华北积层混合云微物理特征的飞机观测分析及数值模拟研究
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摘要
利用国家科技支撑计划重点项目环北京地区三架飞机联合云探测试验数据，研究了2009年4月18日和5月1日两次积层混合云中冰晶形态、分布与增长过程，依据观测结果，考察了中尺度数值模式对积层混合云云物理及降水过程的模拟能力。研究结果表明：
飞机在0－-16oC范围的云层内观测的冰晶形态主要包括板状、针柱状、柱帽状、辐枝状和不规则状。云中低层观测的冰晶形态受云顶温度影响，云顶温度不同，观测的冰晶形态不同，当云顶温度高于-8oC，在云中低层观测的冰晶形态以板状和针柱状为主，当云顶温度低于-13oC时，在云中低层可观测到辐枝状冰晶，当云顶温度低于-18oC时，在云中低层可观测到柱帽状冰晶。同时冰晶形态还受其所处云中位置的影响，不同云区采集的冰晶形态都是多形态的混合，但是对流区域能够采集到更多的辐枝状冰晶和冰晶聚合体，同时冰晶的凇附程度高于层云区域，而层云区域能够采集到清晰的六角板状冰晶；在融化层以上，冰晶的增长过程主要包括凝华、凇附和聚合过程，在垂直方向上，随着高度降低云中过冷水增多，冰晶的凇附增长也相应增强。积层混合云中的对流区和层云区粒子谱下落拓宽速率有明显差别，在4.8－4.2km（-11.6－-8℃）高度层，对流区粒子谱拓宽速率为3mm km-1，而层云区为3.67mm km-1，层云中粒子拓宽增长的速率略高于对流区；而在4.2－3.6km（-8－-5℃）高度层，对流区的粒子谱拓宽速率为6.67mm km-1，层云区为2.33mm km-1，对流区的粒子拓宽增长速率是层云区的近三倍，主要原因是嵌入对流区的低层含有较多过冷水。
数值模拟实验表明，WRF模式能够较准确地模拟出两次积层混合云雷达回波和降水的不均匀性分布特征，模拟的强降水中心的降水量与实况比较一致。对于积层混合云中液态水含量（LWC）的模拟，虽然两次模拟过程中,由于模拟嵌入对流位置的误差，导致在高层（-8－-16℃）飞机轨迹上的LWC模拟有细微误差，但总体上模式能够模拟出积层混合云LWC分布特征，尤其是对中下层LWC的模拟。对于积层混合云中冰水含量（IWC）的模拟，模拟的IWC高于实测值，主要原因是模拟的雪粒子凇附增长较大，而碰并增长过程发生的高度偏高，说明模式在雪粒子凇附增长过程和碰并增长过程处理上存在一些问题，有待改进。而在积层混合云中下层，模式能够较准确模拟云中水凝物的垂直分布，包括融化层的分布。
在云中粒子谱的对比方面，对于4月18日过程，WRF模式模拟的粒子谱参数在云低层与观测具有较好的一致性，但在高层比观测值偏小。在-8℃层，模式计算的粒子谱的截距和斜率都小于实际观测值，主要与该层模式模拟的雪粒子质量浓度偏高有关，在-5℃层，模式计算的截距和斜率接近实际谱，在3℃层，模式计算的斜率接近实际谱，但是截距大于实际谱。同时，随着高度从-8℃层降到3℃层，由于降水粒子的聚合过程和碰并过程，云中的小粒子端粒子浓度逐渐减少，云中降水粒子谱分布逐渐从MP分布转变为Gamma分布。5月1日过程的对比结果与4月18日类似，也是由于模拟的高层雪粒子质量浓度偏高，导致计算的粒子谱斜率小于实际谱斜率。同时在云中随着高度的降低，云中粒子谱分布也表现出从MP分布转变为Gamma分布。另外在积云区和层云区粒子谱分布的对比方面，模拟的积云区粒子谱分布更加接近实测，而层云区粒子谱分布与实测差异较大，同时模式在积云区和层云区计算的粒子谱拓宽速率都小于实际的粒子谱拓宽速率。两次模拟实验的对比结果表明，WRF模式在云冰相过程的参数化描述方面仍然存在较大的问题，特别是雪粒子的凇附增长过程和碰并增长过程，同时模式中降水粒子谱参数的描述方案有待改进，模式中谱形参数μ不应一直设置为0，而是应该随着高度变化而变化。
Ice crystal habits, distribution and growth process in two cases of stratiform clouds withembedded convection on18April2009and1st May2009are analyzed with data observedduring the Beijing Cloud Experiment (BCE), and then, to verify the cloud microphysicalscheme and ability in simulating cloud microphysics, thecloud microphysics and precipitationcharacteristics intwo cases simulated by WRF modelwere compared with data observedduring the BCE. The results show that:
Ice crystal habits in clouds with temperature between0－-16oC were predominantlyplate, needle-column, capped-column, dendrite and irregular. Ice crystal habits were affectedby the cloud top temperature(CTT) and were different with the change of CTT, plate andneedle-columns were predominant habits as CTT warmer than-8oC, but dendritic andcapped-column crystals were observed just as CTT colder than-13oC and-18oC respectively.At the same time,ice crystal habits were also affected by their locations in cloud. A mixture ofseveral ice crystal habits always be recorded in different clouds. But the ice crystal habitsrecorded in embedded convections contained more dendrites and had a heavier riming degree,and the ice crystal recorded in stratiform clouds contained more hexagonal plate crystals.Above the melting layer, ice particle grew mainly by deposition,riming and aggregationprocess,the riming process became more intense in lower cloud layer due to the increase ofsupercooled liquid water content. The broaden rate of Particle size distributions(PSDs) isobviously different between embedded convections and stratiform cloudsin the verticaldirection, at levels4.84.2km(-11.6－-8℃), the PSDs broaden rate in embeddedconvections is3mm km-1,smaller than3.67mm km-1in stratiform clouds, but at levels4.2－3.6km(-8－-5℃), the PSDs broaden rate in embedded convections is6.67mm km-1,whichwas almost three times as big as2.33mm km-1in stratiform clouds, which is mainly due tothat embedded convections had more supercooled liquid water than stratiform cloudsat levels4.2－3.6km.
The simulated results show that the distributions of radar echo and precipitationsimulated by WRF model are in good agreement with observations. The simulated verticaldistribution of Liquid Water Content (LWC) is consistent with aircraft measurements,especialy at middle and low layer of cloud, although the simulated LWC at high layer（-8－-16℃）flight path has some errors with observation due to the location error of embedded convection simulated by model. The Ice Water Content (IWC) at high layer simulated bymodel is higher than observation due to that the simulated riming process is stronger at thislayer, and aggregation process occurred at higher layer, so it needs an improvement atproduction processes of snow. Vertical distributions of water content at middle and low layer(most of cloud water is LWC) are simulated correctly,including the melting layer.
For the case of18April, at-8℃layer, both the intercept and slope of Particle sizedistributions(PSDs) simulated by model are lower than observations due to simulated snowmass concentration is higher than observed. At-5℃layer, both simulated intercept and slopeare consistent with observations. At3℃layer, the simulated slope is consistent withobservation, but the simulated intercept is higher than observation due to concentration ofsmall particles is decreasing in cloud, that suggest the parameter of spectrum shape shoudchange with height in cloud. For the case of1st May, the comparation results were similarwith the case of18April, the simulated slope of PSDs at high layer is smaller thanobservation due to more snow content were simulated at high layer. With the decrease ofheight, the PSDs changed from MP distribution to Gamma distribution. In addition, thesimulated results at embedded convection were closer to observation, and at stratiform regionwere higher than observation. In addition, the simulated broadening rate of PSDs inembedded convection and stratiform region both were smaller than the observed results. Twonumerical experiments suggest that there is a problem with the parameter of ice process incloud physical scheme in WRF model, especialy at riming process and collision process. Atthe same time, the parameter of spectrum shape of PSDs should change with height in cloud.
飞机在0－-16oC范围的云层内观测的冰晶形态主要包括板状、针柱状、柱帽状、辐枝状和不规则状。云中低层观测的冰晶形态受云顶温度影响，云顶温度不同，观测的冰晶形态不同，当云顶温度高于-8oC，在云中低层观测的冰晶形态以板状和针柱状为主，当云顶温度低于-13oC时，在云中低层可观测到辐枝状冰晶，当云顶温度低于-18oC时，在云中低层可观测到柱帽状冰晶。同时冰晶形态还受其所处云中位置的影响，不同云区采集的冰晶形态都是多形态的混合，但是对流区域能够采集到更多的辐枝状冰晶和冰晶聚合体，同时冰晶的凇附程度高于层云区域，而层云区域能够采集到清晰的六角板状冰晶；在融化层以上，冰晶的增长过程主要包括凝华、凇附和聚合过程，在垂直方向上，随着高度降低云中过冷水增多，冰晶的凇附增长也相应增强。积层混合云中的对流区和层云区粒子谱下落拓宽速率有明显差别，在4.8－4.2km（-11.6－-8℃）高度层，对流区粒子谱拓宽速率为3mm km-1，而层云区为3.67mm km-1，层云中粒子拓宽增长的速率略高于对流区；而在4.2－3.6km（-8－-5℃）高度层，对流区的粒子谱拓宽速率为6.67mm km-1，层云区为2.33mm km-1，对流区的粒子拓宽增长速率是层云区的近三倍，主要原因是嵌入对流区的低层含有较多过冷水。
数值模拟实验表明，WRF模式能够较准确地模拟出两次积层混合云雷达回波和降水的不均匀性分布特征，模拟的强降水中心的降水量与实况比较一致。对于积层混合云中液态水含量（LWC）的模拟，虽然两次模拟过程中,由于模拟嵌入对流位置的误差，导致在高层（-8－-16℃）飞机轨迹上的LWC模拟有细微误差，但总体上模式能够模拟出积层混合云LWC分布特征，尤其是对中下层LWC的模拟。对于积层混合云中冰水含量（IWC）的模拟，模拟的IWC高于实测值，主要原因是模拟的雪粒子凇附增长较大，而碰并增长过程发生的高度偏高，说明模式在雪粒子凇附增长过程和碰并增长过程处理上存在一些问题，有待改进。而在积层混合云中下层，模式能够较准确模拟云中水凝物的垂直分布，包括融化层的分布。
在云中粒子谱的对比方面，对于4月18日过程，WRF模式模拟的粒子谱参数在云低层与观测具有较好的一致性，但在高层比观测值偏小。在-8℃层，模式计算的粒子谱的截距和斜率都小于实际观测值，主要与该层模式模拟的雪粒子质量浓度偏高有关，在-5℃层，模式计算的截距和斜率接近实际谱，在3℃层，模式计算的斜率接近实际谱，但是截距大于实际谱。同时，随着高度从-8℃层降到3℃层，由于降水粒子的聚合过程和碰并过程，云中的小粒子端粒子浓度逐渐减少，云中降水粒子谱分布逐渐从MP分布转变为Gamma分布。5月1日过程的对比结果与4月18日类似，也是由于模拟的高层雪粒子质量浓度偏高，导致计算的粒子谱斜率小于实际谱斜率。同时在云中随着高度的降低，云中粒子谱分布也表现出从MP分布转变为Gamma分布。另外在积云区和层云区粒子谱分布的对比方面，模拟的积云区粒子谱分布更加接近实测，而层云区粒子谱分布与实测差异较大，同时模式在积云区和层云区计算的粒子谱拓宽速率都小于实际的粒子谱拓宽速率。两次模拟实验的对比结果表明，WRF模式在云冰相过程的参数化描述方面仍然存在较大的问题，特别是雪粒子的凇附增长过程和碰并增长过程，同时模式中降水粒子谱参数的描述方案有待改进，模式中谱形参数μ不应一直设置为0，而是应该随着高度变化而变化。
Ice crystal habits, distribution and growth process in two cases of stratiform clouds withembedded convection on18April2009and1st May2009are analyzed with data observedduring the Beijing Cloud Experiment (BCE), and then, to verify the cloud microphysicalscheme and ability in simulating cloud microphysics, thecloud microphysics and precipitationcharacteristics intwo cases simulated by WRF modelwere compared with data observedduring the BCE. The results show that:
Ice crystal habits in clouds with temperature between0－-16oC were predominantlyplate, needle-column, capped-column, dendrite and irregular. Ice crystal habits were affectedby the cloud top temperature(CTT) and were different with the change of CTT, plate andneedle-columns were predominant habits as CTT warmer than-8oC, but dendritic andcapped-column crystals were observed just as CTT colder than-13oC and-18oC respectively.At the same time,ice crystal habits were also affected by their locations in cloud. A mixture ofseveral ice crystal habits always be recorded in different clouds. But the ice crystal habitsrecorded in embedded convections contained more dendrites and had a heavier riming degree,and the ice crystal recorded in stratiform clouds contained more hexagonal plate crystals.Above the melting layer, ice particle grew mainly by deposition,riming and aggregationprocess,the riming process became more intense in lower cloud layer due to the increase ofsupercooled liquid water content. The broaden rate of Particle size distributions(PSDs) isobviously different between embedded convections and stratiform cloudsin the verticaldirection, at levels4.84.2km(-11.6－-8℃), the PSDs broaden rate in embeddedconvections is3mm km-1,smaller than3.67mm km-1in stratiform clouds, but at levels4.2－3.6km(-8－-5℃), the PSDs broaden rate in embedded convections is6.67mm km-1,whichwas almost three times as big as2.33mm km-1in stratiform clouds, which is mainly due tothat embedded convections had more supercooled liquid water than stratiform cloudsat levels4.2－3.6km.
The simulated results show that the distributions of radar echo and precipitationsimulated by WRF model are in good agreement with observations. The simulated verticaldistribution of Liquid Water Content (LWC) is consistent with aircraft measurements,especialy at middle and low layer of cloud, although the simulated LWC at high layer（-8－-16℃）flight path has some errors with observation due to the location error of embedded convection simulated by model. The Ice Water Content (IWC) at high layer simulated bymodel is higher than observation due to that the simulated riming process is stronger at thislayer, and aggregation process occurred at higher layer, so it needs an improvement atproduction processes of snow. Vertical distributions of water content at middle and low layer(most of cloud water is LWC) are simulated correctly,including the melting layer.
For the case of18April, at-8℃layer, both the intercept and slope of Particle sizedistributions(PSDs) simulated by model are lower than observations due to simulated snowmass concentration is higher than observed. At-5℃layer, both simulated intercept and slopeare consistent with observations. At3℃layer, the simulated slope is consistent withobservation, but the simulated intercept is higher than observation due to concentration ofsmall particles is decreasing in cloud, that suggest the parameter of spectrum shape shoudchange with height in cloud. For the case of1st May, the comparation results were similarwith the case of18April, the simulated slope of PSDs at high layer is smaller thanobservation due to more snow content were simulated at high layer. With the decrease ofheight, the PSDs changed from MP distribution to Gamma distribution. In addition, thesimulated results at embedded convection were closer to observation, and at stratiform regionwere higher than observation. In addition, the simulated broadening rate of PSDs inembedded convection and stratiform region both were smaller than the observed results. Twonumerical experiments suggest that there is a problem with the parameter of ice process incloud physical scheme in WRF model, especialy at riming process and collision process. Atthe same time, the parameter of spectrum shape of PSDs should change with height in cloud.
引文
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