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Formation Mechanism and Microphysics Characteristics of Heavy Rainfall Caused by Northward-moving Typhoons
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摘要: 利用NCEP FNL分析资料、青岛降水现象仪和双偏振雷达观测资料, 对北上台风利奇马(1909)和巴威(2008)引发的局地对流性强降水微物理特征进行分析, 结果表明: 在台风外围的东南暖湿气流内, 受地形或边界层锋区触发形成的强对流单体后向传播或原地合并加强造成了局地强降水; 雨滴的质量加权平均直径(Dm)和对数归一化浓度(lgNw)分别为1.89 mm和3.86, 与典型台风降水相比平均直径更大、浓度更低, 形状参数μ和斜率Λ的μ-Λ关系也有明显不同; 随着雨强增强, 小雨滴占比下降而中到大雨滴比例明显上升, 直径1~4 mm雨滴对短时强降水的贡献超过90%;雨滴的碰并增长和对云水的聚集作用在对流性降水中占主导地位, 同时深厚的凇附过程对极端强降水的出现也起到了重要作用。Abstract: Local torrential rain and short-term heavy rainfall of small spatial-temporal scale are caused by northward-moving Typhoon Lekima (1909) and Typhoon Bavi (2008) in Qingdao area, with the maximum hourly rainfall of 60.3 mm·h-1 and 130.1 mm·h-1, respectively, while the prediction performance of numerical weather prediction model is very poor. Using NCEP FNL analysis data, raindrop spectrum and polarimetric radar data, the microphysics characteristics of the heavy rainfall are analyzed. The rainfall mainly occurs in a narrow belt region extending northwestward from the coastal mountainous area. The warm and humid air is transported by the southeast wind strengthens the instability. Convective cells are constantly triggered by topography or boundary layer front, and then move northwestward and form linear multicell storms under strong wind condition, or merges into local strong storms when the wind is weak. Both can cause local heavy rainfall. The mass weighted average diameter (Dm) and logarithmic normalized intercept (lgNw) are 1.89 mm and 3.86, respectively, which are between tropical marine-time and continental convective precipitation, indicating a larger mean diameter and lower number concentration compared to the typhoon rainfall in East China and South China. The μ-Λ slope is also significantly different, indicating the dominant microphysical processes are different. With the increase of rainfall intensity, the proportion of small particles below 1 mm decreases significantly, and the proportion of medium-large particles increases, indicating significant collision-coalescence process. Particles with 1-4 mm diameters contribute more than 90% to short-term heavy rainfall. When hourly rainfall is more than 50 mm·h-1, the proportion of small particles increases and particles with 2-3 mm diameter changes little, indicating that breakup and collision-coalescence process reaches equilibrium. Aggregate process and dry snow is dominant above -20℃ level and grapuel produced by riming process is dominant between -10℃ and 0℃ level. With the decrease of height, the values of ZH, ZDR and KDP increase, and raindrops change from light rain to heavy rain particles. At the same time, the liquid water content is significantly greater than ice water content, indicating that the collision-coalescence and accretion process play a critical role in the formation of heavy rainfall. Riming process also plays an important role in extreme heavy rainfall, during which its height can reach near -20℃ layer. The positive feedback of latent heat release leads to the strengthening of convective activity, resulting in more graupel particles and greater ice water content. The melting of graupel directly increases the rainfall. On the other hand, it produces big droplets, which enhance the warm-rain processes and leads to the increase of rainfall intensity.
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图 1 台风路径、地形高度和降水分布 (a)利奇马和巴威逐小时中心位置(方框表示图1b~1d范围)，(b)青岛地区地形海拔高度(阴影)、S波段双偏振雷达(SPOL) 和降水现象仪(PPI)位置(圆圈表示雷达50 km，100 km和150 km距离圈)，(c)2019年8月11日00:00—16:00自动雨量站累积降水量(填色站点；方框表示最大小时雨强出现的站点)，(d)2020年8月26日02:00—18:00自动雨量站累积降水量(说明同图1c)
Fig. 1 The typhoon track, terrain height and precipitation distribution (a)the tracks of Typhoon Lekima and Typhoon Bavi from China Meteorological Administrator (the box denotes the range in next 3 panels), (b)terrain height of Qingdao (the shaded), location of Qingdao S-band polarimetric radar (SPOL) and precipitation phenomenon instrument(PPI) (black circles denote radius of 50 km, 100 km and 150 km), (c)accumulated precipitation of automatic rain gauges (colorful dots) from 0000 BT to 1600 BT on 11 Aug 2019 (the box denotes the station with maximum hourly precipitation), (d)accumulated precipitation of automatic rain gauges from 0200 BT to 1800 BT on 26 Aug 2020 (the same as in Fig. 1c)
图 2 水平风场(风羽)、假相当位温(填色) 和垂直速度(等值线，单位: Pa·s-1) 沿36°N纬向-垂直剖面(三角形表示最大小时雨强站点经度) (a)2019年8月11日02:00，(b)2020年8月26日08:00
Fig. 2 Cross-section of horizontal wind (the barb) and pseudo-equivalent potential temperature (the shaded) and vertical velocity (the contour, unit: Pa·s-1) along 36°N at 0200 BT on 11 Aug 2019(a) and 0800 BT on 26 Aug 2020(b)
(the triangle denotes the longitude of station with maximum hourly precipitation)
图 3 主要降水阶段青岛雷达组合反射率因子
(填色，30 dBZ以下回波未显示；方框表示对流降水微物理特征分析范围)
Fig. 3 Composite reflectivity factor during main precipitation stage
(the shaded, echoes below 30 dBZ are not shown; the box denotes the region of microphysics analysis)
图 4 降水现象仪反演的雨滴谱特征 (a)利奇马和巴威降水Dm-lgNw散点图(橙色菱形表示对流性降水的平均Dm和lgNw，其余各形状点代表不同台风个例的平均值，实线(虚线)方框表示海洋型(大陆型)对流性降水Dm-lgNw平均值分布范围，灰色虚线表示10 mm·h-1雨强位置)，(b)利奇马和巴威5 mm·h-1以上降水(黑色实线) 的μ-Λ关系(彩色虚线表示不同台风个例降水的μ-Λ关系)，(c)不同雨强下不同直径雨滴对数浓度Nt的贡献率，(d)同图 1c，但为对降水量R的贡献率
Fig. 4 Raindrop characteristics based on the PPI observation (a)scatterplot of Dm-lgNw for Typhoon Lekima and Typhoon Bavi (the averaged Dm-lgNw pairs for convective rain of different cases are given by corresponding shape, orange diamond represents average value of Lekima and Bavi, the solid(dashed) rectangle corresponds to the maritime (continental) convective cluster, the gray dashed line indicates the rainfall rate of 10 mm·h-1) (b)scatterplot of μ-Λ for Lekima and Bavi (the black solid line is the relation derived from black scatter points(R1h>5 mm·h-1), colorful dashed lines are for different cases), (c)the contribution of raindrops in different size to Nt in different rain rate, (d)the same as in Fig. 1c, but for rainfall(R)
图 7 对流性降水区域(图 3中方框) 主要粒子相态及固态水含量和液态水含量的时间-高度分布
(利奇马为2019年8月11日03:00—13:00，巴威为2020年8月26日08:00—15:00)
Fig. 7 Dominant hydrometeor class profile and average profiles of ice water content and liquid water content in the convective area (the box in Fig. 3) of Typhoon Lekima
(from 0300 BT to 1300 BT on 11 Aug 2019) and Typhoon Bavi (from 0800 BT to 1500 BT on 26 Aug 2020)
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