## 3 Results
Warm SST indicates the potential for low-pressure systems to form. Figure 2a-d depict the horizontal distributions of SST climatology (1982-2011) and anomalies (\({}^{\circ}\)C) over the NIO region during 1992-2001, 2002-2011, and 2012-2021, respectively. Figure 2b-d depict the horizontal distribution of SST (\({}^{\circ}\)C) anomalies over the NIO region during 1992-2001, 2002-2011, and 2012-2021, respectively. Figure 2a shows a negative anomaly, indicating cooling during the post-monsoon period of the first decade (1992-2001), except in the region of the East Indian Ocean, which shows a positive anomaly. Figure 2b shows a negative anomaly, indicating cooling during the post-monsoon period of the first decade (1992-2001), except in the region of the East Indian Ocean, which shows a positive anomaly. In the second-decadal years, a clear signature of moderate warming environments during 2002-2011 was observed, as compared to 1992-2001. However, the highly positive SST anomaly shows extreme conditions in 2012-2021. In brief, the lower region (south of 10\({}^{\circ}\) S and west of 80\({}^{\circ}\) E) in Figure 2d shows extreme heating conditions, while Figure 2b shows contrasting conditions. After originating over the warm ocean surface, tropical cyclonic disturbances can grow into TCs by inducing upward transport of heat fluxes that are positively related to surface wind speeds [7]. The supply of surface heat fluxes, including both sensible heat (SHX) and latent heat (LHX), is identified as the energy source for the intensification of TCs [33]. From an energetic perspective, the storm extracts latent energy from the underlying ocean via LHX, increasing the available potential energy. By releasing latent energy in convective clouds, a portion of the latent heat release acts to increase the kinetic energy through an inefficient conversion [33]. Hence, LHX is the fundamental energy source for TC intensification. SHX, however, is not directly involved in the energy conversion processes. From a magnitude perspective, SHX is usually several  
Figure 2: **(a)** SST climatology and SST anomaly for three decades: **(b)** 1992–2001, **(c)** 2002–2011, and **(d)** 2012–2021 [1982–2011 climatology used for anomaly]. times smaller than LHX and is generally believed to be much less important than LHX in determining TC development (e.g., [34; 35]). Without the supply of LHX from the ocean, the storm weakens and shrinks rapidly, and its maximum surface winds are reduced to less than 33 m/s within 24 h, leading to a continuous decrease in kinetic energy. The latent heat flux (LHF) is, therefore, indicated to be the dominant energy source for TC intensification, whereas SHX is not. Climatologically, LHF has increased in the western parts of the AS and BoB (Figure S1a). On average, LHF increased linearly over the AS from 1992 to 2021 (Figure S1). The increase in LHF shows enhanced cloud formation and possibly increased precipitation in recent decades (2011-2021) over the AS compared to BoB (Figure S1d) and other decades (Figure S1b,c). Meanwhile, climatologically, it showed an increase in both the AS and BoB. It is clear from Figure 3 that positive SST anomalies persisted over the IOD region, as described by [PERSON] et al. [36]. There is a difference in the SST anomaly between the western (50-70\({}^{\circ}\) E, 10\({}^{\circ}\) S-10\({}^{\circ}\) N) and southeastern (90-110\({}^{\circ}\) E, 10\({}^{\circ}\) S-Equator) called IOD region of the tropical Indian Ocean, AS (55-75\({}^{\circ}\) E; 5-20\({}^{\circ}\) N), BoB (80-100\({}^{\circ}\) E; 5-20\({}^{\circ}\) N), and EEIO (80.5-103.5\({}^{\circ}\) E and 6.5\({}^{\circ}\) S-3.5\({}^{\circ}\) N) sub-regions of the Indian Ocean during the OND season of 1992-2021. Among all the graphs, AS shows a dramatic change from the lowest temperature from 1990 to recent years. The increase in SST can pump more moisture into TC formation from the Indian Oceanic region.