In the case of outdoor arrangement, it is better to consider temperature compensation by mounting an air conditioner in the cabinet. FIG. 24 shows an XYZ electromagnetic field sensor.
Although installation drawings of three directions are shown, one direction is sufficient unless otherwise specified. Although not shown, the earth current measuring instrument 22 has various installation procedures depending on the type of the instrument, and detailed description thereof will be omitted.

FIG. 25 is a diagram showing the basic configuration of the disaster prevention earthquake measurement system. FIG. 26 is a diagram showing an example of a design of a display device in the system. Although the configuration in the case of installing each device has been described above, the system of the present invention can be integrated into one device. A display of the personal computer 6 can be used as the display device 6a, which is a display device. However, a liquid crystal display with a touch panel or the like is used in the display portion, and the computer is built in the display device as a circuit board. Such a design is possible. With such a configuration, the keyboard portion can be simplified and the operation becomes clear, so that it becomes more practical and the burden on the user can be reduced. As shown in FIG. 26, the display of the display is divided into the electromagnetic field display panel 34 and the earthquake display panel 35. The time scale of the earthquake is significantly different from the time scale of the electromagnetic precursory phenomenon. That is the main reason.

In other words, the phenomenon of an earthquake ends in 10 seconds to a few minutes, while the electromagnetic precursory phenomenon requires about 1 week to 1 day. Therefore, displaying the seismic waveform and the electromagnetic precursory phenomenon on the same display is very inconvenient to use. Therefore, FIG.
The display part was divided like this. If it is a display device that can do this on one screen, you can use it.
Noise sometimes appears in the electromagnetic precursory phenomenon, so it is easier to perform maintenance if the seismograph and its arithmetic unit are independent for discrimination and operation check. . Further, since the display device of FIG. 26 has a built-in hard copy printer 36, it can be used for daily observation work. The hard copy printer 36 has a function of making a hard copy of data on the display by selecting the touch panel keys.

The embodiment shown in the present invention is the most preferable example, and it is desirable to install a computer when operating the immediately preceding alarm device unattended or when a seismograph is installed side by side, but the device is operated. In the above, there is no particular need.
Further, in the case of performing earthquake precursory observation using an electron beam, a partial abbreviation of devices and technical means, and devices, circuits, means and their configurations having predetermined technical functions are It is possible to make various changes such as replacement with other devices, circuits, means, and configurations thereof having a common technical function. In addition, introduction of another evaluation method into the evaluation formula, modification of some of the procedures using a computer, an electronic circuit, or a precision machine, or an abbreviation, etc. do not depart from the scope of the claims of the present invention. It can be implemented in a range.

FIG. 15 to FIG. 18 actually recorded as described above.
The results of the hypocenter analysis of the seismic waveform of are shown below.

[Table 1]

[Table 2]

[0056]

As described above, according to the present invention, the fluctuation of the electromagnetic field can be detected by using the means for generating the electrons exposed to the electromagnetic field, and such an electromagnetic field sensor is used. By measuring electrical characteristics such as electron beam pattern, it is possible to detect the precursory phenomenon of an earthquake.
Pre-earthquake warning can be issued accurately just before the occurrence of the main shock. Further, since the electromagnetic field sensor and the seismic sensor are used together, it is possible to eliminate the noise component in the electric characteristics and detect the precursory phenomenon with high accuracy. In addition, by analyzing the seismic waveforms after the main shock it is possible to estimate the seismic intensity of the epicenter in only 1 altogether over data, can build a system that can be organically support to relief efforts from the main shock occurred, such as the communication is interrupted In the event of a large-scale large-scale earthquake, it will be possible to create a system that can act on the spot. This is based on the lesson that during the Great Hanshin Earthquake, buildings such as fire stations and police stations at the epicenter of the earthquake collapsed and communication lines were cut off, failing to exert sufficient functions. By implementing the present invention, it is possible to provide a highly accurate earthquake disaster prevention system to society,
It is possible to protect human life and property from earthquake disasters.

[Brief description of drawings]

FIG. 1 is a configuration diagram of an alarm device just before an earthquake disaster prevention according to a first embodiment of the present invention.

FIG. 2 is a configuration diagram of an earthquake disaster warning device according to a second embodiment of the present invention.

FIG. 3 is an explanatory diagram of electron trajectories that change according to an electromagnetic field.

FIG. 4 is a conceptual structural diagram of a photoelectric tube.

FIG. 5 is a conceptual structural diagram of a cathode ray tube.

FIG. 6 is a configuration diagram of an electron tube electromagnetic field sensor.

FIG. 7 is a configuration diagram of an electron gun type electromagnetic field sensor.

FIG. 8 is a time-intensity characteristic diagram of an electromagnetic precursory phenomenon.

FIG. 9 is a diagram showing a time scale until occurrence of a damaging earthquake.

FIG. 10 is a flow chart of a last minute warning determination process based on last minute observation.

FIG. 11 is a flowchart of seismic intensity estimation processing of the epicenter.

FIG. 12 is a diagram showing a relationship between an observation point and a measurement limit distance.

FIG. 13 is a characteristic diagram of seismic acceleration directly above the epicenter and epicenter depth.

FIG. 14 is a relationship diagram between the epicenter distance and the seismic acceleration.

FIG. 15 is a diagram showing an actually recorded seismic waveform.

FIG. 16 is a diagram showing an actually recorded seismic waveform.

FIG. 17 is a diagram showing an earthquake waveform actually recorded.

FIG. 18 is a diagram showing an earthquake waveform actually recorded.

FIG. 19 is a diagram showing positions of Kobe Meteorological Observatory and Osaka Meteorological Observatory and observed displacement waveforms.

FIG. 20 is a diagram showing a difference in ground conditions between Kobe and Osaka.

FIG. 21 is a diagram showing recorded data of an actually observed electromagnetic field sensor and seismograph.

FIG. 22 is a sectional view of an earthquake pendulum sensor.

FIG. 23 is a layout diagram of a seismograph.

FIG. 24 is a layout view of an electromagnetic field sensor.

FIG. 25 is a basic configuration diagram of a disaster prevention seismograph.

FIG. 26 is a front view of an indicator of the disaster prevention seismograph.

[Explanation of symbols]

1 Electron tube (electron beam generation detection means) 1A electromagnetic field sensor (electron beam generation detection means) 1B Electron gun type electromagnetic field sensor (electron beam generation detection means) 2 Recorder (electrical characteristic detection means) 4 Earthquake pendulum sensor (earthquake measuring means) 6 computer (determination means) 8 seismograph (earthquake measuring means) 22 Earth current measuring device (earthquake measuring means) 23 seismograph (earthquake measuring means) 24 seismic sensor

─────────────────────────────────────────────────── ─── Continuation of front page (51) Int.Cl. ⁷ Identification code FI G01V 8/10 G01V 9/04 Z (58) Fields investigated (Int.Cl. ⁷ , DB name) G01V 1/00 G01V 1 / 18 G01V 1/28 G01V 3/02 G01V 3/12

Claims (5)

(57) [Claims] 1. By changing the orbits of electrons flying in space
Spatial electromagnetic by electron tube that detects the generation of electromagnetic field (magnetic field)
Field sensor and the space electromagnetic field sensor include an artificial electromagnetic field or a space electromagnetic field
Use by exposing to the electromagnetic field,
Immediately before an earthquake, an electrical characteristic detecting means for measuring a signal, an earthquake measuring means by a seismograph for performing an earthquake observation, and a signal from the electrical characteristic detecting means are used immediately before the earthquake.
Electromagnetic precursor that observes the generated electromagnetic precursor
Phenomenon observation means, the seismic measurement means and the electromagnetic precursory phenomenon observation means
According to the observation results by
Even if a period of time or more has elapsed, the seismic wave can be
If it is not measured, it is judged as noise and the seismograph within a predetermined time after the electromagnetic precursory phenomenon is observed.
When the seismic wave was observed by the measuring means,
The vibration duration of the seismic waveform becomes longer, and
When the signal strength of the aerial precursor phenomenon increases, the signal strength
Just before the earthquake when the degree reached a peak and then decreased slightly
Analyzes the earthquake waveforms observed by the earthquake measurement means and the alarm generation means immediately before the earthquake that issues an alarm
However, from the observation data of at least one place in the event of an earthquake
Calculate the epicenter distance by the formula to calculate the epicenter distance, and
The magnitude is calculated by the formula
Distance attenuation that shows that seismic waves attenuate with distance
Estimate the seismic intensity of the epicenter and the depth of the epicenter using the formula
An earthquake alarm system immediately before earthquake disaster prevention, characterized by comprising a hypocenter analysis means . 2. A ground current meter for measuring ground current is further provided.
The electric characteristic detecting means includes an artificial electromagnetic field and a space electromagnetic field.
Signal from the spatial electromagnetic field sensor exposed to an electromagnetic field
And the measurement of earth current by the earth ammeter
And the noise discrimination means changes the earth current by the earth ammeter.
When the correlation is correlated with the output change of the spatial electromagnetic field sensor
If there is no correlation, it is determined to be noise.
The alarm generator immediately before earthquake disaster prevention according to claim 1, wherein 3. The space electromagnetic field sensor is a photomultiplier tube.
Electron beam generator with built-in electron tube or electron gun
Earthquake Disaster shortly before the alarm generating apparatus according to claim 1 or claim 2, wherein it is a location. 4. Use of electrons flying in space for fluctuations in electromagnetic field
Signal from the space electromagnetic field sensor
Signal, the amount of change such as the pulse or voltage average value of the signal
Electrical characteristics until the absolute value increases and the amount of change decreases
Seismometer that measures seismic waves by performing an electrical characteristic detection step that detects
Measuring step and the electrical characteristic detected by the electrical characteristic detecting step
Is regarded as an electromagnetic precursory phenomenon, and is this electrical characteristic detected?
Within a predetermined time from the earthquake measurement step
When not measured, the electromagnetic precursory phenomenon is judged as noise.
Separately, when an earthquake is measured within the prescribed time, it is electromagnetic
The noise discrimination step which is regarded as a precursor phenomenon and the electromagnetic discrimination precursor phenomenon are judged by the noise discrimination step.
Measured in the seismic measurement step and the separated electrical characteristics.
Treated earthquakes as an observation unit, and
Of the electromagnetic precursory phenomenon , and
Signal intensity or observed pulse of electromagnetic electromagnetic precursory phenomenon
The number of observations and the number of observations have increased, and
The duration of seismic waves measured at
Indicates that when electromagnetic swarms are observed, the number of electromagnetic precursory phenomena is small.
Based on the signal strength, if the signal strength is a peak point
The point decreased from that point is defined as the previous alarm point and the previous alarm is output.
A method for issuing an alarm immediately before an earthquake disaster , comprising: an alarm issuing step immediately before an earthquake. 5. At the step of issuing an alarm immediately before the earthquake
In addition, be careful that the value is more than twice the average observation level.
And the increase in the observed value decreases in multiple observations
From the point that the warning was set in the above multiple observations
The method for generating an alarm immediately before an earthquake disaster prevention according to claim 4, wherein the alarm is set to be an alarm immediately before the decrease .