Relationship between Snowfall in the Yanqing Zone of Winter Olympic Games and the Easterly Wind in the Boundary Layer
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摘要: 受特殊地理环境影响，北京地区冬季降雪常与边界层东风相伴，边界层东风所引起的水汽输送和动力辐合效应对降雪发生发展有重要意义。不同于已有边界层东风对平原地区降雪影响的研究，本文结合2022年冬奥会北京延庆赛区的地形特征，对比相似天气背景下不同温湿特性、不同发展高度的边界层东风对降雪的作用机制，研究表明：（1）途经渤海湾的路径较长有利于边界层东风的明显增湿，反之增湿效果则较弱；（2）“干冷”性质的偏东风可形成冷垫抬升北京平原及低海拔地区的暖湿空气；当偏东风在垂直方向发展较为深厚（600 m以上）时，能够翻越延庆东部海拔较低的军都山并在背风坡形成绕流汇合，同时受西部海拔较高的海陀山阻挡，形成迎风坡的强迫抬升，二者共同作用导致延庆区的辐合东强西弱，进而造成降雪分布呈东多西少的特征；（3）“暖湿”性质的边界层东风因垂直延展高度较低，无法向西越过军都山，对延庆赛区降雪基本无影响；（4）空中500 hPa为西北气流影响时，除考虑边界层东风能否越山之外，若存在与地形高度接近的、700 hPa高度附近饱和区与抬升运动的有利配合，将导致延庆赛区的高海拔山区出现明显降雪。Abstract: Affected by the special geographical environment, winter snowfall in Beijing is often accompanied by the easterly wind in the boundary layer. The water vapor transport and dynamic convergence effect caused by the easterly wind in the boundary layer are of great significance to the occurrence and development of snowfall. This paper is based on the topographic characteristics of the Yanqing zone of the 2022 Winter Olympic Games and is different from the existing snowfall studies on the easterly wind of boundary layer in plain areas. The paper compared the easterly wind mechanism in the boundary layer with various thermal and humidity properties and development heights on snowfall under similar weather conditions. The results show that: (1) A longer route through the Bohai Bay is beneficial to the obvious humidification of the boundary layer easterly wind and vice versa. (2) The “dry and cold” easterly wind can form a cold pad to lift the warm and humid air in the Beijing plain area. When the easterly wind develops deep in the vertical direction (over 600 m), it can overturn the Jundu mountain with lower altitudes in eastern Yanqing and form a around-flow confluence on leeward slopes. At the same time, the easterly wind is blocked by the Haituo mountain with higher altitudes in the west, forming the forced uplift of the windward slope. The two effects together lead to the convergence of the strong east and the weak west, which causes more snowfall distribution in the east than in the west. (3) The “warm and humid” boundary-layered easterly wind cannot cross the Jundu mountain westward because of its lower vertical development height, which has little effect on snow in Yanqing. (4) When the air gets affected by the northwest airflow of 500 hPa, closer to the terrain, the saturation area near the 700 hPa height and the lifting movement make the high-altitude mountainous area of Yanqing experience the obvious snowfall.
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图 2 （a、b）2015年11月21日08:00和（c、d）2016年1月21日08:00 500 hPa环流形势（左列；等值线为位势高度场，单位：dagpm；风羽，单位：m s−1）以及海平面气压场（右列；等值线，单位：hPa）分布
Figure 2. Distributions of (a, c) synoptic situation at 500 hPa (contours for geopotential, units: dagpm; barbs for wind, units: m s−1) and (b, d) sea level pressure (contours, units: hPa) at 0800 BJT (Beijing time) on (a, b) November 21, 2015 and (c, d) January 21, 2016
图 3 （a、c）2015年11月21日05:00～16:00和2016年1月21日08:00～18:00北京延庆区总降雪量分布（左列）以及（b、d）逐小时降雪量变化（右列），单位：mm
Figure 3. (a) Distributions of total snowfall amount, (b) variation of hourly snowfalls from 0500 BJT to 1600 BJT on November 21, 2015, units: mm. (c, d) are same as (a, b), but for 0800 BJT to 1800 BJT on January 21, 2016
图 4 （a）2015年11月20日20:00至21日20:00的温度（等值线，单位：°C）、相对湿度（阴影）和风场（箭头，单位：m s−1），（b）2015年11月21日08:00 1000 hPa比湿（等值线，单位：g kg−1）、风场（风向杆，单位：m s−1）及冷平流（阴影，单位：10−5 K s−1）
Figure 4. (a) Distributions of temperature (contours, units: °C), relative humidity (shaded) and wind (barb, units: m s−1) from 2000 BJT 20 to 2000 BJT 21 November 2015, (b) distributions of specific humidity (contours, units: g kg−1), wind (barb, units: m s−1) and cold advection (shade, units: 10−5 K·s−1) at 1000 hPa on 0800 BJT 21 November 2015
图 5 （a）2015年11月21日08:00沿（39.5°N，116.5°E）的96 h后向轨迹（绿色线为200 m，蓝色线为400 m，红色线为600 m），（b）气流后向轨迹对应的相对湿度
Figure 5. (a) Backward trajectories of 96 h at 0000 BJT 21 November 2015 along (39.5°N, 116.5°E) for 200 m (green line), 400 m (blue line) and 600 m (red line) , (b) the corresponding relative humidity of backward trajectory
图 6 （a）2016年1月20日20:00至21日20:00的温度（等值线，单位：°C）、相对湿度（阴影）和风场（箭头，单位：m s−1）分布，（b）2016年1月21日08:00 1000 hPa比湿（等值线，单位：g kg−1）、风场（风向杆，单位：m s−1）及暖平流（阴影，单位：10−5 K s−1）分布
Figure 6. (a) Distributions of temperature (contours, units: °C), relative humidity (shaded) and wind (barb, units: m s−1) from 2000 BJT 20 to 2000 BJT 21 2016, (b) distributions of specific humidity (contours, units: g kg−1), wind (barbs, units: m s−1) and warm advection (shaded, units: 10−5 K s−1) at 1000 hPa on 0800 BJT 21 January 2016
图 8 2015年11月21日（a）00:00～18:00延庆站风廓线（风向杆，单位：m s−1）以及（b）09:00沿40.4°N的垂直剖面（黑色粗实线为地形高度；红色虚线为温度，单位：°C；阴影为辐合区，单位：10−5 s−1；风向杆为水平流场，单位：m s−1）
Figure 8. (a) Wind profile from 0000 BJT to 1800 BJT on November 21, 2015 of the Yanqing station (barbs, units: m s−1), (b) the cross-section along 40.4°N at 0900 BJT on November 21, 2015. Black solid line for terrain height; red contours for temperature, units: °C; shaded for convergence, units: 10−5 s−1; barbs for horizontal wind, units: m s−1
图 9 2016年1月21日（a）00:00～18:00延庆站风廓线（风向杆，单位：m s−1），（b）09:00沿40.0°N的剖面（黑色粗实线为地形高度；红色虚线为温度，单位：°C；阴影为辐合区，单位：10−5 s−1；风向杆为水平流场，单位：m s−1）,（c）10:00至19:00沿（40.56°N，115.82°E）的风场（风向杆，单位：m s−1）、相对湿度（等值线）和上升运动（阴影，单位：Pa s−1）时序剖面
Figure 9. (a) Wind profile from 0000 BJT to 1800 BJT of the Yanqing station (barbs, units: m s−1), (b) the cross-section along 40.0°N at 0900 BJT (black solid lines for the terrain height; red contours for temperature, units: °C; shaded for convergence, units: 10−5 s−1; barb for horizontal wind, units: m s−1), (c) the cross-section of relative humidity (contours), wind (barb for wind，unit: m s−1) and ascending motion (shaded, units: Pa s−1) along (40.56°N, 115.82°E) from 1000 BJT to 1900 BJT on January 21, 2016
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