Overcoming the limitations of traditional single-factor positioning, this method employs a dual-verification approach―combining the minimum sea-level pressure with the maximum relative vorticity at 850 hPa―to locate the typhoon center, thereby avoiding manual positioning errors (Toyoda et al., 2025); Simultaneously, environmental field parameters are calculated using a circular zone with a latitudinal and longitudinal radius of 3˚ - 7˚ around the typhoon center, completely eliminating interference from the typhoon’s own circulation (Oh et al., 2015). This approach aligns with the precise paradigm for analyzing the environmental field of tropical cyclones and resolves the issue of diagnostic distortion in the environmental field caused by traditional methods (Ford & Kench, 2016).

{ P s ( x 0 , y 0 ) = min { P s ( x , y ) } , ( x , y ) ∈ D                                                           ( 1 ) ε 850 ( x 0 , y 0 ) = max { ε 850 ( x , y ) } , ( x , y ) ∈ D                                                           ( 2 ) P s ( x 0 , y 0 ) ≤ 1000 h P a                                                           ( 3 )

Equation (1) P s is sea-level pressure (hPa); ε 850 is the relative vorticity at 850 hPa (10⁻⁵∙s⁻¹); D is the typhoon search area; and ( x 0 , y 0 ) are the coordinates of the typhoon’s center.

Interpolate the wind field from the Cartesian coordinate system to the cylindrical coordinate system (r, θ, p), accurately decomposing the tangential wind, radial wind, and vertical motion; the interpolation method used is bilinear interpolation, with a radial resolution of 10 km and an azimuthal resolution of 10˚. The tangential wind ( V t ) and radial wind ( V r ) in the cylindrical coordinate system are calculated using the following formulas:

V t = − u sin θ + v cos θ (4)

V r = v sin θ + u cos θ (5)

In Equation (4), the radial wind is negative when it flows towards the center. The vertical velocity (ω, unit: hPa∙s⁻¹) is directly taken from ERA5, and the ascending motion is negative.

For the first time, a daily quantitative statistics was conducted in the core area of the eye wall ranging from 70 to 100 kilometers. This enabled a clear identification of the coupling relationship between wind field sudden changes and intensity bursts, compensating for the previous lack of comprehensive wind field analysis and the neglect of the key core area.

Break through the limitations of single dynamic field or thermal field analysis, conduct vertical layer-by-layer coupling analysis of vorticity, divergence, warm core, and humidity, reveal the “cooperative enhancement mechanism of mid-low level dynamic driving and mid-high level thermal support”, and clearly depict the three-dimensional physical process of rapid typhoon intensification (Ford & Kench, 2014).

The guiding airflow of the entire layer is calculated by weighting the 500 hPa and 850 hPa data equally. The environmental vertical wind shear is defined as the difference in the horizontal wind vectors between 200 hPa and 850 hPa. The calculation formula is:

V shear = ( u 200 ¯ − u 850 ¯ ) 2 + ( v 200 ¯ − v 850 ¯ ) 2 (6)

In Equation (6), u ¯ and v ¯ represent the area-averaged meridional wind and zonal wind within a circular area of 3˚ to 7˚ latitude distance from the center of the typhoon. This definition can shield the influence of strong winds in the typhoon core on the estimation of shear. By combining the analysis of multiple systems of the subtropical high, continental high, and South Asian high circulation, it accurately explains the cause of the stable westward path of “Yagi”, solving the problem that traditional single-layer guiding airflow analysis cannot explain the absolute control of the path.

By integrating satellite cloud top temperature data, radar radial velocity data, ground observations and reanalysis data, and using the cross-validation method to verify the analysis results of typhoon intensity, structure and path, the reliability of the conclusions is enhanced.

1) Cross-validation of typhoon path: Average path error

APE = 1 N ∑ i = 1 N arccos [ sin φ i sin φ ′ i + cos φ i cos φ ′ i cos ( λ i − λ ′ i ) ] ⋅ R (7)

In the equation, APE represents the average path error (km); φ, λ are the longitude and latitude of the optimal path; φ', λ' are the paths from reanalysis/inversion; R = 6371 km is the radius of the Earth; N is the number of samples.

2) Cross-validation of typhoon intensity: Mean absolute error and root mean square error

MAE = 1 N ∑ i = 1 N | V max , i − V ′ max , i | (8)

RMSE = 1 N ∑ i = 1 N ( V max , i − V ′ max , i ) 2 (9)

In Equation (8), V max represents the maximum wind speed of the optimal path; V ′ max represents the wind speed derived from radar/satellite measurements.

3) Cross-validation of typhoon structure parameters: Coefficient of consistency

IOA = 1 − ∑ i = 1 N ( X i − X ^ i ) 2 ∑ i = 1 N ( | X i − X ¯ | + | X ^ i − X ¯ | ) 2 (10)

In Equation (10), X represents the observed or actual structural parameters (vorticity, divergence, tangential wind); X ^ represents the simulated values from reanalysis data; IOA ∈ [0, 1], the closer it is to 1, the better the consistency.

The aforementioned innovative method has achieved a leap from “two-dimensional qualitative” to “three-dimensional quantitative”, and from “single-field analysis” to “coupled diagnosis”. This is the core guarantee for this paper to reveal the extreme enhancement mechanism and path causes of “Yagi”.

During the super typhoon stage (from 06:00 on September 5th to 22:00 on September 6^th), “Yagi” exhibited a vertical configuration of strong positive vorticity in the middle and lower levels and weak negative vorticity in the upper levels: the relative vorticity center value at 850 hPa reached 12 to 15 × 10⁻⁵∙s⁻¹, significantly higher than the threshold of an ordinary typhoon; at 500 hPa, it maintained 8 to 10 × 10⁻⁵∙s⁻¹ positive vorticity, and at 200 hPa, it changed to −1 to −2 × 10⁻⁵∙s⁻¹ weak negative vorticity, forming a continuous cyclonic rotational suction effect.

The divergence field presented a coupled characteristic of strong convergence in the lower levels and strong divergence in the upper levels: the convergence center

value at 850 hPa reached −6 to −8 × 10⁻⁵∙s⁻¹, and the divergence center at 200 hPa reached 8 to 10 × 10⁻⁵∙s⁻¹ in Figure 1. Moreover, the divergence range in the upper levels was larger than the convergence area in the lower levels, significantly enhancing the vertical upward movement. This dynamic configuration was the core driving force for the typhoon to complete the four-level consecutive jumps from “strong tropical storm” to “super typhoon” within 15 hours.

The satellite cloud in Figure 2 shows that during this stage, the eye area of the typhoon is clear, and the spiral cloud system is compact, which is highly consistent with the symmetrical distribution of the vorticity field.

From 08:00 to 16:00 on September 6^th (before landing in Wenchang, Hainan), the value of the low-level convergence center at 850 hPa reached −6 to −8 × 10⁻⁵∙s⁻¹ (negative divergence). The convergence area almost completely overlapped with the vorticity center. Figure 3 shows that the rotational airflow and the convergent airflow were highly coupled, and a large amount of warm and humid air was drawn into the core area of the typhoon.

Meanwhile, at the 200 hPa level, there is a strong divergence center with a rate of 8 - 10 × 10⁻⁵∙s⁻¹, and the divergence area is slightly larger than the convergence area at the lower level (with a coverage radius of approximately 6 degrees of latitude). This “strong divergence in the upper layer compared to the convergence in the lower layer” configuration further enhances the suction effect of vertical upward movement, causing the vertical velocity in the eye wall area to reach its peak on September 6^th. Within the typhoon eye area (with a diameter of 20 - 30 km), there is a weak divergence zone, corresponding to the descending air flow, which is consistent with the observed fact of “brief clear sky in the eye area” when the typhoon made landfall in Wenchang.

The thermal structure is one of the core internal driving factors for the maintenance and intensification of typhoons. Especially during the three rapid intensification processes of “Yagi”, the coordinated evolution of the warm core structure and humidity field exhibited significant asymmetry and vertical stratification characteristics. The horizontal distribution of temperature at various pressure levels extracted based on ERA5 reanalysis data (Figures 4(a)-(g)) shows that “Yagi” presented a typical thermal configuration of “warm core in the middle and upper levels, weak warmth in the lower levels, and cold cover in the upper levels” during the super typhoon stage (from 06:00 on September 5^th to 22:00 on September 6^th).

From the distribution of temperature anomalies in each pressure layer (Figures 4(a)-(g)), it can be seen that the warm core structure of “Yagi” is most prominent in the 300 - 500 hPa layer, with positive temperature anomalies generally reaching 3 - 6 K. In some areas of Figure 4(d), the temperature even exceeds 6 K at the 500 hPa layer. This layer overlaps with the main height layer of latent heat release, indicating that the latent heat released by water vapor condensation is the main heat source for maintaining the warm core. In contrast, the positive temperature anomalies in the lower layer (850 - 600 hPa) are only 1 - 3 K (Figures 4(e)-(g)), and the horizontal gradient is weak, reflecting that the thermal response in the lower layer mainly relies on the turbulent heat flux in the boundary layer and the sea-air exchange process. Figure 4(a) shows that the intensity of the warm core at the 200 hPa level significantly weakens but can still be identified, indicating that the vertical development height of the typhoon is relatively high, and the “cold cap” structure at the top of the convection has not been completely destroyed.

It is worth noting that the horizontal distribution of the warm core shows an approximately concentric circular structure. The maximum temperature value of the center is located in the typhoon eye area, and the temperature rapidly decreases with the increase in radius. Especially near the 500 hPa layer, the temperature gradient between the eye area and the eye wall is the steepest, and the

thermal contrast is the most intense. This structure reaches its peak on September 6 at 12:00, corresponding to the peak intensity of the typhoon (68 m∙s⁻¹). In addition, the center of the warm core has a slight tilt in the vertical direction, which may be related to a slight increase in environmental vertical wind shear around 6 days ago, but the overall tilt amplitude is limited and has not caused a significant separation between the thermal center and the circulation center.

Based on the analysis of the relative humidity fields in each pressure layer (Figures 5(a)-(g)), the humidity distribution of “Yagi” presents a typical spiral band structure. The high-humidity areas (RH > 80%) are mainly concentrated in the eye wall and the peripheral spiral rainband region, which is highly consistent with the typhoon circulation pattern. Figure 5(g) shows that the relative humidity at the lower level of 850 hPa is relatively low, indicating that dry air is being drawn in from the periphery of the typhoon. This dry-wet alternating spiral band is

particularly obvious in the 500 - 700 hPa layer (Figures 5(d)-(f)), and may have a local inhibitory effect on the convective activity of the eye wall.

At the upper level of 200 hPa, the relative humidity in the eye wall area shown in Figure 6(a) is close to saturation (RH > 95%), indicating that the water vapor in the upper outflow layer is abundant, which is conducive to the maintenance of radiative cooling and latent heat release. The relative humidity at the middle layer of 500 hPa remains between 70% and 85% (Figure 5(d)), providing good water vapor conditions for the development of deep convection. Overall, the intrusion of dry air mainly occurs in the peripheral area of the lower layer, and has not significantly disrupted the core warm center structure, but its modulation effect on the convective activity of the typhoon periphery is worthy of attention.

By comparing the thermal parameters and intensity changes in the eye wall area (70 - 100 km from the center), it can be known that the intensity and vertical extension height of the thermal structure of “Yagi” are positively correlated with the maximum wind speed at the center. Starting from 06:00 on September 5^th, the intensity of the warm center in the 300 - 500 hPa layer continued to increase, reaching its peak by 12:00 on September 6^th, and then the typhoon entered the Beibu Gulf and entered a re-enhancement stage on September 7^th. Although Figure (c) shows that the latent heat flux increased again, the intensity of the warm center did not return to the peak level, indicating that the recovery of the thermal structure lagged behind the enhancement of the ocean heat flux.

In addition, the weak inversion zone (maximum temperature layer) in the 300 - 400 hPa layer (temperature maximum layer) indicates the direct manifestation of the concentrated release of latent heat. The existence of this layer significantly reduces the vertical temperature gradient at the center of the typhoon, enhances the overall static stability of the air column, and is conducive to the maintenance and further strengthening of the low-pressure center. This feature is most prominent from 08 to 16:00 on September 6^th, which is consistent with the peak intensity height before the typhoon landed in Wenchang, Hainan.

Taking the instantaneous center of the typhoon as the origin, interpolate the Cartesian coordinate grid points to the cylindrical coordinate system (r, θ, p), decompose the tangential wind, radial wind, and extract the vertical velocity. Select the 850 hPa layer in the eye wall area (70 - 100 km from the center), and statistically calculate the key dynamic parameters at 12:00 every day from September 1^st to 9^th as shown in Table 1.

Select the eye wall area at the 850 hPa level (70 - 100 km from the center), and statistically analyze the key dynamic parameters from September 1st to 9^th (negative radial wind indicates inflow, negative vertical velocity indicates upward movement). The results show that the typhoon underwent a complete “development - peak - decay” process. From September 1^st to 2^nd, it was a strong tropical storm, and on the 3^rd, it rapidly intensified to a strong typhoon and maintained this intensity until the 7^th. From the 5^th to the 6^th, it reached its peak intensity, and after landing on the 8^th, it rapidly weakened to below the tropical storm level. The tangential wind speed continuously increased from 21.66 m∙s⁻¹ on September 1st to 43.45 m∙s⁻¹ on the 6^th, and the rotational kinetic energy continuously accumulated; the maximum inflow wind speed reached a peak of −13.36 m∙s⁻¹ on the 6^th, and the intensity of low-level convergence reached its maximum; the negative vertical velocity range was the largest from the 5^th to the 6^th, and the upward movement was the most intense. During the strong typhoon stage, the environmental wind shear remained at a low value, the typhoon structure was symmetrical, and it was conducive to energy concentration.

Analysis of the three-dimensional structure characteristics of the wind field reveals that the maximum tangential wind speed increased continuously from 21.66 m∙s⁻¹ on September 1 to 43.45 m∙s⁻¹ on September 6, and the average tangential wind speed also rose from 13.19 m∙s⁻¹ to 34.52 m∙s⁻¹, indicating that the rotational kinetic energy of the typhoon was continuously accumulating. From September 5 to 6, it was the peak intensity period. Figure 6 shows that the tangential wind speed remained above 40 m∙s⁻¹.

The radial inflow velocity reached its peak on September 6^th at −13.36 m∙s⁻¹ (negative value indicates inflow), with an average radial wind speed of −1.74 m∙s⁻¹, indicating that the low-level convergence was the strongest on that day. The intense convergence transported warm and humid air to the eye wall, providing “fuel” for latent heat release. After September 3rd, the typhoon area changed from divergence to convergence, marking the establishment of the secondary circulation.

The range of vertical velocity (negative value indicates ascent) reached its maximum on September 5 - 6 (−0.0403 to −0.0048 hPa∙s⁻¹), with the most intense ascending motion. The eye wall area was dominated by ascent, while the eye area had weak descent (Figure 7), forming the typical dynamic structure of a mature typhoon. During the entire strong typhoon stage, the environmental vertical wind shear was very small, which was conducive to the maintenance of the axisymmetric structure.

At 12:00 on September 6^th, the center of the typhoon was located at 110.00˚E, 20.00˚N, reaching its peak intensity. The low-level easterly jet stream is obvious, and the radial profile in Figure 7 shows that the tangential wind, radial wind and

vertical velocity undergo sudden changes at a distance of about 65 km from the center. This precisely locates the eye wall position. At this time, strong convergence at the lower level, intense upward movement of the eye wall, and strong divergence at the upper level form an efficient heat engine cycle. Combined with very small vertical wind shear and warm sea temperature, they jointly support an extreme intensity of 68 m∙s⁻¹.

To quantitatively analyze the dominant role of the environmental airflow on the path of “Yagi”, the entire-layer guiding airflow within a 3˚ to 7˚ latitude and longitude range around the typhoon center at 850 to 100 hPa was calculated. The results show that after September 4^th, the direction of the typhoon's movement was consistent with the height of the entire-layer guiding airflow, and the vertical weight of the guiding airflow was biased towards the upper levels (500 to 300 hPa), which is related to the strong intensity and high development height of the typhoon.

As can be seen from Table 2, throughout the entire lifecycle of the typhoon, the weighted guiding airflow direction at 500 hPa and 850 hPa was consistently east wind, which was in perfect agreement with the actual movement direction of the typhoon (northwest to west-northwest to southwest to west-southwest). The weighted guiding wind speed reached 8.45 m∙s⁻¹ and 7.47 m∙s⁻¹ during the peak period from September 5^th to 6^th, which was the strongest period.

The stability of the guiding airflow, the continuous energy supply from the warm sea temperature, and the weak terrain interference jointly contributed to

the “Yagi” typhoon’s unchanging westward path.

Based on the analysis of the experimental results, the core causes of the path stability can be deduced:

・ Guiding airflow dominance: The convergence of the easterly airflow on the south side of the subtropical high and the westward airflow on the south side of the continental high locks in the westward path;

・ Sea temperature support: The SST in the northern part of the South China Sea exceeds the 26.5˚C threshold (as Figure 8 shows), and the thickness of the

warm water layer exceeds 50 meters, maintaining the high intensity and structural stability of the typhoon;

・ Terrain influence is limited: The terrain of Luzon Island only causes a brief deceleration and a slight northward deviation, and after entering the South China Sea, it quickly resumes the positive westward path;

・ Cold air assistance: The strengthening of the weak cold air from the north enhances the low-level convergence, strengthens the typhoon structure, and further stabilizes the path.

The optimal vertical configuration of thermal-hydraulic coupling is the extreme explosive enhancement mechanism of the “Yagi” core. The synergy of strong positive vorticity in the middle and lower layers and weak negative vorticity in the upper layer, as well as strong convergence in the lower layer and strong divergence in the upper layer, drives the development of efficient secondary circulation and supports the rapid consecutive intensification of the typhoon;

The core area of warming at 300 - 500 hPa and the spiral humidity distribution form a stable thermal support. The intensity of the warm core, the evolution of the eye wall wind field, and the intensity burst of the typhoon show a high positive correlation, and it is a key indicator for the early warning of extremely strong typhoons in the South China Sea in autumn;

The eastward guiding airflow superimposed by the subtropical high and the continental high has absolute control over the path of “Yagi”. The abnormal high sea surface temperature in the South China Sea and weak vertical wind shear jointly ensure the stability of the typhoon structure and the long-term maintenance of extremely strong intensity.

The final answers to the three scientific questions raised in this article are as follows:

・ Scientific Question 1: During the rapid intensification of “Yagi”, the dynamic field shows a “lower positive and upper negative” vorticity configuration and a “lower convergence and upper dispersion” divergence configuration. The thermal field has a stratified structure of “strong warm center in the middle and upper layers, weak warm in the lower layers”, and the vertical coupling driving intensity has erupted;

・ Scientific Question 2: In the core area of the eye wall from 70 to 100 km, the tangential wind, radial inflow, and vertical movement reach synchronous peak values, which is highly coupled with the intensity evolution, and is the core feature of the internal core power response of the typhoon;

・ Scientific Question 3: The weighted easterly wind from the middle and upper layers dominates absolutely. The subtropical high and the continental high lock the path together, while the terrain and cold air only play a minor adjusting role.

The core innovation of this paper lies in the construction of a framework integrating dynamics and thermodynamics, three-dimensional wind field decomposition, and integrated analysis of the entire layer of guiding airflow, which enables a systematic analysis of the mechanism of extremely strong typhoons in the South China Sea, quantitatively characterizing the evolution of the wind field in the eye wall core area, and filling the gap in the diagnostic scale of the core of extremely strong typhoons in the South China Sea during autumn.

Future research can be conducted along the following directions: 1) Conduct a comparative energy budget analysis of “Yagi” and similar historical typhoons (such as “Wesmas” and “Squirrel”); 2) Utilize high-resolution large-eddy simulation (LES) to reveal the mesoscale processes between the eye wall convective burst and the kinetic energy generation term; 3) Develop an objective forecast model for typhoon intensity based on the combination of fractal dimension and deep learning. These efforts will help further enhance the forecasting capabilities of typhoons in the South China Sea, especially those that rapidly intensify, and provide more solid scientific support for disaster prevention and mitigation.