波浪对环流输运影响和涌浪传播耗散特征研究
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摘要
波浪往往被认为是时空尺度较小的现象。但是，由于波浪在时空上的持续性和普遍性，又会对较大尺度现象造成影响。本文研究了波浪的大尺度效应即波浪科氏-斯托克斯力（CSF）在上层海洋输送中的影响，尤其关注大洋涌浪在平均方向和波浪诱导的Stokes输运中的作用。从对波动中尺度较大的涌浪传播特征和耗散机制的研究中总结规律，并分析了海浪WW3模式在大洋涌浪模拟方面的性能。
涌浪对波浪诱导的Stokes输运有重要影响，特别对局地波浪的平均方向有所制约。全球Ekman输运主要呈带状分布，赤道海区两侧的信风带上Ekman输运的量值较大，可以的达到3m~2s以上；Ekman输运N-S分量Ty,E与整体量值分布一致，而W-E分量Tx,E受经向风作用呈带状倾斜。全球Stokes输运也主要为带状分布，尤其是两半球西风带的波浪输运量很大。而经向上的输运Ty,S，总的来看也基本呈现带状，但在大洋东侧却明显更强，体现了涌浪的作用。全球Stokes输运占Ekman输运的量值最大可达50%，太平洋和大西洋27.5N，30N和32.5N纬线的积分Ekman输运和Stokes输运有夏秋季强（向北）、冬春季弱（向南）的季节变化趋势，波浪输运不同海区不同季节有正贡献或负贡献。波浪Stokes经向输运沿27.5N，30N和32.5N的纬线积分值与Sverdrup关系估计的西边界流流量呈相似的季节变化，夏秋和冬春季相反；波浪导致的经向输运量值约为整体大洋输运的5到10%，在10月至4月为正贡献，5月至9月为负贡献。与SODA估计的黑潮流量相比，波浪作用可以达到5%。通过浪致表面应力来阐述波浪作用，发现波浪抽吸速度在中高纬海区较强，量值可达5cm/day，是波浪作用产生的源区。而风应力抽吸在副热带最强。各个大洋东西侧的波浪抽吸有局地的特征。
波浪中尺度较大的涌浪在西风带产生的源区可以近似为圆形和点源，长波以风暴生成区为中心以近似扇形散开，沿大圆传播。涌浪各分量以群速传播能量，周期越长的分量传播越快；涌浪平均周期可以较好的保留涌浪传播的信息。在横向上可以基本保持同样的扩散速度，但距离点源越远相关性越低。在海盆靠近陆地的区域由于地形变化，波浪发生折绕射较强，破坏了波峰线的连续性。在局地风较强的区域，涌浪依然会发生与局地风和波浪的相互作用。涌浪在传播过程中会发生能量的衰减，空间耗散率约为-4~5×10~(-7)m~(-1)。在离点源距离较近的6000km以内，风暴强度差异引起能量较离散；6000-12000km之间，涌浪的能量差异减小；当距点源距离大于12000km，能量又有所增加。不同周期的分量耗散率范围没有明显的差别，初始波陡越大，耗散率越大。涌浪能量耗散主要由于其与海气边界层湍应力相互作用和与混合层湍流作用引起耗散。波陡和反波龄是衡量耗散强度的主要参数。反波龄随波陡增加而增大，随周期增大，反波龄降低至-1~1，随着离点源距离增加反波龄增大。波陡δ=0.01处为一较明显的分界线，当δ <0.01时，反波龄在-1~1，正负相当，风速和波速方向同向和反向同样明显，且风速总小于波速；当δ>0.01，普遍倾向于反波龄γ>0，即风向与波向同向较多，且在周期较短的分量上依然有γ>1，风速大于或接近波速，涌浪依然受局地风的影响。
WW3的ACC350配置包含了有关涌浪耗散的物理现象的源函数项，模式对太平洋整体有效波高模拟较好，但约8米以上的波高模拟的有偏大趋势。4月的误差相对较大，12月误差最小；模式在中低纬带误差偏大较为明显。模式可以较好的进行大洋风浪的模拟，精确度较高。对涌浪的模拟波高偏大，整体来讲周期和波向的模拟比波高的精度高；模式对周期模拟的误差主要来自对涌浪周期的模拟误差，整体稍偏大。ACC350配置模式采用的基于涌浪耗散的物理模型可以部分改进BAJ模型涌浪波高模拟误差，尤其是在大洋中部较明显。模式的模拟能力需要依赖大量数据和对物理模型的认识进一步改进。
The persistency and extensiveness of small scale ocean waves makes themimportant to large scale ocean phenomena. In this dissertation, the wave-inducedCoriolis-Stokes effect in upper ocean water transport is analyzed, placing emphasis onocean swells. The large ocean swell transport and dissipation characteristics are alsodiscussed, together with model performance assessment of the newly publishedWavewatchIII v3.14on ocean swells.
Ocean swells are important to wave-induced Stokes transport, especially in theMean Wave Direction calculation. The global Ekman transports are band-likedistributed with maximums at Trade wind areas. The W-E components of the Ekmantransport tilt with longitudinal wind. The Stokes transports are also in band withmaximums at westerlies. The W-E components are large in the eastern parts of theoceans where swell are more dominant. The Stokes transport contributes to the Ekmantransport in50%at large; both of the integrated transports across three latitudesat27.5N,30Nand32.5Nare stronger in summer and autumn and weaker inwinter and spring. The Stokes transports are similar in seasonal variations withSverdrup transports along the three latitudes and occupy5to10%in magnitude, withcontributions from October to April and cancellations from May to September.Compared with SODA Kuroshio transport, a5%contribution of the Stokes transportis also found. By introducing the wave-driven surface stress into the modified Ekmanequation, the wave-driven pumping effect is discussed. The wave-driven pumpingvelocities are large in middle and high latitudes with magnitude of about5cm/day.
The large scale part of ocean waves are often called swells. The source areas inthe westerlies where most swells arose are approximately round and can be regardedas ‘points’4km away from the original areas. Swells disperse and travel along greatcircles in group velocities, and longer ones move faster. The energy signals are wellcarried by Mean Wave Period in propagation after large storms. Swells keep similardispersing velocities in transverse direction but the correlations to the sourcesdecrease with distance. The continuity of wave crest is often broken by land and islands. At local areas with large winds, the swells also interact with winds and windwaves. The dissipation rate of swell energy in space is approximately-4~5×10~(-7)m~(-1).The swell energy is disperse within6000km from the source and tends to contractbetween6000km and12000km but increases a little away from12000km. Dissipationincreases with wave steepness. Swell-turbulent stress interaction in marineatmosphere boundary layer (MABL) and swell-turbulence interaction in ocean mixedlayer (OML) are the main sources of dissipation, and the wave steepness and theinverse wave age are the main index in assessing the dissipation rate. Observedinverse wave age increases with wave steepness and distance to source whiledecreases with wave period. The wave steepness δ=0.01is a dividing line forinverse wave age: whenδ <0.01the inverse wave age is between-1and1withalmost the same positive and negative values, indicating the existence of bothfollowing and against wind waves; but whenδ>0.01, inverse wave age tends to bepositive, indicating that following waves are dominant and short swells remain to beinfluenced by local winds.
Dissipation parameterizations related to ocean swells are included in WW3model ACC350package; comprehensive model assessments show that it can reflectthe wave height very well within8m. Biases are largest in April and smallest inDecember. The wave model errors mainly come from the errors in swell componentsmodeling, especially in wave period. ACC350package is better in performance thanthe default WAM4BAJ package, but still shows room to get progress relying on moreobservations and research on physical processes.
涌浪对波浪诱导的Stokes输运有重要影响，特别对局地波浪的平均方向有所制约。全球Ekman输运主要呈带状分布，赤道海区两侧的信风带上Ekman输运的量值较大，可以的达到3m~2s以上；Ekman输运N-S分量Ty,E与整体量值分布一致，而W-E分量Tx,E受经向风作用呈带状倾斜。全球Stokes输运也主要为带状分布，尤其是两半球西风带的波浪输运量很大。而经向上的输运Ty,S，总的来看也基本呈现带状，但在大洋东侧却明显更强，体现了涌浪的作用。全球Stokes输运占Ekman输运的量值最大可达50%，太平洋和大西洋27.5N，30N和32.5N纬线的积分Ekman输运和Stokes输运有夏秋季强（向北）、冬春季弱（向南）的季节变化趋势，波浪输运不同海区不同季节有正贡献或负贡献。波浪Stokes经向输运沿27.5N，30N和32.5N的纬线积分值与Sverdrup关系估计的西边界流流量呈相似的季节变化，夏秋和冬春季相反；波浪导致的经向输运量值约为整体大洋输运的5到10%，在10月至4月为正贡献，5月至9月为负贡献。与SODA估计的黑潮流量相比，波浪作用可以达到5%。通过浪致表面应力来阐述波浪作用，发现波浪抽吸速度在中高纬海区较强，量值可达5cm/day，是波浪作用产生的源区。而风应力抽吸在副热带最强。各个大洋东西侧的波浪抽吸有局地的特征。
波浪中尺度较大的涌浪在西风带产生的源区可以近似为圆形和点源，长波以风暴生成区为中心以近似扇形散开，沿大圆传播。涌浪各分量以群速传播能量，周期越长的分量传播越快；涌浪平均周期可以较好的保留涌浪传播的信息。在横向上可以基本保持同样的扩散速度，但距离点源越远相关性越低。在海盆靠近陆地的区域由于地形变化，波浪发生折绕射较强，破坏了波峰线的连续性。在局地风较强的区域，涌浪依然会发生与局地风和波浪的相互作用。涌浪在传播过程中会发生能量的衰减，空间耗散率约为-4~5×10~(-7)m~(-1)。在离点源距离较近的6000km以内，风暴强度差异引起能量较离散；6000-12000km之间，涌浪的能量差异减小；当距点源距离大于12000km，能量又有所增加。不同周期的分量耗散率范围没有明显的差别，初始波陡越大，耗散率越大。涌浪能量耗散主要由于其与海气边界层湍应力相互作用和与混合层湍流作用引起耗散。波陡和反波龄是衡量耗散强度的主要参数。反波龄随波陡增加而增大，随周期增大，反波龄降低至-1~1，随着离点源距离增加反波龄增大。波陡δ=0.01处为一较明显的分界线，当δ <0.01时，反波龄在-1~1，正负相当，风速和波速方向同向和反向同样明显，且风速总小于波速；当δ>0.01，普遍倾向于反波龄γ>0，即风向与波向同向较多，且在周期较短的分量上依然有γ>1，风速大于或接近波速，涌浪依然受局地风的影响。
WW3的ACC350配置包含了有关涌浪耗散的物理现象的源函数项，模式对太平洋整体有效波高模拟较好，但约8米以上的波高模拟的有偏大趋势。4月的误差相对较大，12月误差最小；模式在中低纬带误差偏大较为明显。模式可以较好的进行大洋风浪的模拟，精确度较高。对涌浪的模拟波高偏大，整体来讲周期和波向的模拟比波高的精度高；模式对周期模拟的误差主要来自对涌浪周期的模拟误差，整体稍偏大。ACC350配置模式采用的基于涌浪耗散的物理模型可以部分改进BAJ模型涌浪波高模拟误差，尤其是在大洋中部较明显。模式的模拟能力需要依赖大量数据和对物理模型的认识进一步改进。
The persistency and extensiveness of small scale ocean waves makes themimportant to large scale ocean phenomena. In this dissertation, the wave-inducedCoriolis-Stokes effect in upper ocean water transport is analyzed, placing emphasis onocean swells. The large ocean swell transport and dissipation characteristics are alsodiscussed, together with model performance assessment of the newly publishedWavewatchIII v3.14on ocean swells.
Ocean swells are important to wave-induced Stokes transport, especially in theMean Wave Direction calculation. The global Ekman transports are band-likedistributed with maximums at Trade wind areas. The W-E components of the Ekmantransport tilt with longitudinal wind. The Stokes transports are also in band withmaximums at westerlies. The W-E components are large in the eastern parts of theoceans where swell are more dominant. The Stokes transport contributes to the Ekmantransport in50%at large; both of the integrated transports across three latitudesat27.5N,30Nand32.5Nare stronger in summer and autumn and weaker inwinter and spring. The Stokes transports are similar in seasonal variations withSverdrup transports along the three latitudes and occupy5to10%in magnitude, withcontributions from October to April and cancellations from May to September.Compared with SODA Kuroshio transport, a5%contribution of the Stokes transportis also found. By introducing the wave-driven surface stress into the modified Ekmanequation, the wave-driven pumping effect is discussed. The wave-driven pumpingvelocities are large in middle and high latitudes with magnitude of about5cm/day.
The large scale part of ocean waves are often called swells. The source areas inthe westerlies where most swells arose are approximately round and can be regardedas ‘points’4km away from the original areas. Swells disperse and travel along greatcircles in group velocities, and longer ones move faster. The energy signals are wellcarried by Mean Wave Period in propagation after large storms. Swells keep similardispersing velocities in transverse direction but the correlations to the sourcesdecrease with distance. The continuity of wave crest is often broken by land and islands. At local areas with large winds, the swells also interact with winds and windwaves. The dissipation rate of swell energy in space is approximately-4~5×10~(-7)m~(-1).The swell energy is disperse within6000km from the source and tends to contractbetween6000km and12000km but increases a little away from12000km. Dissipationincreases with wave steepness. Swell-turbulent stress interaction in marineatmosphere boundary layer (MABL) and swell-turbulence interaction in ocean mixedlayer (OML) are the main sources of dissipation, and the wave steepness and theinverse wave age are the main index in assessing the dissipation rate. Observedinverse wave age increases with wave steepness and distance to source whiledecreases with wave period. The wave steepness δ=0.01is a dividing line forinverse wave age: whenδ <0.01the inverse wave age is between-1and1withalmost the same positive and negative values, indicating the existence of bothfollowing and against wind waves; but whenδ>0.01, inverse wave age tends to bepositive, indicating that following waves are dominant and short swells remain to beinfluenced by local winds.
Dissipation parameterizations related to ocean swells are included in WW3model ACC350package; comprehensive model assessments show that it can reflectthe wave height very well within8m. Biases are largest in April and smallest inDecember. The wave model errors mainly come from the errors in swell componentsmodeling, especially in wave period. ACC350package is better in performance thanthe default WAM4BAJ package, but still shows room to get progress relying on moreobservations and research on physical processes.
引文
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