热带气旋内外雨带结构、外雨带生成和准周期活动
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摘要
本论文利用高分辨率理想数值模式（TCM4）分析了热带气旋螺旋内外雨带的结构特征、外雨带形成机制及其准周期活动，此外也研究了准周期外雨带活动对热带气旋结构和强度的影响。
文中首先系统性地比较了控制试验中模拟的内雨带和外雨带结构和活动的异同。内雨带通常活跃在眼壁外的快速涡丝化带中，而外雨带则活跃在3倍最大风半径外区域。内雨带具有对流耦合涡旋Rossby波特征。外雨带的移动与低层风矢量有关，即沿着轴平均低层风和下沉运动导致的边界层冷池产生的径向向外跨雨带非对称风矢量移动。外雨带中的对流单体呈现典型的对流系统特征，在较大（小）半径处切向方向气旋式运动，径向上向外（里）移动。向上的净垂直质量输送在内雨带区域贯穿整个对流层，而在外雨带区域向下的净质量输送出现在4km高度以下。在内雨带区域仅只有非常浅薄的净水平辐合层位于2-km以下，外雨带区域则在7.5km高度以下为净辐合，以上为净辐散。内雨带中存在两个切向风大值区，一个位于入流边界层顶，另一个位于出流层底。在外雨带内侧边缘4km高度存在次级水平风大值。外雨带上游、中游和下游部分的结构也存在明显差异。
控制试验中模拟的外螺旋雨带通常在60km半径（约为3倍最大风半径）附近生成，生成后它们通常以约5m s-1的速度径向向外传播。外雨带的生成呈显准周期性，周期约为22-26小时。内雨带与对流耦合的涡旋Rossby波有关，因此其生成主要是涡旋Rossby波的激发，但外雨带的形成则更为复杂。外雨带生成位置主要由快速涡丝化过程对深对流的抑制作用同触发深对流所需动力和热力条件之间的平衡所决定。
控制试验中外雨带的准周期活动与边界层从对流消耗CAPE以及对流下沉的影响中恢复过程有着紧密关系。一旦外雨带生成，雨带中的对流会产生强烈的干冷下沉运动并消耗CAPE，这将减弱外雨带生成位置附近的对流。随着外雨带向外传播以及对流消亡，外雨带生成附近的边界层通过从洋面吸收能量历经大约10小时逐渐恢复，此后新的对流和外雨带将生成。然后上述物理过程重复发生，形成外雨带的准周期活动。随着外雨带的准周期活动，模拟的热带气旋强度也经历类似的准周期振荡，其强度或增强率在外雨带生成后约4小时开始减小。上述结果为热带气旋中观测到的准周期（准一天）强度和出流层云砧变化提供了另一种可能的解释。
为研究外核区地表熵通量对外雨带活动的影响，我们设计了两个敏感性试验，分别将外核区地表熵通量各人为地增加和减小20%。这两个试验结果也显示了准周期的外雨带活动。加强的径向风导致的负的水平平流作用以及非对称涡动导致的正的作用使得地表熵通量增强试验中外雨带活动的周期更长。同控制试验结果一致，地表熵通量减小试验中模拟的外雨带活动明显地抑制气旋强度，然而地表熵通量增强试验中外雨带对强度的影响则不显著。外雨带中的非绝热加热可以增强外核区切向风，进而增大内核尺度，因此准周期的外雨带活动也会导致热带气旋内核区尺度的准周期变化。
The structures of inner and outer spiral rainbands, the formation mechanism andquasi-periodic nature of the outer rainbands simulated with TCM4in a quiescent environmentare investigated in the thesis, and the impact of quasi-periodic behavior of the simulated outerrainbands on tropical cyclone (TC) structure and intensity is examined as well.
The simulated inner and outer spiral rainbands in the control simulation (CTL) are firstcompared. The inner rainbands are generally active immediately outside the eyewall in therapid filamentation zone, while the outer rainbands are active in regions outside about3timesthe radius of maximum wind. The inner rainbands are characterized by the convectivelycoupled vortex Rossby waves (VRWs). The movement of the outer rainbands follows thelow-level vector winds associated with the azimuthally averaged low-level flow and theradially outward cross-band flow caused by the downdraft-induced cold pool in the boundarylayer. Convective cells in outer rainbands are typical of convective systems and movecyclonically and radially outward (inward) at large (small) radii. Net upward vertical masstransports (VMTs) appear throughout the depth of the troposphere in the whole inner-rainbandregion, while net downward VMTs are found below4km height in the outer-rainband region.In the whole inner-rainband region, only a very shallow layer with net horizontal convergenceappears below2-km height, while a deep layer with net convergence is found below7.5-kmheight with net divergence aloft in the outer-rainband region. The inner rainband shows twotangential wind maxima, respectively, located near the top of the inflow boundary layer and immediately below the upper tropospheric outflow layer. A secondary horizontal windmaximum occurs at about4-km height on the inner edge of the outer rainband. Distinctfeatures of the upwind, middle, and downwind sectors of the outer rainband are alsodiscussed.
In CTL, outer spiral rainbands are preferably initiated near the60-km radius, or roughlyabout three times the radius of maximum wind (RMW). After initiation, they generallypropagate radially outward with a mean speed of~5m s-1. They are reinitiatedquasi-periodically with a period between22h and26h in the simulation. While the innerspiral rainbands, which form within a radius of about three times the RMW, are characterizedby the convectively coupled VRWs, the formation of outer spiral rainbands, namely,rainbands formed outside a radius of about three times the RMW, is much more complicated.It is shown that outer spiral rainbands are triggered by the inner-rainband remnantsimmediately outside the rapid filamentation zone and inertial instability in the uppertroposphere. The preferred radial location of initiation of outer spiral rainbands is understoodas a balance between the suppression of deep convection by rapid filamentation and thefavorable dynamical and thermodynamic conditions for initiation of deep convection.
The quasi-periodic occurrence of the outer spiral rainbands simulated in CTL is found tobe associated with the boundary layer recovery from the effect of convective downdrafts andthe consumption of convective available potential energy (CAPE) by convection in theprevious outer spiral rainbands. Specifically, once convection is initiated and organized in theform of outer spiral rainbands, it will produce strong downdrafts and consume CAPE. Theseeffects weaken convection near its initiation location. As the rainband propagates outwardfurther, the boundary layer air near the original location of convection initiation takes about10h to recover by extracting energy from the underlying ocean. Convection and thus newouter spiral rainbands will be initiated near a radius of about three times the RMW. This willbe followed by a similar outward propagation and the subsequent boundary layer recovery,leading to a quasi-periodic occurrence of outer spiral rainbands. In response to thequasi-periodic appearance of outer spiral rainbands, the storm intensity experiences a similarquasi-periodic oscillation with its intensity or intensification rate starting to decrease after about4h of the initiation of an outer spiral rainband. The results provide an alternativeexplanation or one of the mechanisms that are responsible for the quasi-periodic(quasi-diurnal) variation in the intensity and in the area of outflow-layer cloud canopy ofobserved TCs.
The influence of outer-core surface entropy fluxes (SEFs) on outer rainband activity isinvestigated through conducting sensitivity numerical experiments. The sensitivityexperiments with the outer-core SEF artificially increased and decreased by20%, respectively,also simulate quasi-periodic outer rainband behavior. The larger negative horizontal advectiondue to the greater radial wind and the positive contribution by asymmetric eddies lead to alonger period of outer rainband activity in the SEF-enhanced experiment. The activity ofhealthy outer rianbands in the SEF-reduced simulation significantly limits the TC intensity,whereas such an intensity suppression influence is not pronounced in the SEF-enhancedexperiment. As diabatic heating in outer rainbands enables to strengthen the outer-coretangential wind, the quasi-periodic activity of outer rainbands contributes to thequasi-periodic variations of the inner-core size of the TCs.
文中首先系统性地比较了控制试验中模拟的内雨带和外雨带结构和活动的异同。内雨带通常活跃在眼壁外的快速涡丝化带中，而外雨带则活跃在3倍最大风半径外区域。内雨带具有对流耦合涡旋Rossby波特征。外雨带的移动与低层风矢量有关，即沿着轴平均低层风和下沉运动导致的边界层冷池产生的径向向外跨雨带非对称风矢量移动。外雨带中的对流单体呈现典型的对流系统特征，在较大（小）半径处切向方向气旋式运动，径向上向外（里）移动。向上的净垂直质量输送在内雨带区域贯穿整个对流层，而在外雨带区域向下的净质量输送出现在4km高度以下。在内雨带区域仅只有非常浅薄的净水平辐合层位于2-km以下，外雨带区域则在7.5km高度以下为净辐合，以上为净辐散。内雨带中存在两个切向风大值区，一个位于入流边界层顶，另一个位于出流层底。在外雨带内侧边缘4km高度存在次级水平风大值。外雨带上游、中游和下游部分的结构也存在明显差异。
控制试验中模拟的外螺旋雨带通常在60km半径（约为3倍最大风半径）附近生成，生成后它们通常以约5m s-1的速度径向向外传播。外雨带的生成呈显准周期性，周期约为22-26小时。内雨带与对流耦合的涡旋Rossby波有关，因此其生成主要是涡旋Rossby波的激发，但外雨带的形成则更为复杂。外雨带生成位置主要由快速涡丝化过程对深对流的抑制作用同触发深对流所需动力和热力条件之间的平衡所决定。
控制试验中外雨带的准周期活动与边界层从对流消耗CAPE以及对流下沉的影响中恢复过程有着紧密关系。一旦外雨带生成，雨带中的对流会产生强烈的干冷下沉运动并消耗CAPE，这将减弱外雨带生成位置附近的对流。随着外雨带向外传播以及对流消亡，外雨带生成附近的边界层通过从洋面吸收能量历经大约10小时逐渐恢复，此后新的对流和外雨带将生成。然后上述物理过程重复发生，形成外雨带的准周期活动。随着外雨带的准周期活动，模拟的热带气旋强度也经历类似的准周期振荡，其强度或增强率在外雨带生成后约4小时开始减小。上述结果为热带气旋中观测到的准周期（准一天）强度和出流层云砧变化提供了另一种可能的解释。
为研究外核区地表熵通量对外雨带活动的影响，我们设计了两个敏感性试验，分别将外核区地表熵通量各人为地增加和减小20%。这两个试验结果也显示了准周期的外雨带活动。加强的径向风导致的负的水平平流作用以及非对称涡动导致的正的作用使得地表熵通量增强试验中外雨带活动的周期更长。同控制试验结果一致，地表熵通量减小试验中模拟的外雨带活动明显地抑制气旋强度，然而地表熵通量增强试验中外雨带对强度的影响则不显著。外雨带中的非绝热加热可以增强外核区切向风，进而增大内核尺度，因此准周期的外雨带活动也会导致热带气旋内核区尺度的准周期变化。
The structures of inner and outer spiral rainbands, the formation mechanism andquasi-periodic nature of the outer rainbands simulated with TCM4in a quiescent environmentare investigated in the thesis, and the impact of quasi-periodic behavior of the simulated outerrainbands on tropical cyclone (TC) structure and intensity is examined as well.
The simulated inner and outer spiral rainbands in the control simulation (CTL) are firstcompared. The inner rainbands are generally active immediately outside the eyewall in therapid filamentation zone, while the outer rainbands are active in regions outside about3timesthe radius of maximum wind. The inner rainbands are characterized by the convectivelycoupled vortex Rossby waves (VRWs). The movement of the outer rainbands follows thelow-level vector winds associated with the azimuthally averaged low-level flow and theradially outward cross-band flow caused by the downdraft-induced cold pool in the boundarylayer. Convective cells in outer rainbands are typical of convective systems and movecyclonically and radially outward (inward) at large (small) radii. Net upward vertical masstransports (VMTs) appear throughout the depth of the troposphere in the whole inner-rainbandregion, while net downward VMTs are found below4km height in the outer-rainband region.In the whole inner-rainband region, only a very shallow layer with net horizontal convergenceappears below2-km height, while a deep layer with net convergence is found below7.5-kmheight with net divergence aloft in the outer-rainband region. The inner rainband shows twotangential wind maxima, respectively, located near the top of the inflow boundary layer and immediately below the upper tropospheric outflow layer. A secondary horizontal windmaximum occurs at about4-km height on the inner edge of the outer rainband. Distinctfeatures of the upwind, middle, and downwind sectors of the outer rainband are alsodiscussed.
In CTL, outer spiral rainbands are preferably initiated near the60-km radius, or roughlyabout three times the radius of maximum wind (RMW). After initiation, they generallypropagate radially outward with a mean speed of~5m s-1. They are reinitiatedquasi-periodically with a period between22h and26h in the simulation. While the innerspiral rainbands, which form within a radius of about three times the RMW, are characterizedby the convectively coupled VRWs, the formation of outer spiral rainbands, namely,rainbands formed outside a radius of about three times the RMW, is much more complicated.It is shown that outer spiral rainbands are triggered by the inner-rainband remnantsimmediately outside the rapid filamentation zone and inertial instability in the uppertroposphere. The preferred radial location of initiation of outer spiral rainbands is understoodas a balance between the suppression of deep convection by rapid filamentation and thefavorable dynamical and thermodynamic conditions for initiation of deep convection.
The quasi-periodic occurrence of the outer spiral rainbands simulated in CTL is found tobe associated with the boundary layer recovery from the effect of convective downdrafts andthe consumption of convective available potential energy (CAPE) by convection in theprevious outer spiral rainbands. Specifically, once convection is initiated and organized in theform of outer spiral rainbands, it will produce strong downdrafts and consume CAPE. Theseeffects weaken convection near its initiation location. As the rainband propagates outwardfurther, the boundary layer air near the original location of convection initiation takes about10h to recover by extracting energy from the underlying ocean. Convection and thus newouter spiral rainbands will be initiated near a radius of about three times the RMW. This willbe followed by a similar outward propagation and the subsequent boundary layer recovery,leading to a quasi-periodic occurrence of outer spiral rainbands. In response to thequasi-periodic appearance of outer spiral rainbands, the storm intensity experiences a similarquasi-periodic oscillation with its intensity or intensification rate starting to decrease after about4h of the initiation of an outer spiral rainband. The results provide an alternativeexplanation or one of the mechanisms that are responsible for the quasi-periodic(quasi-diurnal) variation in the intensity and in the area of outflow-layer cloud canopy ofobserved TCs.
The influence of outer-core surface entropy fluxes (SEFs) on outer rainband activity isinvestigated through conducting sensitivity numerical experiments. The sensitivityexperiments with the outer-core SEF artificially increased and decreased by20%, respectively,also simulate quasi-periodic outer rainband behavior. The larger negative horizontal advectiondue to the greater radial wind and the positive contribution by asymmetric eddies lead to alonger period of outer rainband activity in the SEF-enhanced experiment. The activity ofhealthy outer rianbands in the SEF-reduced simulation significantly limits the TC intensity,whereas such an intensity suppression influence is not pronounced in the SEF-enhancedexperiment. As diabatic heating in outer rainbands enables to strengthen the outer-coretangential wind, the quasi-periodic activity of outer rainbands contributes to thequasi-periodic variations of the inner-core size of the TCs.
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