Precipitation Characteristics of an Abrupt Heavy Rainfall Event over the Complex Terrain of Southwest China Observed by the FY-4A Satellite and Doppler Weather Radar

: On 22 July 2019, mesoscale convective systems (MCSs) with an abrupt heavy rainfall event (AHRE) hit Shuicheng County of Guizhou Province in Southwest China causing landslide and debris ﬂow secondary disasters. The AHRE over the complex terrain of Shuicheng County had di ﬀ erences in location and intensity during two stages of the event. The two stages could be divided into di ﬀ erent rainfall types (topographic rainfall and synoptic-weather-related rainfall) according to the spatiotemporal distribution and organization of MCSs based on surface and midlevel environmental ﬁeld conditions. During the topographic rainfall stage, smaller meso- γ -scale (2–20 km) convective cells with lower echo-top heights (6–10 km) occurred along the windward slope of the primary mountain peak. During the synoptic-weather-related rainfall stage, a meso- β -scale (20–200 km) convective echo band with higher echo-top heights (10–14 km) occurred in the valley of the region. An adverse wind area (AWA) with distinct convergence of radar radial velocity existed over Shuicheng County. A formation mechanism analysis of the AHRE showed that topographic rainfall occurred in the warm and moist area, while synoptic-weather-related rainfall occurred due to local convergence and the intrusion of a cold tongue. Compared to the early stage, the cold tongue from the higher terrain superimposed over the warm sector at the base of major mountain ranges appeared to strengthen the rainfall. topography of County


Introduction
In Southwest China, an abrupt heavy rainfall event (AHRE) is defined as a period of 3 h of rainfall ≥ 50 mm with at least one 1 h rainfall period of ≥20 mm during the successive three-hour period [1,2]. The Yunnan-Guizhou Plateau of Southwest China is dominated by complex terrain, which often experiences landslide and debris flow disasters when AHREs happen [3][4][5]. With the availability of long-term precipitation data based on gauge observations, several studies have focused

Doppler Weather Radar
Four C-band Doppler weather radars in the region operate on a 5 cm wavelength and provide nine unique elevation scans every 6 min. The beam widths of the four Doppler radars are 1 • and the physical widths of the beam 100-200 km from Shuicheng County are more than 1 km (about 1.74-3.49 km). In this study, we used two sets of radar data, namely (1) the three-dimensional mosaic production derived from four radars and (2) the data from the Xingyi radar. This mosaic dataset was produced by the Institute of Heavy Rain (IHR) [25], which has been used to identify convective systems [26]. The quality control method of individual radar data was mainly based on a fuzzy-logic algorithm to remove ground clutter [27], and the improved three-step postprocessing algorithm of the dual pulse repetition frequency (dual PRF) technique was used for the quality control of the radial velocity [28]. For the three-dimensional mosaic method, we (1) calculated the elevation, azimuth, and range using the longitude, latitude, and height under Cartesian coordinates; (2) used nearest-neighbor interpolation methods on range-azimuth planes combined with linear interpolation in the vertical direction to remap volumetric radar data from polar coordinates onto fine mesh grids (0.01 • × 0.01 • horizontal and 0.5 km vertical spacing) under Cartesian coordinates; (3) remapped the reflectivity fields from multiple radars onto a common Cartesian grid by using an exponential distance-weighting function; (4) set the interval time to remap multiple radars onto a common grid to be no greater than six minutes. The composite reflectivity and echo top height were obtained from the three-dimensional mosaic data set. The composite reflectivity was calculated by the vertical maximum reflectivity in all vertical levels. The echo top height was calculated from the height of 18 dBZ reflectivity [29].
Additionally, our study used the monitoring network of more than 1500 AWSs over the Yunnan-Guizhou Plateau in 10 min intervals to provide the surface precipitation, wind, temperature, and moisture fields. To analyze the MCS activities and related synoptic-weather systems, we used the latest ECMWF atmospheric reanalysis ERA5 (https://cds.climate.copernicus.eu/cdsapp#!/home) with a horizontal resolution of 0.25 • × 0.25 • and a time interval of 1 h.

Topography and Observed Precipitation
In Figure 1a, the Yunnan-Guizhou Plateau is the second-step terrain in the downstream region of Qinghai-Tibet Plateau (the first-step terrain). Shuicheng County is located in the eastern part of the Yunnan-Guizhou Plateau and is characterized by local complex terrain due to the Wumeng Mountains. The southwest boundary of Shuicheng County is dominated by the Niupengliangzi main peak with a height of 2865 m, and the middle part of the county is also occupied by higher terrain, with heights exceeding 2300 m. The southern area of Shuicheng County is located between two higher terrain areas with heights exceeding 2000 m, but the altitude of the southeastern part is less than 1750 m and has a narrow entrance with a height less than 1000 m. Therefore, Shuicheng County forms a typical "bellmouth" topography with a narrow southeastern airflow entrance between two higher terrain regions (Figure 1a). This "bellmouth" topography interacts with the easterly air flow, thereby creating favorable conditions for topographic rainfall. The landslide point of Jichang is located in the northern slope of the Niupengliangzi main peak, and the landslide and debris flow have a southwest-northeast trend from the hillside (Figure 1b). The geological and hydrological settings of Shuicheng County are vital for gaining a greater understanding of this landslide event. The red solid triangle represents the location of the landslide; Shuicheng County is outlined in blue.
In the inset map of panel (a), the Yunnan-Guizhou Plateau is outlined in blue, and the area of interest is outlined with a red box.
From 09:00 to 16:00 UTC on 22 July, a sudden rainstorm with a shorter duration occurred in the complex terrain of Shuicheng County; Figure 2 shows the hourly accumulated precipitation and topographic characteristics during the AHRE. The slope of the main peak is the transitional zone with a higher altitude gradient (e.g., red circle in Figure 2a), while the valley regions have relatively flat areas between the higher terrains (e.g., blue circle in Figure 2e). It can be seen that a 1 h rainfall amount ≥ 20 mm occurred from 09:00 to 10:00 UTC on 22 July, but only one station with a rainfall amount of 39.9 mm was located in the windward slope of the Niupengliangzi main peak (red circle area in Figure 2a). From 10:00 to 11:00 UTC, three stations located in the slope of the middle main peak of Shuicheng County had 1 h rainfall amounts of ≥20 mm. From 11:00 to 12:00 UTC, a west-east rainstorm belt was apparent in northern Shuicheng County at 26.6° N. In addition, there were three isolated stations in the southern part of the rainstorm belt: two stations in the slope of the Niupengliangzi main peak and another station in southeastern Shuicheng County that recorded rainfall in excess of 20 mm/h. Here, the station 5.4 km south of the landslide point had a 1 h rainfall amount of 25.4 mm and a 3 h rainfall amount of 65.3 mm from 09:00 to 11:00 UTC, which satisfied the conditions for an AHRE in the windward slope of the Niupengliangzi main peak (red circle area in Figure 2c). From 12:00 to 13:00 UTC, the blue-colored stations with 1 h rainfall amounts ≥ 20 mm increased rapidly and showed a northwest-southeast orientation band in the valley region between the major mountain ranges, such as two stations with 1 h rainfall amounts ≥ 20 mm 10 km north of the landslide point. From 13:00 to 14:00 UTC, the 1 h rainfall amount increased suddenly in the valley region, and four stations within the 8 km to the east of the landslide point recorded more than 50 mm of rain (blue circle area in Figure 2e), while there was no obvious heavy rainfall in the slope of the main peak (red circle area in Figure 2a). From 14:00 to 15:00 UTC, stations exceeding 20 mm decreased rapidly in the valley region, but, since stations had still previously recorded more than 50 mm of rain in the valley near the landslide location, the AHRE conditions were still satisfied. From the spatiotemporal distribution of the rainstorm, it can be seen that there were two rainfall stages in center Shuicheng County: an isolated rainfall in the slope of the main peak during the early stage (Figure 2a-c) and a stronger rainfall band located in the valley between the major mountain ranges during the later stage (Figure 2d  From 09:00 to 16:00 UTC on 22 July, a sudden rainstorm with a shorter duration occurred in the complex terrain of Shuicheng County; Figure 2 shows the hourly accumulated precipitation and topographic characteristics during the AHRE. The slope of the main peak is the transitional zone with a higher altitude gradient (e.g., red circle in Figure 2a), while the valley regions have relatively flat areas between the higher terrains (e.g., blue circle in Figure 2e). It can be seen that a 1 h rainfall amount ≥ 20 mm occurred from 09:00 to 10:00 UTC on 22 July, but only one station with a rainfall amount of 39.9 mm was located in the windward slope of the Niupengliangzi main peak (red circle area in Figure 2a). From 10:00 to 11:00 UTC, three stations located in the slope of the middle main peak of Shuicheng County had 1 h rainfall amounts of ≥20 mm. From 11:00 to 12:00 UTC, a west-east rainstorm belt was apparent in northern Shuicheng County at 26.6 • N. In addition, there were three isolated stations in the southern part of the rainstorm belt: two stations in the slope of the Niupengliangzi main peak and another station in southeastern Shuicheng County that recorded rainfall in excess of 20 mm/h. Here, the station 5.4 km south of the landslide point had a 1 h rainfall amount of 25.4 mm and a 3 h rainfall amount of 65.3 mm from 09:00 to 11:00 UTC, which satisfied the conditions for an AHRE in the windward slope of the Niupengliangzi main peak (red circle area in Figure 2c). From 12:00 to 13:00 UTC, the blue-colored stations with 1 h rainfall amounts ≥ 20 mm increased rapidly and showed a northwest-southeast orientation band in the valley region between the major mountain ranges, such as two stations with 1 h rainfall amounts ≥ 20 mm 10 km north of the landslide point. From 13:00 to 14:00 UTC, the 1 h rainfall amount increased suddenly in the valley region, and four stations within the 8 km to the east of the landslide point recorded more than 50 mm of rain (blue circle area in Figure 2e), while there was no obvious heavy rainfall in the slope of the main peak (red circle area in Figure 2a). From 14:00 to 15:00 UTC, stations exceeding 20 mm decreased rapidly in the valley region, but, since stations had still previously recorded more than 50 mm of rain in the valley near the landslide location, the AHRE conditions were still satisfied. From the spatiotemporal distribution of the rainstorm, it can be seen that there were two rainfall stages in center Shuicheng County: an isolated rainfall in the slope of the main peak during the early stage (Figure 2a

Tracking and Organization of the MCSs
The propagation process of MCSs is very complicated and includes multiple cloud cluster movements, extinction, regeneration, merging, and splitting [26,30]. Figure 3a depicts the MCS centroid locations and their propagation paths over Southwest China objectively. The MCSs formed in the southern part of Sichuan Basin at 19:00 UTC on 21 July and then propagated eastward until 13:00 UTC on 22 July. Afterwards, the MCSs split into two parts located in either Chongqing or the Yunnan-Guizhou Plateau. The southern part of the MCSs had a longer duration of 7 h, which appeared to have southeastward and then westward propagation in the Yunnan-Guizhou Plateau. Figure 3b depicts the evolution of the MCS, which formed with a radius of 69 km before growing

Tracking and Organization of the MCSs
The propagation process of MCSs is very complicated and includes multiple cloud cluster movements, extinction, regeneration, merging, and splitting [26,30]. Figure 3a depicts the MCS centroid locations and their propagation paths over Southwest China objectively. The MCSs formed in the southern part of Sichuan Basin at 19:00 UTC on 21 July and then propagated eastward until 13:00 UTC on 22 July. Afterwards, the MCSs split into two parts located in either Chongqing or the Yunnan-Guizhou Plateau. The southern part of the MCSs had a longer duration of 7 h, which appeared to have southeastward and then westward propagation in the Yunnan-Guizhou Plateau. Figure 3b depicts the evolution of the MCS, which formed with a radius of 69 km before growing significantly to its maximum radius of 309 km at 09:00 UTC on 22 July; this was the strongest stage of the MCS, corresponding to a minimum TBB of 186 K. Between 06:00 and 09:00 UTC, the MCS grew substantially but decreased in circularity, which suggests that it merged with southern banded convective systems, lost its circular shape (Figure 3c), and evolved into a more complicated structure (Figure 3d). At 14:00 UTC, this MCS split into two components, with properties of the southern part still present in Figure 3b. At this point, the southern MCS over Yunnan-Guizhou Plateau reached Shuicheng County and its strongest stage again, with a minimum TBB of 186 K. Figure 3c-f provides infrared images of the TBB and the corresponding 10 min accumulated precipitation. In Figure 3d, there were two rainbands in the southern MCS: a northern rainband along its northern edge and a southern small-scale rainband in Shuicheng County,~200 km south of the main rain belt. At 13:40 UTC, the banded MCS split into two parts, and the southern MCS adopted an east-west orientation in the Yunnan-Guizhou Plateau. Meanwhile, the northern edge of the southern MCS with the main rain belt hit Shuicheng County. At 18:30 UTC, the southern MCS moved westwards, and the heavy rainfall weakened in Shuicheng County. The main rain belt was located along the northern edge of the identified banded MCSs (northern ellipses in Figure 3d,e), while a small-scale local rainband occurred in front of the banded MCSs over complex terrain (southern ellipses in Figure 3d). However, the small-scale local rainband over complex terrain in Shuicheng County is difficult to predict by the large-scale and mesoscale numerical models ( Figures A1 and A2).
Water 2020, 12, x FOR PEER REVIEW 7 of 19 significantly to its maximum radius of 309 km at 09:00 UTC on 22 July; this was the strongest stage of the MCS, corresponding to a minimum TBB of 186 K. Between 06:00 and 09:00 UTC, the MCS grew substantially but decreased in circularity, which suggests that it merged with southern banded convective systems, lost its circular shape (Figure 3c), and evolved into a more complicated structure (Figure 3d). At 14:00 UTC, this MCS split into two components, with properties of the southern part still present in Figure 3b. At this point, the southern MCS over Yunnan-Guizhou Plateau reached Shuicheng County and its strongest stage again, with a minimum TBB of 186 K. Figure 3c-f provides infrared images of the TBB and the corresponding 10 min accumulated precipitation. In Figure 3d, there were two rainbands in the southern MCS: a northern rainband along its northern edge and a southern small-scale rainband in Shuicheng County, ~200 km south of the main rain belt. At 13:40 UTC, the banded MCS split into two parts, and the southern MCS adopted an east-west orientation in the Yunnan-Guizhou Plateau. Meanwhile, the northern edge of the southern MCS with the main rain belt hit Shuicheng County. At 18:30 UTC, the southern MCS moved westwards, and the heavy rainfall weakened in Shuicheng County. The main rain belt was located along the northern edge of the identified banded MCSs (northern ellipses in Figure 3d,e), while a small-scale local rainband occurred in front of the banded MCSs over complex terrain (southern ellipses in Figure 3d). However, the small-scale local rainband over complex terrain in Shuicheng County is difficult to predict by the large-scale and mesoscale numerical models ( Figures A1 and A2). The MCSs may take on different types of organization in regions with different environmental conditions [31]. In this study, we describe the organization of the convective cloud clusters in the MCSs by combining the surface and midlevel environmental field conditions to evaluate the two heavy rainfall stages in Shuicheng County. To show the overall convective characteristics in the MCSs clearly, the convective cloud cluster in the satellite images and corresponding radar composite reflectivity under different environmental field conditions are shown in Figure 4. At 09:00 UTC, during the early rainfall stage, a banded convective cloud cluster with a northeast-southwest orientation was located on the northwest edge of Shuicheng County. At this point, the body of this MCS had not moved into Shuicheng County, and Shuicheng County was dominated by southwesterly winds with no obvious synoptic-weather system present (Figure 4a). However, southeasterly warm and moist air at the surface flowed into the "bellmouth" topography, which contributed to the topographic rainfall in Shuicheng County (Figure 4b). In addition, the obvious vertical shear environment of the horizontal winds over Shuicheng County from the surface to 700 hPa favored the formation of topographic convection [32]. At 12:00 UTC, before the later rainfall stage happened, convective cloud clusters in the MCSs had organized into a west-east oriented band that corresponded to an intense radar echo belt in the northwestern and northeastern areas of Shuicheng County. Meanwhile, a low-vortex weather system of cyclonic winds at 700 hPa (the "L" in Figure 4c) formed in the southwest of Shuicheng County, and a stronger airflow convergence line occurred in the northern area of this low-vortex. Here, the convergence zone of the surface wind fields had moved southwards (Figure 4d). At 14:00 UTC, during the later rainfall stage, a convective cloud band moved southwards and formed an intense cold core high over Shuicheng County. This intense cold core developed into its strongest stage in Figure 3b, with a minimum TBB of 186 K and a cloud-top height of 17,100 m. Meanwhile, the low-vortex enhanced and moved southwards, and stronger southeasterly winds flowed into Shuicheng County. The stronger convective echo belt was located in the northeastern area of the midlevel low-vortex (Figure 4e). In the surface environmental field, the convergence zone was pushed to the southern border of Shuicheng County, and cold air hit the southern region of Shuicheng County (Figure 4f).
According to the spatiotemporal evolution and organizational characteristics of the MCSs, using both the surface and midlevel environmental field conditions, we could conclude that two stages of heavy rainfall in Shuicheng County occurred with different rainfall types. During the early stage, the body of the banded MCSs was located in the northwest of Shuicheng County, while the southeasterly warm and moist air at the surface in front of the MCSs flowing into the "bellmouth" topography caused topographic rainfall. During the later stage, the banded MCSs split into two parts, and the southern MCS with an intense cold core hit Shuicheng County. The AHRE at this stage was related to the environmental conditions of the 700 hPa low-vortex and the surface cold and warm air convergence zones, i.e., the synoptic-weather-related rainband.

Precipitation Characteristics Observed by Doppler Radar
Radar detection over the Yunnan-Guizhou Plateau may be influenced by complex terrain, so it is important to determine how the observation capacity and precipitation characteristics from Doppler radar differ during the two rainfall stages. Consider the evolution of the radar composite reflectivity and echo-top height from the three-dimensional mosaic dataset in detail to evaluate the terrain precipitation (in Figures 5 and 6). In this study, we used the maximum composite reflectivity within one hour to avoid the randomness of time selection, allowing the radar reflectivity to be closer to the distribution of the hourly accumulated precipitation [33]. Shinoda et al. [34] demonstrated that convective cells (≥30 dBZ) with low echo-top heights less than 1 km above the environmental 0 °C

Precipitation Characteristics Observed by Doppler Radar
Radar detection over the Yunnan-Guizhou Plateau may be influenced by complex terrain, so it is important to determine how the observation capacity and precipitation characteristics from Doppler radar differ during the two rainfall stages. Consider the evolution of the radar composite reflectivity and echo-top height from the three-dimensional mosaic dataset in detail to evaluate the terrain precipitation (in Figures 5 and 6). In this study, we used the maximum composite reflectivity within one hour to avoid the randomness of time selection, allowing the radar reflectivity to be closer to the distribution of the hourly accumulated precipitation [33]. Shinoda et al. [34] demonstrated that convective cells (≥30 dBZ) with low echo-top heights less than 1 km above the environmental 0 • C level have typical horizontal scales of less than 20 km (meso-γ-scale). The height of the environmental 0 • C level is about 6 km over Shuicheng County from the adjacent sounding station (not shown). The uncertainty on the echo top height from a single radar at 100 km range in our study region is about 2 km. The three-dimensional mosaic from four radars could reduce this uncertainty, but it still remains. So, we defined the low echo top heights for convective cells as less than 10 km in this study.
During the topographic rainfall stage (Figures 5a-c and 6a-c), there are several isolated meso-γ-scale (2-20 km) convective cells with lower echo-top heights (6-10 km) that occurred in the slope of the main peak. From 09:00 to 10:00 UTC, a separate convective cell "A" with reflectivity values over 30 dBZ and an echo-top height of about 6-10 km was collocated with a 1 h rainfall amount of 39.9 mm 5 km south of the landslide point. The convective cells "B," "C," "D," and "E" also have lower echo-top heights of about 6-10 km in the windward slope of the main peak. In addition to the convective cells, there was an obvious convective band with a higher echo-top height (10-14 km) located in the northern part of the topographic rainfall area, which was caused by surface convergence (Figure 4b). From 10:00 to 11:00 UTC, cells "A" through "D" had moved northeastwards and merged into the stronger convective cells "A + B" and "C + D" due to the 700 hPa southwesterly winds over the topographic rainfall area (Figure 4a). The cells "A + B" and "C + D" were collocated with two distinct rainfall centers of 1 h rainfall amounts ≥ 20 mm in the slope of the middle main peak, and the composite reflectivity of cell "C + D" reached 45 dBZ with an echo-top height of 10 km in the narrow southeasterly airflow entrance area. Moreover, the synoptic-weather-related echo band in northern Shuicheng County moved southwards and approached the topographic rainfall area. From 11:00 to 12:00 UTC, cells "A + B" and "C + D" continued to moved northeastwards, and cells "C + D" and "E" had merged into a convective cell with a 1 h rainfall amount of ≥20 mm. In the meantime, there was a new convective cell "F" formed on the eastern slope of the Niupengliangzi main peak. The synoptic-weather-related echo band had moved to the middle of Shuicheng County. During the synoptic-weather-related rainfall stage (Figures 5d-f and 6d-f), there were obvious meso-β-scale (20-200 km) convective bands with higher echo-top heights (10-14 km) in Shuicheng County. From 12:00 to 13:00 UTC, cells "A + B" and "C + D + E" during the topographic rainfall stage had merged into a synoptic-weather-related echo band with a northwest-southeast orientation, which corresponded to the banded rainfall with a 1 h rainfall amount of ≥20 mm in the valley between the major mountain ranges. The echo-top height reached 14 km in the south of echo belt. From 13:00 to 14:00 UTC, the echo belt moved southwards and passed through the valley of Shuicheng County. It can be seen that an area of composite reflectivity exceeding 35 dBZ increased in the valley, with the location of the landslide located just west of the echo belt location. Four weather stations recorded hourly accumulated rainfall amounts of more than 50 mm with weaker recorded reflectivity values than those of the band to the east because of the beam blockage from the Niupengliangzi main peak. The echo-top heights of composite reflectivity exceeding 30 dBZ were about 10-14 km in the valley region. From 14:00 to 15:00 UTC, the echo belt with a higher echo-top height continued to move southwards to the south of the landslide point. From the above analysis, it seems that Doppler radar should have been able to observe the same precipitation characteristics obtained over Shuicheng County in Section 3.1; however, beam blockage in the region reduced the intensity of the radar reflectivity. During the synoptic-weather-related rainfall stage, there was stronger convective development in the valley region. Figure 7 provides the Plan Position Indicator (PPI) and Range Height Indicator (RHI) scans of the reflectivity and radial velocity to show the precipitation structure and corresponding local wind field information during the synoptic-weather-related rainfall stage. It should be noted that the RHI is reconstructed from the PPI volume scan, so it is not a true RHI scan; therefore, observations at different elevation angles will be temporally displaced. Larger reflectivity values exceeding 30 dBZ were found over the valley terrain of Shuicheng County 120 km north of Xingyi in the PPI scans. Meanwhile, the RHI scan along the intense echo center could only observe During the synoptic-weather-related rainfall stage, there was stronger convective development in the valley region. Figure 7 provides the Plan Position Indicator (PPI) and Range Height Indicator (RHI) scans of the reflectivity and radial velocity to show the precipitation structure and corresponding local wind field information during the synoptic-weather-related rainfall stage. It should be noted that the RHI is reconstructed from the PPI volume scan, so it is not a true RHI scan; therefore, observations at different elevation angles will be temporally displaced. Larger reflectivity values exceeding 30 dBZ were found over the valley terrain of Shuicheng County 120 km north of Xingyi in the PPI scans. Meanwhile, the RHI scan along the intense echo center could only observe these higher reflectivity values above 3.5 km, and the echo-top height of the 18 dBZ values approached 14 km (Figure 7b).
In contrast to the reflectivity, a distinct convergence zone of the radial velocity was found along the echo belt, with an area of divergence to the north of the belt. The negative radial velocity zone was surrounded by a positive radial velocity zone, which indicates an adverse wind area (AWA) over Shuicheng County. AWAs are related to strong mesoscale convection, and the edge of the AWA corresponds to the heavy rain area [35]. On the RHI of the radial velocity, there is a distinct vertical convergence zone from 3.5 to 8 km.
Water 2020, 12, x FOR PEER REVIEW 13 of 19 these higher reflectivity values above 3.5 km, and the echo-top height of the 18 dBZ values approached 14 km (Figure 7b). In contrast to the reflectivity, a distinct convergence zone of the radial velocity was found along the echo belt, with an area of divergence to the north of the belt. The negative radial velocity zone was surrounded by a positive radial velocity zone, which indicates an adverse wind area (AWA) over Shuicheng County. AWAs are related to strong mesoscale convection, and the edge of the AWA corresponds to the heavy rain area [35]. On the RHI of the radial velocity, there is a distinct vertical convergence zone from 3.5 to 8 km.

Formation Mechanism of the AHRE
To briefly show the formation mechanism of the AHRE during the two rainfall stages, Figure 8 shows the surface wind fields and equivalent potential temperature θe fields during the two rainfall stages. θe was used in this paper because it was calculated using air pressure, temperature, and dewpoint temperature, and its variation with time reflects the temperature and moisture content of air passing over a site [36]. At 09:00 UTC during the topographic rainfall stage, the stronger southeasterly winds surged into the "bellmouth" topography of Shuicheng County, and a weak local convergence zone developed in northern Shuicheng County. On the interpolated θe fields, there were larger value areas of θe in Shuicheng County, which corresponded to warm and moist areas. Therefore, we can conclude that the warm and moist southeasterly flow encountered the "bellmouth" topography of Shuicheng County that favors the generation of topographic rainfall.

Formation Mechanism of the AHRE
To briefly show the formation mechanism of the AHRE during the two rainfall stages, Figure 8 shows the surface wind fields and equivalent potential temperature θ e fields during the two rainfall stages. θ e was used in this paper because it was calculated using air pressure, temperature, and dewpoint temperature, and its variation with time reflects the temperature and moisture content of air passing over a site [36]. At 09:00 UTC during the topographic rainfall stage, the stronger southeasterly winds surged into the "bellmouth" topography of Shuicheng County, and a weak local convergence zone developed in northern Shuicheng County. On the interpolated θ e fields, there were larger value areas of θ e in Shuicheng County, which corresponded to warm and moist areas. Therefore, we can conclude that the warm and moist southeasterly flow encountered the "bellmouth" topography of Shuicheng County that favors the generation of topographic rainfall. cells occurred in the southern warm and moist area with bigger θe values. The topographic rainfall was caused by the interaction of the atmospheric flow with the terrain. During the synoptic-weatherrelated rainfall stage, a convective echo belt was enhanced when local convergence and a cold tongue reached the valley region in Shuicheng County. This indicates that a cold tongue from higher terrain superimposed over warm sectors in the bases of major mountain ranges could strengthen the rainfall in valleys. Here, the warm and moist air flowing into the "bellmouth" topography formed a warm sector in the valley. Douglas [37] demonstrated that rain in the warm sectors of valleys plays a large and often dominant part in substantial orographic rainfall in the British Isles. At 12:00 UTC, before the synoptic-weather-related rainfall happened, the speed of the northeasterly winds increased and that of the southerly winds decreased, as the local convergence zone moved to the northwestern edge of the valley region. On the interpolated θ e fields, an obvious cold tongue that was caused by the northeasterly winds reached the northwestern edge of Shuicheng County. At 13:40, during the synoptic-weather-related rainfall stage, the local convergence zone was pushed to the southern border of Shuicheng County, and the θ e field indicated that the cold tongue became superimposed over the warm sector in the valley, which led to atmospheric convective instability. Houze [38] also noted that MCSs occurring near mountains are affected by the channeling of airflow near the mountains, capping the moist boundary layers by flow subsiding from the higher terrain.
From the above analysis, there are different environmental conditions and formation mechanisms during the two rainfall stages. During the topographic rainfall stage, isolated convective cells occurred in the southern warm and moist area with bigger θ e values. The topographic rainfall was caused by the interaction of the atmospheric flow with the terrain. During the synoptic-weather-related rainfall stage, a convective echo belt was enhanced when local convergence and a cold tongue reached the valley region in Shuicheng County. This indicates that a cold tongue from higher terrain superimposed over warm sectors in the bases of major mountain ranges could strengthen the rainfall in valleys.

Summary
Shuicheng County is characterized by locally complex terrain in the eastern Yunnan-Guizhou Plateau. At 09:00 to 16:00 UTC on 22 July 2019, an AHRE occurred in Shuicheng County. This event attracted significant attention in China because of the resulting serious natural disaster, which is unsuited for multiple large-scale numerical models to predict the small-scale orographic and convective components of the event. Additionally, the high-resolution mesoscale numerical model has not resolved the location and intensity of heavy rainfall over complex terrain. In this study, we used multiple observational datasets to provide support for understanding such an AHRE. First, based on the topography and observed precipitation distribution, the heavy rainfall over complex terrain showed two stages of location and intensity differences. Then, according to the spatiotemporal evolution and organizational characteristics of MCSs determined by combining surface and midlevel environmental field conditions, the AHRE was divided into two types: topographic rainfall and synoptic-weather-related rainfall. Next, multiple Doppler weather radars were utilized to depict radar echo characteristics during the two stages. Finally, surface AWSs and terrain data were used to analyze the surface wind, temperature, and humidity fields to briefly demonstrate the environmental conditions and formation mechanisms of the AHRE.
The observed precipitation showed that isolated rainfall centers occurred in the slope of the main peak during the early stage and that a stronger rainfall band located in the valley region between major mountain ranges occurred during the later stage. Upper-level observations of the MCSs by combining surface and middle-level environmental field conditions showed that different rainfall types affected the two stages of heavy rainfall in Shuicheng County. During the early stage, the body of the banded MCSs was located in northwestern Shuicheng County, while the southeasterly warm and moist air at the surface in front of the MCSs flowing into the "bellmouth" topography caused topographic rainfall. During the later stage, the banded MCSs split into two parts, and the southern MCS with intense cold core impacted Shuicheng County; the AHRE occurred due to the interaction of surface convergence and midlevel low-vortex systems.
An observational analysis of Doppler weather radar data showed that echo characteristics were also different during the two rainfall stages. During the topographic rainfall stage, smaller meso-γ-scale (2-20 km) convective cells with lower echo-top heights (6-10 km) occurred in the windward slope of the main peak; during the synoptic-weather-related rainfall stage, meso-β-scale (20-200 km) convective echo bands with higher echo-top heights (10-14 km) occurred in the valley. The terrain beam blockage also reduces the intensity of the observed radar reflectivity values. An AWA with distinct convergence of radial velocity existed over Shuicheng County.
The analysis of surface AWSs and terrain datasets showed that topographic rainfall occurred in the southern warm and moist area, while synoptic-weather-related rainfall occurred due to local convergence and the intrusion of a cold tongue. The superimposition of a cold tongue from the higher terrain over the warm sector at the base of the mountain range likely strengthened the rainfall.
The present study suggests that MCSs with different types of rain over complex terrain are important for forecasting AHREs, given the precipitation features and formation mechanisms of the AHRE considered herein from multiple observational datasets. However, this study lacked vertical observations of atmospheric environmental fields with higher resolutions, such as those from wind profile radar and sounding balloon observations, which provide additional wind, temperature, and humidity data at various pressure levels. In addition, data assimilation of in-storm Doppler weather radar reflectivity and radial velocity observations could be further utilized to initialize the mesoscale models and predict smaller-scale topographic rainfall. Additionally, high-resolution observations from the FY-4A, especially the horizontal gradients in environmental conditions could be very useful in obtaining more accurate representations of environmental conditions when assimilated in conjunction with radar observation.    The GRAPES has two forecast systems, i.e., GRAPES_GFS (global forecast system) and GRAPES_MESO (regional forecast system). The GRAPES_MESO has assimilated the observational data of FY-2E satellite but not Dopppler wather radar. The dashed-line red box outlines the area of interest in our study.