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Diurnal Evolution of the Urban Boundary Layer Structure During a Snow Process in Urumqi
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摘要: 利用Vaisala系留探空仪系统在2008年1月乌鲁木齐探测所得资料，分析了降雪和非降雪过程中温度、湿度和风的垂直结构及其变化特征。结果表明：降雪和非降雪天，白天对流边界层特征均较明显，但在暖气团影响下，对流边界层特征消失，出现深厚平流逆温，夜间多出现贴地逆温。白天平流逆温强度较夜间逆温更强，白天逆温层出现湿中心，上部出现干中心。降雪天湿中心高度低于非降雪天。夜间近地层出现微弱的逆湿现象，上部出现干中心，降雪天近地层逆湿现象比非降雪天弱；降雪天和非降雪天近地层风向分布均较散乱，主导风向为偏北风，高空主导风向为东南风。风速多因风向改变而出现极大值或极小值，其值常以“高-低-高-低”形式出现于特定高度，风速因风向变化呈波动状随高度递增。Abstract: For the purpose of studying the boundary layer characteristics in snowy day and non-snowy day of Urumqi, 20 times of continuous observations from 11 to 13 in January 2008 and 12 times non-snowy day's observations from 21 to 23 in January 2008 are conducted based upon the Vaisala tethered balloon in the middle of the city. The detecting elements include temperature, dew point, wind speed and wind direction etc. The potential temperature and depression of the dew point isoline and wind profile are studied for investigating the characteristics of the boundary layer and the influence of warm advection and snowing on the boundary layer.The convective boundary layer (CBL) is very typical with clear ultra-adiabatic lapse layer, mixed layer (ML) and capping inversion layer (CIL) in the daytime, and there tends to be a surface inversion during the nighttime. In fact, the temperature stratification isn't affected much by snowing. When the warm advection invades, an intense surface inversion occurs in the daytime, but it's still weaker than that in the nighttime. Furthermore, compared with the nighttime, the temperature inversion is even fiercer when warm advection approaches.In the CBL, vapor is blocked at the bottom of the CIL, forming a wet center, as height increases, vapor decreases to form a dry center. The height of the wet center in the snowing day is lower than usual. Under the influence of warm advection, large area of wet center appears near the ground surface. In the evening, weak humidity inversion occurs in the surface layer, besides, the upper layer has an obvious dry center.Although wind direction is dispersed in the surface layer, the main direction still can be estimated as "N". It changes by clockwise or anti-clockwise from the surface layer to the higher layer, the main direction in the upper air is "SE". The wind speed follows the "high-low-high-low" rule at certain heights, and the extreme speed appears at the height where wind direction shifts. In conclusion, wind speed tends to rise by fluctuates with wind direction shifts.
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图 1 乌鲁木齐2008年1月10日20:00 (a) 与11日20:00 (b) 500 hPa高度场 (单位：dagpm)
Fig. 1 500 hPa geopotential height at 20:00 10 January 2008 (a) and 20:00 11 January 2008 (b) (unit: dagpm)
图 2 2008年1月11—13日探测期位温垂直结构及其变化情况 (单位：℃)
Fig. 2 Evolution of the potential temperature structure during the detection period of 11—13 January 2008(unit:℃)
图 3 2008年1月11—13日探测期超绝热递减层顶与逆温层底高度 (a) 和逆温强度 (b)
Fig. 3 Ultra-adiabatic lapse layer tops and inversion layer bottoms (a) and inversion temperature strengths (b) during the detection period of 11—13 January 2008
图 4 2008年1月12日沿探测地点所在经度87.5°E温度平流的经向垂直剖面 (单位：10-5 ℃·s-1)
Fig. 4 The meridian-height section of temperature advection (unit: 10-5 ℃·s-1) along 87.5°E through the detection area on 12 January 2008
图 5 2008年1月11—13日探测期温度露点差垂直结构及变化情况 (单位：℃)
Fig. 5 Evolution of the depression of the dew point structure during the detection period of 11—13 January 2008(unit:℃)
图 6 2008年1月12日沿探测地点所在经度87.5°E相对湿度分布的经向垂直剖面 (单位：%)
Fig. 6 The meridian-height section of relative humidity along 87.5°E through the detection area on 12 January 2008(unit:%)
图 7 2008年1月11—13日探测期风速与风向廓线图
Fig. 7 Wind speed and direction profiles during the detection period of 11—13 January 2008
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