The RWP observations collected from 31 stations across China (Fig. 1) from April to October in 2023–2024 were analyzed in this study, which can provide wind speed and direction with a vertical resolution of 120 m and an interval of 6 min (Liu et al., 2019). To reduce the potential influence of poor data quality, RWP data underwent strict quality control following procedures proposed by Wei et al. (2014) and Miao et al. (2018). Firstly, to minimize contamination from precipitation particles, which can introduce significant errors in Doppler-based wind retrieval, all observations during rainfall periods were removed. Secondly, within each profile below 3 km above ground level (a.g.l.), missing values and significant outliers that were defined as values exceeding 2.5 standard deviations from the mean were removed. Next, for each profile, if more than 40 % of the data points below 3 km a.g.l. were outliers or missing, that entire profile was discarded. Finally, discontinuous, or missing data points were estimated using linear interpolation. Following this quality control process, 109 400 wind profiles were discarded and a total of 2 606 042 profiles across China were available for analysis during the study period.

In addition, 1-min rainfall measurements were directly acquired from the rain gauge measurements at 2160 national weather stations across China to identify rainfall events. Rainfall amounts were accumulated over 6-min intervals to ensure temporal alignment with the RWP measurements. Ground-based meteorological variables are measured at 1-min intervals from national weather stations, including 2-m air temperature, relative humidity, and surface pressure. All ground-based data have undergone rigorous quality control (China Meteorological Administration, 2020; Zhao et al., 2024) and are publicly accessible at the National Meteorological Information Center of China Meteorological Administration (CMA).

Furthermore, to diagnose large-scale circulation patterns and environmental conditions preceding nocturnal rainfall influenced by LLJs, this study utilized meteorological variables derived from the fifth generation of the European Centre for Medium-Range Weather Forecasts atmospheric reanalysis (ERA5) of the global climate (Hersbach et al., 2023). The ERA5 data features a horizontal resolution of 0.25° × 0.25° across 37 vertical pressure levels and hourly temporal resolution. Unless otherwise specified, all datasets cover the study period of April to October in 2023–2024.

Firstly, days with typhoon activity were excluded. To minimize the impact of rainfall on RWP measurements, a minimum dry interval of 2 h was required between consecutive rainfall events. Following the methodology of Li et al. (2024), a rainfall occurrence was defined when the accumulated rainfall measured by all rain gauges within a 25-km radius of each RWP station exceeded 0.1 mm. To account for rainfall intermittency and filter out transient noise, a valid rainfall event required the initial detection to be followed by at least two subsequent occurrences within 30 min. Any isolated initial occurrence not meeting this criterion was discarded. Notably, this 25-km radius serves as a rigorous spatial constraint to not only mitigates the limitations of single-gauge measurements but also ensures the onset of rainfall at this scale are temporally coherent with that of the rain gauge co-located with RWP (as confirmed by sensitivity tests in Fig. S1 and Table S1 in the Supplement). This guarantees direct physical coupling between local rainfall and the RWP-observed wind profiles.

Nocturnal rainfall events were defined as those occurring between 20:00 and 08:00 Local Standard Time (LST). Based on operational classifications from the National Water Resources Bureau and CMA, the rainy season was categorized into four consecutive phases: (1) the South China Pre-summer Rainy Season (1 April–8 June 2023 and 1 April–9 June 2024), (2) the Meiyu Season (9 June–14 July 2023 and 10 June–21 July 2024), (3) the North China Rainy Season (15 July–31 August 2023 and 22 July–31 August 2024), and (4) the West China Autumn Rainy Season (1 September–31 October for both 2023 and 2024). These phases are subsequently designated as Phase 1 to Phase 4 throughout this study. Four regions of interest (ROIs) were subsequently selected for detailed analysis (see Table 1).

Further screening identified locally nocturnal HR events, where the mean 6-min rainfall intensity exceeded the 75th percentile of all recorded rainfall events at each station. This threshold can effectively distinguish significant HR from weak rainfall while ensuring a sufficient sample size for robust statistical analysis of minute-scale LLJ dynamics (Table S1). Furthermore, a sensitivity test by varying the thresholds to 85th and 95th percentile to ensure that the main conclusion regarding the precursory signals of LLJs is robust within a reasonable threshold range (see Figs. S2–S5).

Statistical analysis revealed 3155 nocturnal rainfall events during the 2023–2024 warm seasons (within the 31 red circles shown in Fig. 1). Event counts per rainy season phase were 1109, 689, 652, and 705 respectively, with 841 events classified as nocturnal HR events.

To ensure identified LLJs exhibit significant vertical wind shear characteristic of jet-like profiles, the following criteria are adopted: (1) a maximum horizontal wind speed exceeding 10 m s⁻¹ in the lowest 3 km a.g.l., and (2) a wind speed reduction of at least 3 m s⁻¹ from the maximum to minimum below 3 km a.g.l., or to 3 km a.g.l. if no minimum exists. These deliberately conservative wind speed thresholds maximize LLJ sample size for enhanced statistical robustness. This definition standard has been widely adopted in previous studies (Bonner, 1968; Whiteman et al., 1997; Du et al., 2014; Yan et al., 2021). The strength of LLJ or jet nose is defined as the maximum wind speed along the entire profile. The LLJ core height is defined as the altitude of the wind speed maximum during LLJ occurrences. Correspondingly, the LLJ direction is determined by the wind direction at the height of the LLJ.

We define rainfall events where LLJ occurs at least twice within 2 h before rainfall as an LLJ event (Li et al., 2024). The HR events influenced by LLJs (LLJ_HR events), HR events without LLJ influence (non-LLJ_HR events), and non-HR events affected by LLJ (LLJ_non-HR events) are further distinguished.

Firstly, we characterized the spatiotemporal patterns of rainfall and LLJs observed nationwide during the 2023–2024 warm season. Nationally, nocturnal rainfall accounted for 50.9 % of total warm-season rainfall, with pronounced concentrations over North, Northeast and Southwest China (Fig. 2d and 2g). In contrast, the pronounced daytime rainfall dominance in South China (Fig. 2a) may arise from the interaction between enhanced onshore monsoonal flows and terrain (Bai et al., 2021), sea breeze fronts and cold pool (Chen et al., 2016). In terms of frequency, nocturnal rainfall occurred more frequently, constituting 52.5 % of the total rainfall frequency versus 47.5 % for the daytime, with the highest nocturnal proportions found in southwestern and eastern regions (Fig. 2e and h). Although the national mean rainfall intensity was generally lower at night (1.2 mm h⁻¹) than during the day (1.8 mm h⁻¹; Fig. 2c and f), the probability of nocturnal HR occurrence was significant (51.3 %), particularly across western, northern, and northeastern China (Fig. 2i).

Figure 3 displays the key attributes of LLJs detected at all 31 RWPs across China using the criteria defined in Sect. 2. Nocturnal LLJ activity occurred more frequently, with an overall occurrence frequency increase of nearly 18 % relative to diurnal LLJs (Fig. 3a and e). This pronounced nighttime enhancement is consistent with the classical IO mechanism, whereby reduced surface friction after sunset allows the decoupled boundary layer to accelerate and form stronger LLJs. Spatially, both daytime and nighttime LLJs were more prevalent in eastern and southeastern China, particularly along the Yangtze River basin and coastal regions, where moisture-rich monsoonal flows dominate. In contrast, lower frequencies were observed over northwestern China, likely reflecting weaker large-scale moisture transport and reduced baroclinicity in arid inland regions.

In terms of jet core height (Fig. 3b and f), nocturnal LLJs generally exhibited slightly lower core altitudes compared to their daytime counterparts, with most cores concentrated below ∼1500 m. This lowering of the jet core at night is consistent with boundary-layer stabilization and the formation of a shallow nocturnal inversion, which confines the jet maximum to lower altitudes. Regarding jet intensity (Fig. 3c and g), nighttime LLJs were typically stronger, with a higher proportion of stations reporting wind speeds exceeding 16–18 m s⁻¹. The combination of enhanced wind speed and reduced core height suggests a more concentrated and dynamically organized jet structure during nighttime hours. The dominant wind directions (Fig. 3d and h) further reflect regional circulation controls. Southeasterly and southwesterly LLJs prevailed in eastern China, consistent with the transport of warm, moist air from the South China Sea and western Pacific during the warm season. In northern and northwestern regions, LLJs exhibited more variable directional characteristics, likely influenced by synoptic-scale pressure gradients and topographic channeling effects.

Overall, Fig. 3 demonstrates that nocturnal LLJs are not only more frequent but also stronger and lower in altitude than their daytime counterparts. These structural differences imply enhanced moisture transport efficiency and greater potential for nighttime convective organization, providing a dynamical foundation for the observed diurnal asymmetry in heavy rainfall occurrence examined in subsequent sections.

Statistical analysis revealed a substantial linkage between LLJs and nocturnal rainfall. Specifically, 56 % of all nocturnal rainfall events across China were preceded by the presence of LLJs within 2 h, establishing nocturnal rainfall influenced by LLJs as a major component of warm-season rainfall in China. This relationship was strongly modulated by the seasonal migration of the western Pacific subtropical high (WPSH), whose northward progression and subsequent retreat governed the latitudinal displacement of HR belts and closely synchronized with the spatiotemporal evolution of LLJ activity. The proportion of nocturnal rainfall events associated with LLJs during the four rainy season phases reached 60.4 %, 56.3 %, 49.4 %, and 54.9 %, respectively (solid-filled bars in Fig. 4a). Among 841 identified nocturnal HR events nationwide, 33.9 %–47.2 % were classified as LLJ_HR events across the four phases (diagonally striped bars in Fig. 4a). This contrast between the high LLJ association for general nocturnal rainfall and the more moderate fraction for HR indicates that, although LLJs are a frequent precursor to rainfall, their presence alone does not guarantee the occurrence of heavy rainfall.

A more detailed statistical analysis of ROIs revealed the key role of LLJ coupling in primary rain belt regions of each phase. A total of 71, 49, 33, and 34 nocturnal HR events were identified in these ROIs during the period from Phase 1 to Phase 4 (Fig. 4b). On average, nearly 45.0 % of HR events in these regions were associated with LLJs within 2 h before onset. Spatial analysis further confirmed that these LLJ_HR events consistently produced heavier rainfall intensities than non-LLJ_HR events (red boxes in Fig. 5), particularly within the four ROIs (red boxes in Fig. 5). Nevertheless, the non-LLJ_HR events exhibited spatially heterogeneous intensity distributions, where localized maxima may occur in areas outside the primary rain belts. For instance, during Phase 2 in ROI-3 (Fig. 5f), sporadic high-intensity events driven by deep cold trough system resulted in high site-averaged intensities even without LLJs, whereas in ROI-2, the absence of LLJs typically corresponded to weaker frontal precipitation (Fig. S6).

Furthermore, at the national scale, probability distributions of rainfall intensity (Fig. 6) indicated that LLJ_HR events exhibited a significantly higher tail (≥2.0 mm 6 min⁻¹) compared to non-LLJ_HR events during Phases 1 and 3. During Phases 2 and 4, however, the distributions of the two event types were comparable, with LLJ_HR events showing slightly weaker intensities. Regionally, rainfall intensities within the key ROIs generally exceeded the national average, particularly for LLJ_HR events. Specifically, ROI-1 and ROI-2 demonstrated significantly higher probabilities of heavier rainfall (≥2.0 mm 6 min⁻¹) in LLJ_HR events. Notably, LLJ_HR events in ROI-4 favored intensities near 0.5 and 2.8 mm 6 min⁻¹, yet the overall probabilities of heavier rainfall remained slightly lower than non-LLJ_HR events. Despite the relatively high frequency of LLJ_HR events in ROI-3 during Phase 3 (see the pie charts in Fig. 6), their probability of producing heavier rainfall was comparable to – rather than substantially greater than – that of non-LLJ_HR events. Moreover, this region exhibited the sharpest decay in probability density for heavier rainfall among all regions. This behavior suggests that, although LLJs occur frequently in this region and season, their contribution to extreme rainfall intensity is not dominant. Instead, other non-LLJ forcing mechanisms, such as topographic lifting and mesoscale convective systems, may play an equally or more significant role in generating HR in ROI-3 during Phase 3.

In summary, although LLJ_HR events were generally associated with enhanced rainfall intensities across most ROIs and most phases, only ∼31.1 % of all identified LLJ events were ultimately classified as HR events (Fig. 4b). This relatively low conversion rate indicates that the mere presence of LLJs is not sufficient to produce HR. The substantial number of LLJ_non-HR events implies that additional dynamic and thermodynamic conditions must coexist with LLJs to trigger HR. In particular, factors such as moisture transport efficiency, vertical wind shear configuration, atmospheric stability, and mesoscale lifting mechanisms may modulate whether an LLJ evolves into a heavy-rain-producing system. Therefore, a detailed further examination of the fine-scale vertical structures of LLJs prior to rainfall onset is crucial to disentangle the dynamical characteristics that distinguish HR-producing LLJs from non-HR cases, as explored in the following sections.

To elucidate the contrasting precursor characteristics of LLJs that lead to nocturnal rainfall of differing intensities, this section examines fine-scale vertical structure and continuous evolution of LLJs within 2 h preceding both LLJ_HR and LLJ_non-HR events during four phases in their respective ROIs. The results revealed the distinct spatiotemporal variations in vertical structure and evolutionary patterns of LLJs occurred across seasonal phases.

During Phase1 in ROI-1, LLJ_HR events exhibited a significant increase in frequency starting 108 min before rainfall onset, reaching secondary peaks at -84 and -60 min, culminating in maximum frequency immediately preceding HR (Fig. 7a). Meanwhile, the average wind profiles showed a rapid intensify trend from 48 min before HR onset, with the jet core reaching its peak wind speed (about 12.2 m s⁻¹) and its height distinctly decreased (Fig. 8a), although there is the transient weakening of jet strength within 60–48 min preceding HR. These LLJs featured a bimodal vertical distribution with frequent occurrence layers at 0.5–1 km and 1.5–2 km a.g.l. This structure was characteristic of double low-level jets (DLLJs), where the coexistence of the boundary layer jets (BLJs) and synoptic-system-related jets (SLLJs) generated a deep layer of forced ascent via BLJ-exit convergence and SLLJ-entrance divergence. This dynamical coupling significantly favors organized deep convection in ROI-1 (Uccellini and Johnson, 1979; Du and Chen, 2018, 2019; Liu et al., 2020). Note that the composite wind profile (Fig. 8a) does not show a distinct bimodal vertical distribution due to smoothing from averaging. Detailed examination of wind profiles revealed that approximately 40 % of LLJ_HR events exhibited DLLJs, while only 20 % of LLJ_non-HR events showed such a structure. Therefore, LLJ_non-HR events lacked this dynamic coupling, with jets predominantly confined to the single 0.5–1 km layer. Although LLJ_non-HR events showed a gradual increase in frequency from -48 min, along with strengthening winds prior to rainfall (Figs. 7e and 8e), these changes were rather limited compared to the pronounced evolution seen in LLJ_HR events under a background of overall lower frequency and weaker intensity. This steady and weak dynamical structure failed to provide sufficient dynamic lifting to efficiently initiate strong convection.

Both event types exhibited notably high frequencies and intensities of LLJs over ROI-2 during Phase 2, yet their evolutionary dynamics diverged sharply. For LLJ_HR events, a coherent oscillatory vertical reorganization of LLJs is evident (Figs. 7b and 8b). At the first stage, both LLJ frequency and wind speed maximum peaked (exceeding 12 m s⁻¹) at -120 min, with the core situated 1.5–2 km a.g.l. Subsequently, a rapid descent of frequently occurring height of LLJs to below 1 km a.g.l., occurred, accompanied by a concurrent decline in frequency and profile intensity to a minimum around 84–72 min preceding HR. Analysis of wind kinetic energy and its vertical transport (see Eqs. 1 and 2 in the Supplement) confirmed that the “sudden drop” likely results from the downward momentum transfer (Fig. S7a and c), which can efficiently enhance low-level disturbances and dynamic forcing and serve as an effective indicator of HR 1–2 h later (Liu et al., 2003; Fu et al., 2020). Following this descent, a distinct recovery phase ensued from -60 min, where the frequency increased reaching a secondary peak at -48 min and jet core re-ascended to 1–2 km a.g.l. The LLJ profile strength re-intensified to about 11.4 m s⁻¹. This rise of the jet core and secondary enhancement are likely tied to cold pool-LLJ interactions and intensified upward motion or latent heat release in convective clouds (further discussed in Sect. 3.3). In conclusion, this pattern suggests an intense internal dynamical adjustment process. In comparison, LLJ_non-HR events lacked such low-level momentum transfer signals (Fig. S7b and d) and maintained a quasi-steady state, with consistent LLJs strength (near 11.8 m s⁻¹) and a preferred height range of 1–2 km a.g.l. (Fig. 8f). The LLJs frequency exhibited gradual changes, peaking weakly at 36 min preceding rainfall before a subsequent rapid decrease (Fig. 7f). This pattern indicates an absence of the rapid dynamical redistribution observed in LLJ_non-HR events.

During Phase 3 in ROI-3, LLJ_HR events exhibited a bimodal temporal distribution in LLJ frequency, with prominent peaks at -96 and -48 min (Fig. 7c). The dominant LLJ height was centered between 1–1.5 km a.g.l. The wind profiles showed a corresponding evolution where the maximum wind speed increased from approximately 8.0 m s⁻¹ at -120 min to a first peak about 9.5 m s⁻¹ by -84 min. Following a transient weakening (-48 to -24 min), a secondary intensification occurred immediately preceding HR onset (Fig. 8c). Conversely, LLJ_non-HR events were characterized by substantially lower LLJs frequency (around 20 %) and a more diffuse structure (Fig. 7g), with wind profiles exhibiting weaker intensification preceding rainfall (Fig. 8g). Consequently, the rapid reorganization and final intensification of LLJs appeared to be critical dynamical drivers for HR. However, despite the potential influences of regional thermodynamics and topography, the insufficient dynamical forcing from overall weaker wind profiles in ROI-3 remained the primary reason for its comparatively lower probability of heavier rainfall (≥2.0 mm 6 min⁻¹).

During Phase 4 in ROI-4, LLJ_HR events exhibited a distinctive two-stage intensification process. The wind profiles initially strengthened rapidly starting from -120 min, reaching a primary peak of approximately 12.8 m s⁻¹ at -72 min (Fig. 8d), coinciding with a secondary peak in LLJ frequency. Following a brief weakening (-60 to -48 min), a renewed and explosive intensification occurred from -48 min onwards, continuing until rainfall onset. Throughout this period, the LLJ cores remained concentrated between 0.5–1.5 km a.g.l. (Fig. 7d). In sharp contrast, LLJ_non-HR events displayed a pattern of premature peaking followed by decay. Both frequency and intensity peaked earlier at -84 min, followed by general attenuation (Fig. 7h). By -48 min, weakened wind profiles stabilized into a double-core structure maintaining around 10 m s⁻¹, with distinct jet cores near 0.8 km and 1.7 km a.g.l. (Fig. 8h). Crucially, in the LLJ_non-HR event, this premature peak and the subsequent continuous attenuation of the low-level wind field resulted in a lack of sustained dynamic forcing during the critical pre-rainstorm stage, failing to trigger HR.

Synthesizing the evolution across all phases, although a distinct transient weakening of the jet profile was consistently observed, LLJs exhibited a rapid re-intensification of wind speed accompanied by a lowering of the jet core height during approximately the final 30 min preceding HR. This recurring pre-rainfall adjustment suggests that LLJs underwent a short-term dynamical reorganization prior to HR onset. We propose that this minute-scale oscillatory behavior – characterized by a “weakening-then-strengthening” or “descent-then-ascent” pattern – constitutes a robust dynamic precursor of HR. Physically, the temporary weakening may reflect momentum redistribution or enhanced turbulent mixing, whereas the subsequent intensification and descent of the jet core likely enhance low-level moisture convergence and vertical wind shear, thereby strengthening upward motion and promoting convective development (Markowski and Richardson, 2011). Such rapid structural adjustment indicates that the timing and vertical evolution of LLJs, rather than their mere presence, play a critical role in modulating heavy rainfall production.

Furthermore, probability distributions of LLJ strength and height within 2 h preceding rainfall were compared across key regions (Fig. 9). During Phase 1 in ROI-1, the strength of LLJs in LLJ_HR events was notably stronger by 2–3 m s⁻¹ than that in LLJ_non-HR events (Fig. 9a). Height distributions showed distinct bimodal peaks near 0.9 km and 1.75 km a.g.l. (Fig. 9e). The average LLJs height was generally higher in LLJ_HR events, which is usually affected by the coupling of the upper-level jet stream or the land-sea breeze. During Phase 2 in ROI-2, LLJ_HR events showed higher probabilities of strong LLJs (17–28 m s⁻¹) compared to the dominant 13 m s⁻¹ intensity in LLJ_non-HR events (Fig. 9b). Influenced by large-scale circulation patterns, both event types featured LLJs centered near 1.5 km a.g.l. (Fig. 9f), though LLJ_HR events developed a secondary maximum near 0.8 km a.g.l. due to pre-rainfall descent of the jet core (Fig. 7b). Contrastingly, Fig. 9c shows that LLJ_HR events were associated with weaker jet strengths (around 11 m s⁻¹) compared to LLJ_non-HR events (14–23 m s⁻¹) in ROI-3 during Phase 3, suggesting that strong LLJs do not necessarily induce HR here. The height of LLJ in LLJ_HR events mainly concentrated near 1.2 km a.g.l., whereas in LLJ_non-HR events, it was more uniformly distributed between 0–3 km a.g.l. with a higher probability nearly 1.5 km (Fig. 9g). For Phase 4 in ROI-4, LLJs strength peaked near 15 m s⁻¹ in both event types, but LLJ_HR events featured stronger jets reaching 25–30 m s⁻¹ (Fig. 9d). The LLJs height in both events peaked predominantly at 0.8 km a.g.l., with secondary peaks at 1.5 km for LLJ_HR and 2.0 km a.g.l. for LLJ_non-HR events (Fig. 9h).

In summary, although different internal dynamic adjustments, including frequency, occurrence height, and wind profile intensity of LLJs, preceding LLJ_HR events were observed due to the different dominant mechanisms influencing rainfall in each phase, our findings highlight the role of fine-scale LLJ structures and their rapid vertical reorganization in modulating nocturnal rainfall intensity, offering valuable insights for improving regional nocturnal HR forecasting.

The Sect. 3.2 has clarified that the fine-scale dynamic characteristics of LLJs – including their temporal evolution, vertical structure and intensity variations – play a pivotal role in modulating nocturnal rainfall intensity during rainy season phases. However, the influence of LLJs on rainfall generation and intensification rarely operates in isolation; instead, it depends strongly on the accompanying large-scale thermodynamic environment, which provides the necessary moisture supply and convective instability to sustain or amplify heavy rainfall. Thus, to fully unravel the mechanisms underlying the distinction between LLJ_HR and LLJ_non-HR events, it is essential to complement the dynamic analysis with an in-depth examination of the thermodynamic conditions associated with LLJs within the immediate pre-convective environment (within 1-h preceding rainfall).

Further analysis of the large-scale thermodynamic conditions at 1 h prior to rainfall onset (Figs. 10 and 11) reveals consistently stronger thermal instability for LLJ_HR versus LLJ_non-HR events, accompanied by stronger MFC within key regions during each rainy season.

During Phase 1 in ROI-1, thermodynamic conditions were comparable between event types. Southwesterly LLJs transported warm-moist air masses from the South China Sea and Bay of Bengal, forming a pronounced warm-humid tongue (Fig. 10a and e). Coupled with MFC centers developing north of the jet axis (Fig. 11a and e), this configuration facilitated nocturnal rainfall development. During Phase 2 in ROI-2, LLJ_HR events exhibited a significantly stronger warm-moisture tongue with core θe reaching 358 K – approximately 2 K higher than in non-HR events (Fig. 10b and f). Dynamically, the stronger LLJ core (difference >1.2 m s⁻¹) drove a sharper, continuous band of MFC along the left flank of the jet axis (Fig. 11b), creating a robust triggering mechanism for HR (Fig. 11b). During Phase 3 in ROI-3, intensified southwesterly LLJs in HR events drove substantial northward transport of abundant moisture and higher θe air (difference > 2 K) northward into a low θe environment (Fig. 10c), enhancing convective instability. The synergistic interaction of this moist, high-energy advection with orographic forcing from the Taihang Mountains generated intense MFC, with peak values south of Beijing approximately 30×10-5 km m⁻² s⁻¹ (Fig. 11c) larger than those in LLJ_non-HR events, thereby driving nocturnal HR. Thermodynamic contrasts were most pronounced during Phase 4 in ROI-4. Thermodynamic contrasts were most pronounced during Phase 4 in ROI-4. LLJ_HR events featured a deep high-θe region (>356 K) over the southeastern Tibetan Plateau (Fig. 10d), contrasting with the cold highs located to the northeast of ROI-4 and lower θe prevalent in LLJ_non-HR events (Fig. 10h). Concurrently, accelerated easterly-southeasterly LLJs drove warm, moist air towards the steep eastern Plateau margin. The impingement of this flow against the sharp topographic gradient generated intense dynamic lifting and low-level convergence. This mechanically forced ascent, synergizing with the abundant moisture transport and strong MFC (Fig. 11h), played an essential role in triggering the observed nocturnal HR in this region.

To elucidate the rapid processes leading to occurrence of rainfall, the minute-scale evolution of key thermodynamic and dynamic parameters was further analyzed (Fig. 12), including surface θe, LLJ index and VWS. Specifically, LLJ index is defined as the ratio of maximum wind speed below 3 km to the height where wind first exceeds 10 m s⁻¹. A rapid rise in LLJ index will reflect the extension and pulsing intensity of the LLJ, and its magnitude has been shown to be positively correlated with subsequent rainfall intensity 1–2 h later (Liu et al., 2003). VWS is calculated as the wind speed difference between the surface and jet height divided by the jet height and is used to characterize the bulk shear from the surface to the jet layer associated with the dynamical forcing and organization of convection (Wei et al., 2014).

Figure 12a illustrated that during Phase 1 in ROI-1, despite the similarity in large-scale environments between LLJ_HR and LLJ_non-HR events, they exhibited distinct differences in the continuous evolution of LLJ-associated thermodynamic conditions preceding rainfall onset. LLJ_HR events exhibited abrupt thermodynamic enhancement from 90 min preceding the onset of rainfall driven by rapid intensification of LLJs, with surface θe and VWS surging approximately 1.5 K and 0.005 s⁻¹ respectively. Concurrently, the LLJ index surged from approximately 0.05 to 0.08 and VWS peaked sharply at -60 min, signaling LLJs intensification and core descent (Figs. 7a, 8a). This rapid, minute-scale co-intensification of thermodynamic and dynamic processes serves as a critical precursor triggering HR. In contrast, LLJ_non-HR events showed weaker increases of θe and VWS and a declining LLJ index (by about 0.02) alongside rising jet cores, reducing low-level shear and convergence efficiency, thereby diminishing overall rainfall intensity.

During Phase 2 in ROI-2, the thermodynamic environment displayed a distinct “weakening-reintensification” pattern (Fig. 12b), which aligns precisely with the intrinsic dynamical adjustments of the wind field presented in Fig. 8b. Initially, at -120 min, concurrent peaks in the LLJ index and VWS were observed, coupled with a high surface θe of 348.3 K. During the subsequent transition period, a drastic elevation in the jet core height starting from -84 min caused a precipitous drop in the LLJ index. The timing of this rapid evolution suggests a transient optimal window for nocturnal rainfall triggering that is characteristic of LLJ_HR events in ROI-2. Following this, rapid surface cooling began 60 min prior to HR. This cooling was likely induced by the cold pool outflows associated with alternation or propagation of convective systems embedded within the Mei-Yu front cloud system (Zhang et al., 2023). The resulting dense cold air wedging beneath the strong southwesterly LLJs can lift the jet axis above the coldpool interface, further enhancing uplift and promoting rainfall (Luo et al., 2014). This in turn facilitated the final re-intensification of the jet structure (Figs. 7b and 8b). Crucially, this reorganized configuration sharply enhances lowlevel vertical wind shear and horizontal convergence (Fig. 12b), further promoting HR development. In contrast, LLJ_non-HR events exhibited weaker thermodynamic support and diminished dynamic forcing with consistently lower LLJ indices within 60 min preceding rainfall, resulting in insufficient lift to sustain HR. Compared with the disordered fluctuations of the LLJ_non-HR events, LLJ_HR events highlight the importance of thermal-dynamic synergy influenced by LLJs evolution. Even though the LLJ evolution may be modulated by convective feedback, the resulting reorganized jet profile still can serve as a robust dynamical precursor essential for triggering local HR.

During Phase 3 in ROI-3, LLJ_HR events featured prominent thermal compensation (surface Δθe > 1 K, 850 hPa Δθe>2 K versus non-HR events) – despite possessing generally weaker dynamical forcing compared to other phases (Fig. 12c). Temporally, the evolution was marked by distinct pulsations: The LLJ index exhibited a rapid rise (from ∼0.03 to ∼0.06) starting 84 min prior to HR onset (Fig. 12c) driven by a surge of LLJs profiles, while VWS peaked synchronously with the maximum LLJ frequency. Subsequently, a secondary peak in both the LLJ index and VWS was observed between -60 and -48 min. Although the subsequent declines in wind speed and frequency led to notable fluctuations in these parameters, the VWS and LLJ index underwent substantial intensification (with VWS increasing by ∼1.5 s⁻¹) in the final 24 min, driven by the rapid acceleration of the LLJ wind field. This co-evolution with rapid surface warming (increase of 0.25 K) released convective instability and enhanced convergence (Fig. 10). Nevertheless, the overall weaker dynamical conditions likely limited the depth and organization of convection, potentially accounting for the reduced probability of heavier rainfall compared to other phases. In contrast, during LLJ non-HR events, the LLJ index (∼0.03) and θe vary rather gradually.

During Phase 4 in ROI-4, under the favorably thermal environments (θe>346 K), LLJ_HR events showed a two-stage dynamic intensification. Initially, the LLJ index surged, while the VWS and jet intensity reached synchronous secondary peaks at -72 min. In the second stage, VWS increased rapidly by ∼0.9 (Fig. 12d), and the LLJ index maintained an overall upward trend, peaking immediately prior to onset due to the surging jet. But LLJ_non-HR events showed weakening trends in both dynamic and thermodynamic conditions during the final 30 min and exhibited weaker changes (ΔVWS < 0.45 s⁻¹, ΔLLJ index < 0.02), reflecting an absence of the coordinated intensification necessary to initiate and sustain HR.

Although the evolution paths of the thermodynamic environment vary across different phases, a universal cross-region precursor emerges: the LLJ index and VWS consistently exhibits a strengthening or stabilizing trend in the final approximately 30 min preceding HR onset, operating in concert with significant low-level warming (rising θe). In contrast, non-HR events generally lack this culminating dynamical intensification. Overall, these results adequately showcase the sensitivity of regional HR to the fine-scale structural evolution of LLJs and their coupling with thermodynamic environments.