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Diurnal Variation in the Vertical Profile of the Raindrop Size Distribution for Stratiform Rain as Inferred from Micro Rain Radar Observations in Sumatra
Advances in Atmospheric Sciences ( IF 6.5 ) Pub Date : 2020-07-02 , DOI: 10.1007/s00376-020-9176-9
Ravidho Ramadhan , Marzuki , Mutya Vonnisa , Harmadi , Hiroyuki Hashiguchi , Toyoshi Shimomai

The diurnal variation in the vertical structure of the raindrop size distribution (RSD) associated with stratiform rain at Kototabang, West Sumatra (0.20°S, 100.32°E), was investigated using micro rain radar (MRR) observations from January 2012 to August 2016. Along with the MRR data, the RSD from an optical disdrometer and vertical profile of precipitation from the Tropical Rainfall Measuring Mission were used to establish the microphysical characteristics of diurnal rainfall. Rainfall during 0000–0600 LST and 1800–2400 LST had a lower concentration of small drops and a higher concentration of large drops when compared to rainfall during the daytime (0600–1800 LST). The RSD stratified on the basis of rain rate (R) showed a lower total concentration of drops and higher mass-weighted mean diameter in 0000–0600 LST and 1800–2400 LST than in the daytime. During the daytime, the RSD is likely governed by a riming process that can be seen from a weak bright band (BB). On the other hand, during 0000–0600 LST and 1800–2400 LST, the BB was stronger and the rainfall was associated with a higher concentration of midsize and large drops, which could be attributed to more active aggregation right above the melting layer with minimal breakup. Diurnal variation in the vertical profile of RSD led to a different radar reflectivity (Z)-R relationship in the rain column, in which Z during the periods 0000–0600 LST and 1800–2400 LST was larger than at the other times, for the same R.

中文翻译:

从苏门答腊微雨雷达观测推断的层状雨雨滴大小分布垂直剖面的日变化

2012 年 1 月至 2016 年 8 月,使用微雨雷达 (MRR) 观测研究了与西苏门答腊 Kototabang(0.20°S,100.32°E)层状雨相关的雨滴尺寸分布(RSD)垂直结构的日变化. 与 MRR 数据一起,来自光学偏差计的 RSD 和来自热带降雨测量任务的降水垂直剖面被用来建立昼夜降雨的微物理特征。与白天 (0600-1800 LST) 的降雨相比,0000-0600 LST 和 1800-2400 LST 的降雨量较小,而大水滴的浓度较高。根据降雨率 (R) 分层的 RSD 显示,与白天相比,0000-0600 LST 和 1800-2400 LST 的雨滴总浓度较低,质量加权平均直径较高。在白天,RSD 可能受边缘过程控制,可以从弱亮带 (BB) 看到。另一方面,在 0000-0600 LST 和 1800-2400 LST 期间,BB 更强,降雨与更高浓度的中大水滴有关,这可能归因于融化层上方更活跃的聚集,最小分手。RSD 垂直剖面的日变化导致雨柱中不同的雷达反射率 (Z)-R 关系,其中 0000-0600 LST 和 1800-2400 LST 期间的 Z 大于其他时间,对于一样的R。RSD 可能受边缘过程控制,可以从弱亮带 (BB) 看到。另一方面,在 0000-0600 LST 和 1800-2400 LST 期间,BB 更强,降雨与更高浓度的中大水滴有关,这可能归因于融化层上方更活跃的聚集,最小分手。RSD 垂直剖面的日变化导致雨柱中不同的雷达反射率 (Z)-R 关系,其中 0000-0600 LST 和 1800-2400 LST 期间的 Z 大于其他时间,对于一样的R。RSD 可能受边缘过程控制,可以从弱亮带 (BB) 看到。另一方面,在 0000-0600 LST 和 1800-2400 LST 期间,BB 更强,降雨与更高浓度的中大水滴有关,这可能归因于融化层上方更活跃的聚集,最小分手。RSD 垂直剖面的日变化导致雨柱中不同的雷达反射率 (Z)-R 关系,其中 0000-0600 LST 和 1800-2400 LST 期间的 Z 大于其他时间,对于一样的R。这可能归因于熔化层正上方的更活跃的聚集,并且破裂最小。RSD 垂直剖面的日变化导致雨柱中不同的雷达反射率 (Z)-R 关系,其中 0000-0600 LST 和 1800-2400 LST 期间的 Z 大于其他时间,对于一样的R。这可能归因于熔化层正上方的更活跃的聚集,并且破裂最小。RSD 垂直剖面的日变化导致雨柱中不同的雷达反射率 (Z)-R 关系,其中 0000-0600 LST 和 1800-2400 LST 期间的 Z 大于其他时间,对于一样的R。
更新日期:2020-07-02
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