Vol.33, NO.1, 2022
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Li Xin, Zhang Lu. Formation mechanism and microphysics characteristics of heavy rainfall caused by northward-moving typhoons. J Appl Meteor Sci, 2022, 33(1): 29-42. DOI:  10.11898/1001-7313.20220103.
Citation: Li Xin, Zhang Lu. Formation mechanism and microphysics characteristics of heavy rainfall caused by northward-moving typhoons. J Appl Meteor Sci, 2022, 33(1): 29-42. DOI:  10.11898/1001-7313.20220103.
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Formation Mechanism and Microphysics Characteristics of Heavy Rainfall Caused by Northward-moving Typhoons

DOI: 10.11898/1001-7313.20220103

  • Qingdao Meteorological Bureau, Qingdao 266003

  • Received Date: 2021-08-08
  • Rev Recd Date: 2021-11-17
  • Publish Date: 2022-01-19
    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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  • 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)

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    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)

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    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)

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    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)

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    Fig. 5  Vertical probability distributions (the shaded) and average profiles (the black solid line) of ZH, ZDR, KDP in the convective area (the box in Fig. 3) of Typhoon Lekima and Typhoon Bavi

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    Fig. 6  Frequency of each hydrometer class changing with height in the convective area (the box in Fig. 3) of Typhoon Lekima and Typhoon Bavi

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    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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    • Received : 2021-08-08
    • Accepted : 2021-11-17
    • Published : 2022-01-19
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