KR101624858B1 - Method for producing radius of strong wind and storm of typhoon using satellite data of Chullian satellite - Google Patents

Method for producing radius of strong wind and storm of typhoon using satellite data of Chullian satellite Download PDF

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KR101624858B1
KR101624858B1 KR1020150165304A KR20150165304A KR101624858B1 KR 101624858 B1 KR101624858 B1 KR 101624858B1 KR 1020150165304 A KR1020150165304 A KR 1020150165304A KR 20150165304 A KR20150165304 A KR 20150165304A KR 101624858 B1 KR101624858 B1 KR 101624858B1
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김옥희
차은정
김진철
홍성은
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대한민국(기상청장)
(주)지아이소프트
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Abstract

Disclosed is a method to calculate a radius of a strong wind and a storm of a typhoon using satellite data of a communication, ocean, and meteorological satellite (COMS) which increases accuracy. The method to calculate the radius of the strong wind and storm of the typhoon using satellite data of the COMS comprises: a process of defining a symmetric wind speed (V(r′)) of a typhoon by the following mathematical equation; a process of modeling two relaxation coefficients (a1, a2) using satellite data of the COMS; and a process of using the two relaxation coefficients (a1, a2) to calculate the radius of the strong wind and storm of the typhoon.

Description

[0001] The present invention relates to a method for generating strong wind and storm radius of a typhoon using Chollian satellite data,

The present invention relates to a method for calculating a strong wind and a storm radius of a typhoon, and more particularly, to a method for calculating a strong wind and storm radius of an improved typhoon using dual parameters calculated using the first geostationary orbit satellite, will be.

It is very important to understand the wind velocity structure of the typhoon. In particular, the radius of maximum wind (hereinafter referred to as RMW) is the distance from the center of the typhoon to the place having the maximum wind velocity, Variable. Maximum precipitation appears near RMW, and maximum intensity of typhoon can be estimated using RMW. Especially, in order to predict the storm surge and wave more precisely during typhoon surveillance, it is necessary to calculate accurate sea wind. Typhoon parameters such as typhoon center pressure, RMW, and ambient pressure distribution are used for this sea wind calculation.

The method of calculating RMW is as follows. Kossin et al. (2007) calculated the RMW using the size of the typhoon eye (REye) as follows.

RMWest = a0 + a1 REye

Here, a0 and a1 are constants a0 = 2.8068 and a1 = 0.8361. This regression equation accounts for 60% of the total RMW variability.

The size of the typhoon eye REye is calculated as follows.

First, the typhoon 's snowblown typhoon has a warm core at the center due to strong winds and strong winds. Therefore, the TBB (brightness temperature, black body temperature) at the center of the typhoon should be higher than the surrounding area. And a 45-degree isotherm can be defined as the wall of the typhoon eye (Kossin et al., 2007). In particular, when the TBB is below -50 on the typhoon eye wall, the value of REye is defined as the average of the distance from the center of the typhoon to the sub-zero of 45 degrees. This method can be calculated only when the typhoon is clearly visible, so this algorithm is included in ADT (Advanced Dvorak Technique) Typhoon analysis system, which is operated by the Meteorological Agency. However, the calculation results of RMW are database not.

Lajoie and Walsh (2008) proposed a method to calculate the RMW using the size of the typhoon 's eye and the lowest temperature at the top of the cloud based on the study on the structure of the typhoon' s eye. If h is a parameter for the cloud structure, RMW is calculated as follows.

RMWest = [(1 - h) RTop + h REye]

Where RTop is the minimum temperature at the top of the cloud. h has an average value of 0.6 as a result of observation data such as aeronautical observation and drop zone measurement. Lajoie and Walsh (2008) show that the RMW and observed RMW are very similar when h is fixed at 0.6. However, this method can also be used only when the eye of the typhoon is clear.

In the absence of typhoon eyes, the RMW has a linear relationship with very high accuracy, depending on the maximum wind speed. The following RMW can be proposed by modeling this.

Figure 112015114969167-pat00001

Where the unit is km. This is applied to the existing galeoid radius equation to complete the strong wind radius algorithm.

For storms with a maximum wind speed of 15 m / s or less, the storm radius can be calculated as follows.

Figure 112015114969167-pat00002

here,

Figure 112015114969167-pat00003
Is the relaxation coefficient,
Figure 112015114969167-pat00004
Wow
Figure 112015114969167-pat00005
Is a constant.
Figure 112015114969167-pat00006
Is the maximum wind speed.

The storm radius can be calculated as follows for a typhoon with a maximum wind speed of 25 m / s or more.

Figure 112015114969167-pat00007

Knowing the center position of the typhoon, the maximum wind speed radius, the relaxation coefficient, and the maximum wind speed, the wind field corresponding to the large diameter plane can be obtained. Here we add the velocity of the typhoon to produce an asymmetric wind field.

The velocity of the typhoon is obtained by dividing the center position at the time before analysis and the distance of the center position in the analysis time by the analysis time difference. Since there is an error in the center position, the wind field is repeatedly generated for the eight surrounding positions shifted by 0.1 degree from the center position. Each of these wind fields is called an ensemble member. These are averaged to yield the final asymmetric wind field. Here, a wind speed line such as 15 m / s and a wind speed line such as 25 m / s are displayed to indicate the gust radius and the storm radius including asymmetry.

The problem of this conventional algorithm proposed by Lajoie and Walsh is that the relaxation coefficient

Figure 112015114969167-pat00008
Is assumed to be a linear form of maximum wind speed, it can have considerable errors in weak typhoons and strong typhoons.

Fig. 1 shows the comparison of the repetitive symmetric wind speeds with the modeled symmetric wind speeds observed in strong and weak typhoons.

Figure 1 compares the symmetric wind speeds of the typhoons obtained from the YOTC reanalysis data with the symmetric wind speeds modeled by the upper storm / storm radii divided into strong and weak typhoons. In FIG. 1, the horizontal axis represents the distance from the center of the typhoon, and the vertical axis represents the symmetric wind speed of the typhoon. All the typhoons are divided into strong typhoons and weak typhoons, respectively.

Referring to FIG. 1, it can be seen that the values are comparable to those obtained from relatively reanalysed data for weak typhoons (see Figure (a)), .

This means that the conventional algorithms are relatively well-suited for typhoons with moderate or smaller sizes, but there is a significant level of error for strong typhoons. The reason is that strong typhoons suddenly develop near the center of the typhoon, so the structure of the symmetrical wind speed is broken. That is, it is difficult to assume a symmetric wind speed structure that exponentially decreases in the vicinity of the center. On the other hand, far away from the typhoon, the structure of the typhoon is decreasing exponentially before the typhoon is strongly developed.

In fact, comparing the radial radius calculated using the conventional algorithm and the actual radial gauge is almost the same for weak typhoons, but it can be seen that there is some difference between model and observations for strong typhoons.

Next, since the coefficients of the existing strong wind / storm radius algorithm are determined as YOTC reanalysis data, there is a problem that it needs to be corrected to values of other observation data. In particular,

Figure 112015114969167-pat00009
in
Figure 112015114969167-pat00010
Wow
Figure 112015114969167-pat00011
Is a value determined from the YOTC reanalysis data, so it is necessary to recalculate the relaxation coefficient to the value based on the observed data, ie, the polar orbital satellite sea-wind data.

In addition, the conventional algorithm has a disadvantage that the strong wind radii are underestimated in the case of a strong typhoon.

In addition, since the wind structure of typhoon is generally asymmetric, asymmetric wind speed should be considered.

The present invention has been devised to solve the above problems, and a method of calculating a strong wind and a storm radius of a typhoon using the Chollian satellite data which can increase the accuracy by adjusting the relaxation coefficient determined using the YOTC reanalysis data using the QSCAT ground wind data The purpose of the presentation is to do so.

A method for calculating a strong wind and a storm radius of a typhoon using satellite data according to the present invention,

A Method for Calculating Strong Wind and Storm Radius of Typhoon Using Chollian Satellite Data

A process of defining the symmetric wind speed V (r ') of the typhoon by the following equation;

Figure 112015114969167-pat00012

Here, r 'is a distance from the maximum wind speed radius V MAX

Figure 112015114969167-pat00013
ego

        r is the distance from the typhoon center

R MAX is the maximum wind speed radius

        a1 and a2 are the relaxation coefficients

Figure 112015114969167-pat00014

Figure 112015114969167-pat00015

Modeling the two mitigation coefficients a1 and a2 through the quasi-satellite data;

Calculating a strong wind and a storm radius using the two relaxation factors a1 and a2;

And a control unit.

Here, the process of modeling the two relaxation coefficients a1 and a2

Using the QSCAT data as observations,

Figure 112015114969167-pat00016
To minimize
Figure 112015114969167-pat00017
and
Figure 112015114969167-pat00018
.

Here, a numerical method was used. That is, by substituting all possible values,

Figure 112015114969167-pat00019
To minimize
Figure 112015114969167-pat00020
and
Figure 112015114969167-pat00021
, And then calculated
Figure 112015114969167-pat00022
and
Figure 112015114969167-pat00023
Respectively
Figure 112015114969167-pat00024
Assuming a linear equation for the regression coefficient and constant
Figure 112015114969167-pat00025
,
Figure 112015114969167-pat00026
, And
Figure 112015114969167-pat00027
,
Figure 112015114969167-pat00028
.

Here, the symmetrical wind field is obtained using the storm radius of the calculated typhoon, the asymmetric wind field is made by adding the typhoon moving speed at the same time to the symmetrical wind field, and a wind speed line such as 25 m / s is connected at the asymmetric wind field And calculating a storm radius including the asymmetry.

Here, a symmetrical wind field is obtained by using the calculated typhoon radius of wind, and an asymmetrical wind field is added to the symmetrical wind field by collectively adding a typhoon moving speed. In this asymmetric wind field, a wind speed line of 15 m / And calculating a gust factor radius including the gender.

According to the method of calculating the strong wind and the storm radius using the Chollian satellite data according to the present invention, it is possible to obtain the result that the gust radius directly obtained from the QSCAT and the correlation coefficient of about 0.96 can be more precisely predicted the strong wind and the storm radius of the typhoon .

Meanwhile, the method of calculating the strong wind and the storm radius using the Chollian satellite data according to the present invention has an effect of accurately predicting the strong wind and the storm radius of the typhoon by introducing the asymmetry of the strong wind in consideration of the direction of the typhoon.

Fig. 1 shows the comparison of the repetitive symmetric wind speeds with the modeled symmetric wind speeds observed in strong and weak typhoons.
Figure 2 shows the synthesis of typhoons from QSCAT ground wind data.
3 shows the relationship between the maximum wind speed and the estimated relaxation coefficient.
FIG. 4 shows a comparison between the calculated value and the observed value of the strong wind radius algorithm using YOTC and QSCAT.
Figure 5 shows the QSCAT data for all hurricanes, weak typhoons, mid-storms, and strong typhoons and the symmetric wind speed using a double exponential equation.
Fig. 6 shows the compatibility of the maximum wind speed and the double index coefficient of the typhoon.
FIG. 7 shows the symmetrical gust fan radius and the QSCAT ground wind estimated from the strong wind and storm radius calculation algorithm according to the present invention.
FIG. 8 shows the gust wind radius calculated by the improved algorithm and the gust wind radius of QSCAT.
Fig. 9 shows a schematic diagram of a typhoon rotation.
Fig. 10 shows an example of typhoon rotation.
11 shows the brightness temperature according to the traveling direction of the typhoon.
Fig. 12 shows the sea wind according to the traveling direction of the typhoon.
Figure 13 shows the TBB according to the intensity of the typhoon.
Fig. 14 shows the TBB composition and the left / right structure of the progress direction according to the intensity of the typhoon.
FIGS. 15A and 15B show the front and rear left and right structures of the TBB composition and the traveling direction according to the latitude value at the center of the typhoon.
FIGS. 16A and 16B show the front wind direction and the left wind direction and the right wind direction, respectively, of the sea wind composition and the traveling direction according to the latitude value of the typhoon center.
FIG. 17 shows the TBB composition and the left / right structure before and after the direction of the progress of the typhoon according to the hardness value of the typhoon.
Fig. 18 shows the front wind direction and the left wind direction and the right wind direction of the wind direction in accordance with the hardness value of the center of the typhoon.
FIG. 19 shows the dispersion of the gust wind radius calculated by WINDSAT and the gust wind radius calculated by the algorithm.
FIG. 20 shows the distribution of the gust winds calculated by WINDSAT and the gust wind radii calculated by the algorithm.
FIG. 21 is a block diagram showing a configuration of an apparatus using a method of calculating a strong wind and a storm radius of a typhoon using the Chollian satellite data according to the present invention.

DETAILED DESCRIPTION OF THE PREFERRED EMBODIMENTS Hereinafter, the present invention will be described in detail with reference to the accompanying drawings.

The definitions of the terms used in the present invention are as follows.

Wind speed (15-m / s isotach): 15 m / s Wind speed line

Storm radius (25-m / s isotach): 25 m / s Wind speed line

Maximum Wind Speed: The maximum sustained wind speed of the typhoon, which is also known as the maximum wind speed, V MAX .

Radius of Maximum Wind (RMW): Distance from the center of the typhoon to where the maximum wind speed appears, also called R MAX .

R TOP : The distance from the center of the typhoon to the point where the minimum cloud temperature appears.

Typhoon Eye size: The size of typhoon eye, also known as R EYE .

Relaxation coefficient: The degree of symmetric wind speed decreases with distance in the maximum wind speed radius of typhoon. It is a function of maximum wind speed.

YOTC (Year of Tropical Convection): High-resolution reanalysis data produced by using both real observations, satellite observations, and models to detect equatorial and subtropical convective activity.

QSCAT (Quick Scatterometer) Source: One of the sea-based data produced by microwave imaging of polar orbiting satellites.

Figure 2 shows the synthesis of typhoons from QSCAT ground wind data.

Referring to FIG. 2, it can be seen that the right side of the movement direction of the typhoon is greater than the left side. This means the wind speed generated by typhoon movement. Since the other effects are relatively small, it seems reasonable to add the speed of movement to the symmetric wind to produce asymmetric wind speed.

Referring to FIG. 2, a wind structure of a typhoon that is likely to have a relatively large number of samples can be seen. Since this data is only available until 2009, it is difficult to compare directly with the typhoon parameters obtained from the Chollian satellite data. However, because the nature of the typhoon satisfies stationarity, it can be used to adjust the coefficients used in the typhoon algorithm. Using these data, we estimated two coefficients of the linear form that estimate the mitigation coefficient.

Even though only one of the YOTC data and the QSCAT data can estimate the mitigation coefficient, this is because the YOTC data is a reanalysis data and may differ slightly from the facts. However, QSCAT data is also produced from polar orbiting satellites, so the QSCAT data may be slightly different from the facts. However, since the QSCAT data is judged to be a more credible data, the QSCAT data is written and compared with the YOTC data.

The two coefficients estimated using YOTC data are as follows.

Figure 112015114969167-pat00029

Figure 112015114969167-pat00030

The adjusted coefficients using QSCAT are as follows.

Figure 112015114969167-pat00031

Figure 112015114969167-pat00032

It can be seen that accuracy is improved when the adjusted coefficient is used as a result of calculating the radius of gust using this adjusted coefficient (see FIG. 3)

3 shows the relationship between the maximum wind speed and the estimated relaxation coefficient.

In Fig. 3, the blue solid line is the YOTC data, and the solid red line is the QSCAT data. Vertical error bars mean 95% confidence intervals.

FIG. 4 shows a comparison between the calculated value and the observed value of the strong wind radius algorithm using YOTC and QSCAT.

Using the calculated a, the gale radius (horizontal axis) produced by the algorithm and the gale radius (vertical axis) of the observed data were compared. The correlation coefficients of the two are shown at the upper left of the figure. The use of QSCAT data is slightly better than that of YOTC data.

Figure 5 shows the potential accuracy of the algorithm. Since the wind velocity structure of the typhoon is known from the observation (QSCAT) data, the gust wind radius and the observed gust wind radius produced by the algorithm are confirmed by the scatter diagram. The correlation coefficient between these two values is 0.96, indicating that the algorithm is potentially very accurate. However, the radius of the strong wind produced by the algorithm here is possible from the observation (QSCAT) to know the exact center position, the maximum wind speed radius, the maximum wind speed, and the relaxation coefficient. If the calculation accuracy of the center position, the maximum wind speed, and the maximum wind speed radius is decreased, the accuracy of calculating the gust wind radius is decreased.

In order to solve the problem of the above-mentioned algorithm, the following algorithm is proposed. If typhoons develop strongly in the vicinity of the center, a single exponential coefficient can not adequately represent the symmetric wind velocity structure of the typhoon, so a double exponential equation can be used to estimate a more accurate relaxation coefficient. First, the distance from the maximum wind speed radius can be redefined as follows.

Figure 112015114969167-pat00033

Using this, the symmetric wind velocity of typhoon can be defined as follows.

Figure 112015114969167-pat00034

This equation can be expressed in terms of two mitigation factors taking into account all of the rapidly increasing typhoons in the center.

Using the QSCAT data, the symmetric structure of the observed typhoon and the observed typhoon of the modeled typhoon were compared (see FIG. 5).

Figure 5 shows the QSCAT data for all hurricanes, weak typhoons, mid-storms, and strong typhoons and the symmetric wind speed using a double exponential equation.

Fig. 5 shows the result of calculating the figure of Fig. 1 in the same manner using the double exponential formula.

As a result of using two exponential expressions, the errors which are rapidly increasing in the vicinity of the existing center can be removed neatly. The green line represents the sum of the double exponents and is close to the observed value, the red line contributes to the first exponent, and the blue contributes to the second exponent.

As shown in FIG. 5, in the case of a weak typhoon, the contribution of the second index is small, but in the case of a large typhoon, its contribution is relatively large. Applying this algorithm is expected to improve the accuracy of typhoon wind radius algorithm.

On the other hand, since two exponential expressions must be used, the relaxation coefficient must also be calculated as two values. These two mitigation coefficients are modeled as follows. (See Fig. 6)

If the relaxation factor is two (

Figure 112015114969167-pat00035
), Respectively. As in the single exponential algorithm, each relaxation factor
Figure 112015114969167-pat00036
, And the result of each coefficient is the same. Since there are two mitigation factors
Figure 112015114969167-pat00037
Four coefficients of < / RTI >

The modeled relaxation factors are as follows.

Figure 112015114969167-pat00038

Figure 112015114969167-pat00039

here,

Figure 112015114969167-pat00040

to be.

In the present invention, QSCAT data is used as an observation value. There are many cases where the symmetric wind speed can be obtained because there is a wind field around the typhoon.

Figure 112015114969167-pat00041
To minimize
Figure 112015114969167-pat00042
and
Figure 112015114969167-pat00043
The goal is to find. Since this value can not be obtained by the analytic method, the numerical method was used. That is, if all possible values are substituted by the computer, the above values become minimum
Figure 112015114969167-pat00044
and
Figure 112015114969167-pat00045
Can be found. Since then,
Figure 112015114969167-pat00046
and
Figure 112015114969167-pat00047
Respectively
Figure 112015114969167-pat00048
Assuming a linear equation for the regression coefficient and constant
Figure 112015114969167-pat00049
,
Figure 112015114969167-pat00050
, And
Figure 112015114969167-pat00051
,
Figure 112015114969167-pat00052
to be.

A sample result of the estimated wind velocity algorithm using this algorithm is shown in Fig.

FIG. 7 shows the symmetrical gust fan radius and the QSCAT ground wind estimated from the strong wind and storm radius calculation algorithm according to the present invention.

As shown in Fig. 7, the calculated algorithm seems to be quite probable. Theoretically, this computed algorithm can be seen to be more accurate than the existing algorithm. This is because the error of the double exponential equation is smaller than that of the existing single exponential equation. In fact, using QSCAT data, we assumed the accuracy of the improved algorithm, assuming all the other output values were correct.

FIG. 8 shows the gust wind radius calculated by the improved algorithm and the gust wind radius of QSCAT.

Fig. 8 shows the accuracy of the gust radius calculated from the QSCAT data and the improved algorithm for the center of the typhoon, the maximum wind speed, and the maximum wind speed radius.

As shown in FIG. 8, the gust wind radius directly obtained from QSCAT has a correlation coefficient of about 0.96. This accuracy means the upper limit of the algorithm accuracy. In other words, to improve the accuracy of the algorithm, the center of the typhoon, the maximum wind speed, and the maximum wind speed radius estimation accuracy should be increased.

On the other hand, in consideration of the asymmetry of the strong wind radii, in the conventional algorithm, when the influence of the typhoon is calculated by the radius of the strong wind and the radius of the storm, the propagation direction of the typhoon is not considered.

When QSCAT is used to obtain the wind field around the typhoon and the wind field is rotated in the direction of the movement of the typhoon, it is concluded that the major cause of the asymmetry of the typhoon wind is asymmetry due to the movement of the typhoon. In other words, the direction of movement of the typhoon is strong on the right side and the wind on the left side is weak. This was used to calculate the asymmetric gust storm wind radius. Using the previously calculated hurricane symmetrical galeoid radius, we obtain a horizontally accurate east-west symmetric wind field. This wind field adds typhoon moving speed in a lump. Then, an asymmetric wind field is created. In this wind field, connecting a wind speed line such as 15m / s produces a strong wind radius including asymmetry.

To do this, we first try to compare the sea-wind structure and brightness temperature by considering the direction of the typhoon.

The typhoon center location provided by the RSMC (Best Regional Specialized Meteorological Center) best track was used to calculate the direction of the typhoon. The data used were the blackbody brightness temperature (TBB), which was extracted from the infrared image data of Chollian satellite for 6 hours. In addition, wind speed (WS) data observed from a satellite (Quick Scatterometer Satellite; QSCAT) was used. The method of calculating the direction of the typhoon progression for each case from the position of the center of the typhoon is as follows.

Using the center position of each case and the center position of the previous record, the tangent value of the direction based on the north side of the path of the typhoon, and the recorded central position and the central position immediately after the typhoon, The direction of the typhoon was defined as the average of tangent values in one direction. Then, using the calculated cosine and sine values, the traveling direction of each case was rotated so as to face the north direction (refer to FIGS. 9 and 10)

Fig. 9 shows a schematic diagram of a typhoon rotation.

Fig. 10 shows an example of typhoon rotation.

Satellite images were rotated with the direction of movement of the typhoon up and down, and a composite map was obtained.

11 shows the brightness temperature according to the traveling direction of the typhoon.

11 (a) is a synthesis diagram of the brightness temperature (2011-2013) of the typhoon with the traveling direction of the typhoon directed toward the north direction, (b) shows the front / rear structure of the typhoon traveling direction, Shows the left / right structure of the typhoon progression direction.

The asymmetry of the TBB structure appears along the left / right and front / back directions based on the direction of the typhoon. Although the temperature rise at the center of the typhoon does not appear due to the error of the positional information of the typhoon 's eye, the TBB at the center of the typhoon appears to be lower than that at the periphery of the typhoon. It can be seen that as the distance from the center portion increases, the temperature rise on the right side is stronger than the left side in the traveling direction, and the hardness of TBB is larger on the right side. Also, the asymmetry of the TBB appears before and after the traveling direction. The TBB hardness in the forward direction (forward direction) is larger and the TBB is higher than the rear (forward direction).

Fig. 12 shows the sea wind according to the traveling direction of the typhoon.

12 (b) shows the front / rear structure of the typhoon progression direction, and (c) shows the front / rear structure of the typhoon progression direction. Shows the left / right structure of the direction of the typhoon.

The offshore wind is relatively clear from the center of the left / right asymmetric structure of the direction of the typhoon. From the right side of the typhoon's progressive direction, the sea-side wind is stronger and the overall strong sea-level wind is shifted from the center to the right. The front and rear sea wind structures in the direction of travel are relatively symmetrical about the center.

Figure 13 shows the TBB according to the intensity of the typhoon.

To determine whether the structure and asymmetry of the typhoon are affected by typhoon intensity and stiffness, we calculated the degree of typhoon intensity and the degree of typhoon stiffness. Tropical Depression (TD), Tropical Storm (TS), Severe Tropical Storm (STS) and Typhoon (TY) cases were synthesized according to the strength classification of optimal path data provided by RSMC. As the intensity of the typhoon increases, the horizontal structure of the TBB is close to the circle, and the TBB of the center is lower. However, the asymmetry of the forward and backward directions of the typhoon is higher than that of the rear portion Structure.

The asymmetry of the left and right sides of the typhoon according to the strength of the typhoon is also different in degree as shown in Fig. 14, but the TBB of the right side is higher than that of the left side, and its hardness is stronger. The asymmetric structure of the typhoon seems to depend on the direction of the typhoon.

In most synthesized cases, the center of the typhoon is more north than 30, the circular structure weakens and the typhoon declines. As far as the intensity of the typhoon is maintained, the front and rear TBBs in the traveling direction do not significantly change with respect to the latitude value of the center position of the typhoon, and all the TBBs have an asymmetric structure. Comparing the left and right TBBs in the direction of the typhoon progression, the structure also maintains a higher TBB on the right side of the travel direction regardless of the latitude value of the center position (see FIGS. 15A and 15B).

Unlike the TBB results, the offshore winds tend to be relatively obscured when the center of the typhoon is located to the south of 15, and the strongest part of the typhoon is located in the 20- It is time to reach 25. The front and rear sea wind structures in the direction of the hurricane are symmetrical, and the maximum velocity of the sea wind is located at the center. On the other hand, the asymmetry of the left / In other words, it seems that the traveling direction rather than the latitude value of the center position predominantly influences the horizontal asymmetry of the sea wind (see Figs. 16A and 16B).

When the center of the typhoon is located at 120-140, the TBB at the center of the typhoon appears to be the lowest, the typhoon has the strongest intensity, and the horizontal structure is close to the circular shape. As the distance increases from the lowest TBB value in the center of the typhoon to the right side in the direction of travel, the asymmetry in which the TBB is higher appears as a whole regardless of the central hardness value. The asymmetry of the forward and backward TBB in the direction of the heading is most evident in the typhoon belonging to the hardness 120-140, which is stronger than the hardness 100-120 and the hardness 140-160, which indicates the typhoons of relatively weak intensity. (See Fig. 17).

Fig. 14 shows the TBB composition and the left / right structure of the progress direction according to the intensity of the typhoon.

FIGS. 15A and 15B show the front and rear left and right structures of the TBB composition and the traveling direction according to the latitude value at the center of the typhoon.

FIGS. 16A and 16B show the front wind direction and the left wind direction and the right wind direction, respectively, of the sea wind composition and the traveling direction according to the latitude value of the typhoon center.

FIG. 17 shows the TBB composition and the left / right structure before and after the direction of the progress of the typhoon according to the hardness value of the typhoon.

Fig. 18 shows the front wind direction and the left wind direction and the right wind direction of the wind direction in accordance with the hardness value of the typhoon center.

Fig. 19 shows (a) an improved algorithm and (b) a previous algorithm of the gust factor radius calculated by WINDSAT and the calculated gust curve radius by an algorithm. Here, WINDSAT is a sensor for measuring sea level wind direction and wind speed of Coriolis satellite.

The sea wind wind speed at the center of the typhoon is also highest when the center of the typhoon is located at the hardness of 120-140, that is, the typhoon has the strongest strength and the horizontal structure is close to the circular shape. The structural asymmetry in which the composition is incomplete due to the lack of the sample case of the typhoon in the 100-120 degree of hardness but the sea air is stronger in the direction of the right side than the left direction appears in all three sections. Unlike the case in which the maximum velocity of the sea wind is deviated to the right side of the traveling direction, the front and rear portions of the traveling direction are symmetrical, and the result of the entire composite also agrees with the result. The structural asymmetry of left / right and front / rear of sea-wind is not influenced by the location of center of typhoon like TBB, that is, the direction of typhoon is most influenced by the wind / . (See Fig. 18)

We verified the improved algorithm using WINDSAT satellite data. From 2011 to 2013, all data were interpolated into time-series data to find a total of 107 cases where the typhoon passed at the same time. The symmetric components were calculated based on the center position (SDT) created by the satellite center, and the maximum wind speed, the maximum wind speed radius, the strong wind radius, and the storm radius were obtained. In addition, the improved algorithm was applied to the Chollian satellite data to calculate the gust radius and the storm radius for 107 cases. The results are shown in Fig.

Fig. 19 (a) shows the variance of the gust wind radii calculated by WINDSAT and the algorithm, and Fig. 19 (b) shows the results calculated by the previous algorithm.

The output value of the improved algorithm is improved compared to the previous algorithm. The calculated values are 91, and for the 91 probability samples, if the correlation coefficient is more than 0.17, the improved algorithm shows statistically significant results because it is significant at the 95% confidence level by the Student t-test.

FIG. 20 shows the distribution of the gust winds calculated by WINDSAT and the gust wind radii calculated by the algorithm.

20 is the same as that shown in Fig. 19 except for the storm radius, (a) shows that it is calculated by the improved algorithm, and (b) shows that it is calculated by the previous algorithm.

Referring to FIG. 20, the improved algorithm also shows improved results for the storm radius, and the storm radius shows statistically significant results. The overall low correlation is due to the large error in the center position of the WINDSAT data, and the symmetric wind speed in each case is very noisy. On the other hand, the maximum wind speed calculated from WINDSAT and the maximum wind speed of RSMC optimum path data are somewhat different. For 91 cases, the correlation coefficient is 0.48, which is somewhat low.

In order to increase the accuracy of the wind radius and storm radius calculation, the accuracy of the typhoon center position and the maximum wind speed should be improved. If these two parameters are very accurate, the accuracy of the strong wind radius can have a correlation coefficient of 0.96 as a correlation coefficient.

FIG. 21 is a block diagram showing a configuration of an apparatus for calculating a strong wind and a storm radius of a typhoon using the Chollian satellite data according to the present invention.

The apparatus shown in Fig. 21 includes an ADT 202, a symmetrical wind speed section 204, an asymmetric wind speed section 206, and an information display section 208.

The ADT 202 analyzes the infrared satellite data 210 to calculate the center and intensity of the typhoon.

The symmetrical wind speed section 204 calculates a relaxation coefficient, a first wind speed radius, a symmetrical strong wind radius and a symmetrical storm radius.

The asymmetric wind speed section 206 calculates the moving speed and the asymmetric wind speed of the typhoon.

The information display section 208 displays the sea wind.

In the symmetrical wind speed section 204, the radius of symmetrical strong wind and the radius of symmetrical storm are calculated using the center position and strength provided to the ADT 202. Since the intensity is known, the relaxation coefficient is calculated by substituting the relaxation coefficient into the relaxation coefficient calculation formula, and the maximum wind speed radius is calculated by applying the satellite image to the maximum wind speed radius calculation formula. The parameters for calculating the wind / storm radius are the maximum wind speed, the maximum wind speed (intensity), and the relaxation coefficient, so all of them are used to calculate the symmetrical wind / storm radius.

First, the distance from the maximum wind speed radius can be redefined as follows.

Figure 112015114969167-pat00053

Using this, the symmetric wind velocity of typhoon can be defined as follows.

Figure 112015114969167-pat00054

This equation can be expressed in terms of two mitigation factors taking into account all of the rapidly increasing typhoons in the center.

If the relaxation factor is two (

Figure 112015114969167-pat00055
), Respectively. As in the single exponential algorithm, each relaxation factor
Figure 112015114969167-pat00056
, And the result of each coefficient is the same. Since there are two mitigation factors
Figure 112015114969167-pat00057
Four coefficients of < / RTI >

The modeled relaxation factors are as follows.

Figure 112015114969167-pat00058

Figure 112015114969167-pat00059

here,

Figure 112015114969167-pat00060

to be.

In the present invention, QSCAT data is used as an observation value. There are many cases where the symmetric wind speed can be obtained because there is a wind field around the typhoon.

Figure 112015114969167-pat00061
To minimize
Figure 112015114969167-pat00062
and
Figure 112015114969167-pat00063
The goal is to find. Since this value can not be obtained by the analytic method, the numerical method was used. That is, if all possible values are substituted by the computer, the above values become minimum
Figure 112015114969167-pat00064
and
Figure 112015114969167-pat00065
Can be found. Since then,
Figure 112015114969167-pat00066
and
Figure 112015114969167-pat00067
For each
Figure 112015114969167-pat00068
Assuming a linear equation for the regression coefficient and constant
Figure 112015114969167-pat00069
,
Figure 112015114969167-pat00070
, And
Figure 112015114969167-pat00071
,
Figure 112015114969167-pat00072
to be.

In the asymmetric wind speed section 206, an asymmetric wind field is generated using the strong wind / storm radius provided in the symmetrical wind speed section 204, and the asymmetric wind / storm radius is calculated using the asymmetric wind field.

For this purpose, the center position of the typhoon calculated by the ADT 202 is used. This is because the velocity of the typhoon is calculated by dividing the observation time interval at the distance where the center position is moved. The asymmetric wind field is calculated by adding the moving speed of the typhoon to the symmetrical wind field, and the asymmetric wind / storm radius is calculated using this.

The information display unit 208 displays the calculated strong wind / storm radius using web-based typhoon analysis system software. First, numerical wind / storm radii produced are output to the screen using a graphic processing module. If there is a polar orbit satellite sea wind data, a sea wind wind field is displayed on the indicated gale / storm radius for comparison .

202 ... ADT (ADT) 204 ... Symmetrical wind speed section
206 ... asymmetric wind speed section 208 ... information display section

Claims (5)

A Method for Calculating Strong Wind and Storm Radius of Typhoon Using Chollian Satellite Data
A process of defining the symmetric wind speed V (r ') of the typhoon by the following equation;
Figure 112015114969167-pat00073

Here, r 'is a distance from the maximum wind speed radius V MAX
Figure 112015114969167-pat00074
ego
r is the distance from the typhoon center
R MAX is the maximum wind speed radius
a1 and a2 are the relaxation coefficients
Figure 112015114969167-pat00075

Figure 112015114969167-pat00076

Modeling the two mitigation coefficients a1 and a2 through the quasi-satellite data; And
Calculating a strong wind and a storm radius using the two relaxation factors a1 and a2;
And calculating a storm radius and a strong wind intensity of the typhoon using the quill satellite data.
2. The method of claim 1, wherein modeling the two relaxation coefficients a1 and a2 comprises:
Using the QSCAT (Quick Scatterometer) data as observations,
Figure 112015114969167-pat00077
Lt; RTI ID = 0.0 >
Figure 112015114969167-pat00078
and
Figure 112015114969167-pat00079
A method for calculating a strong wind and a storm radius of a typhoon using Chollian satellite data.
3. The method of claim 2,
The numerical method, i.e., substituting all possible values,
Figure 112015114969167-pat00080
Lt; RTI ID = 0.0 >
Figure 112015114969167-pat00081
and
Figure 112015114969167-pat00082
Lt; RTI ID = 0.0 > e < / RTI >
Figure 112015114969167-pat00083
and
Figure 112015114969167-pat00084
Respectively
Figure 112015114969167-pat00085
, And that finding a regression coefficient and a constant
Figure 112015114969167-pat00086
,
Figure 112015114969167-pat00087
, And
Figure 112015114969167-pat00088
,
Figure 112015114969167-pat00089
A method for calculating a strong wind and a storm radius of a typhoon using the satellite data.
The method as claimed in claim 1, wherein the asymmetric wind field is created by obtaining a symmetrical wind field using the storm radius of the calculated typhoon and collectively adding the typhoon moving speed to the symmetrical wind field, And calculating the storm radius including the asymmetry by connecting the line to the calculated storm radius of the typhoon.
The method as claimed in claim 1, wherein the asymmetric wind field is created by obtaining a symmetrical wind field using the radius of strong wind of the calculated typhoon and adding the typhoon moving speed to the symmetrical wind field collectively, And calculating a gale radius including asymmetry by connecting the gullwing lines and the gullwing radius of the typhoon.
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