【摘要】 <正> 为了在考虑到(1)产生海流的大气作用;(2)湍流粘滞系量值是计算的而不是假设的;(3)海洋具有实际可变的而非常量的深度等情况下,较易地计算出特别是铅直坐标函数的海流速度,本文提出一种大气-海洋三层模式。近似中性层结状态的大气被考虑是两个层的组合,第一层是紧贴海面的湍流边界层,第二层是位于第一层之上的Ekman层。仅考虑铅直湍流的海洋,被看成是从海面到海底的一整层。海面风应力分布和海洋中海水密更多还原

【Abstract】 For the purpose of calculating the velocity of ocean current feasible in the case of the function of the vertical coordinate pertaining to (1) the atmospheric effect on the generation of ocean current, (2) a calculated coefficient of eddy viscosity instead of an assumed one and (3) the sea with actual variable depth under consideration. The atmosphere and ocean constituting a model of three layers is in this paper. The atmosphere of nearly neutral stratification state is to be considered as a combination of two layers, one is the turbulent layer just over the sea surface, while the other is the Ekman layer laid above the former. Below the water surface only the vertical turbulence is under consideration from surface to bottom. The distribution of wind stresses over the sea surface and the distribution of the densities of sea water in the sea are known. Firstly we may find out the. expressions of roughness of sea surface and height of atmospheric turbulent layer from the formulae showing the profiles of wind velocity over the airbdynamically rough surface and the airodynamically smooth surface, besides, the idea that the geostrophic wind velocities being nearly nondivergent, thence the wind velocity at the top of atmospheric turbulent layer and the values of parameter characterizing the strength of vertical turbulence in the atmosphere may be obtained. Introducing the idea that the wind velocities at the boundary surface between the top of turbulent layer and the bottom of Ekman layer being coupled and equalized, we get an important formula about the sum of the horizontal gradients of atmospheric pressure at sea surface and the elevation of sea surface. However, as the current velocity at sea bottom with greater depth being nearly equal to zero so that the value of horizontal turbulent stress would be maximum there, an another form of formula showing the same sum may be obtained. Substituting these two formulae and the simplified surface velocity of ocean current into the equation of state of sea surface by introducing into the so-called rigid lid approximation of sea surface, it gives the values of parameter characterizing the strength of vertical turbulence in the sea. Then we may obtain the formula for calculating the horizontal current velocities by solving the steady equation of motion with the known value of above mentioned parameters, while the vertical velocities may be calculated from the equation of continuity by the aid of the calculated horizontal current velocities. We have calculated the current velocities of Kuroshio in East China Sea by applying the above described method, it gives more satisfactory results.更多还原