3.1. Superficial Ekman Current Deviation
The variability effect of the turbulent viscosity coefficient on the deviation of the Ekman current is presented in
Figure 6. The results were obtained by considering the vectors
u0 and
v0 from Equations (10) and (12). They were calculated for different finite depths, from 5 to 1000 m for highly stratified profiles and from 5 to 500 m for slightly stratified profiles. The deviations of the currents of the upper boundary layer of the spiral of the modified Ekman model are observed when the variations of
kz simulate a highly stratified water profile in
Figure 6.
Figure 6a,b shows the results for middle and high latitudes, i.e., 70° and 40° degrees of latitude. The deviation of the surface current tends to an angle of 40° for a water column with depths close to 400 m. In addition, turbulent viscosity profiles with low values, such as
kz0 = 0.001 m
2/s, were considered, and they are represented by a continuous “blue line”. For intermediate values of the turbulent viscosity profile, i.e.,
kz0 = 0.01 m
2/s, the trend toward 40° is observed for water columns greater than 600 m. It is represented by the “red line”.
However, for turbulent viscosity profiles with a surface value of kz0 = 0.1 m2/s, represented by the “yellow line”, it is observed that from a depth of 800 m, the curve shows a trend smaller than 40° (towards around 35°–40°) deviation of the Ekman surface current.
In addition,
Figure 6c shows the behaviors in regions close to the tropics, i.e., 10° latitude. Turbulent viscosity profile is considered with
kz0 = 0.001 m
2/s (blue lines) and
kz0 = 0.01 m
2/s (red line) on the surface. The trend toward 35° and 40° deviation from the surface current of the spiral is shown. It is obtained at around 600 and 800 m in depth, respectively. Meanwhile, for a turbulent viscosity profile with a viscosity at surface
kz0 = 0.1 m
2/s, an increasing curve is observed towards a 30° deviation of the surface current concerning the wind velocity.
The obtained results are contrasted with the application of the modified Ekman model for slightly stratified profiles. As seen in
Figure 6d–f, a 45° deviation angle from the current surface is reached with the velocity vector from the wind for 100 meters-deep water columns in the case of regions of 40° and 70° degrees of latitude. On the other hand, for tropical latitudes of 10°, the 45° deviation angle occurs in areas with a depth of 200 m, as shown in
Figure 6f.
The behavior of the deviation of the surface current of the Ekman spiral for little stratification and water columns with depths greater than 200 m is similar to the classical theory [
4].
Note that for latitudes of 10° and higher values of turbulent viscosity coefficient on the surface, the angle of deviation of the surface current shows a slight tendency towards smaller deviation angles of around 30°. This is shown in
Figure 6c and represented by the yellow line. In contrast, for regions of greater latitude (40° lat. and 70° lat.), a more evident deviation to 40° is observed for all values of k
z0. The observed result is because, at higher latitudes, the Coriolis force diverts the water mass to a greater extent than in the tropics [
22], which translates into a more active effect on the surface current, on a column of water, for a given depth.
For the analysis of shallow water columns, considered less than 100 m, and highly stratified profiles, it can be observed that in the middle and upper regions of 70° and 40° latitude, for water columns with depths of 5 to 100 m, an increasing curve is observed in the ranges 0°–7°, 2°–20°, and 7°–35° in the value of the angles of surface current deviation for turbulent viscosity coefficients. Surface values of
kz01 = 0.001 m
2/s,
kz02 = 0.01 m
2/s, and
kz03 = 0.1 m
2/s were represented in blue, red, and yellow lines, respectively, as presented in
Figure 6a,b.
For tropical latitudes of 10° (
Figure 6c) and the same range of depths and profiles of turbulent viscosity coefficients on the surface, minor surface current deviations are observed in the ranges 0°–4°, 1°–7°, and 5°–30°. This indicates that the surface current vectors of the Ekman spiral are closer to the direction of the wind. This occurs because as the bottom boundary layer is near the surface, the Ekman transport is increasingly reduced because the wind shear forces predominate over the short water column. As a result, the Ekman spiral is underdeveloped.
For slightly stratified profiles, as shown in
Figure 6d–f, a significant variation is observed between the angles of deviation of the surface current of the Ekman spiral of 10°, 28°, and 33° for shallow depths. It occurs in or around 5 m depth for regions of 10°, 40°, and 70° of latitude, correspondingly. The more significant deviations of this surface layer of the water column are due to the more significant influence of the Coriolis force on a profile with a lower turbulent viscosity gradient.
3.2. Ekman Transport
Using the turbulent viscosity coefficient profiles with their surface values
kz01,
kz02, and
kz03 described in
Figure 4, a range of depths were evaluated between 5 and 1000 m (for highly stratified profiles) and between 5 and 500 m (for slightly stratified profiles).
Figure 7 shows the transport results applying the modified Ekman model for the 10°, 40°, and 70° regions. From the horizontal velocity components, u and v, vertically integrated along the Ekman spiral, its resulting velocity U and V are calculated using the following expressions:
Figure 7 shows the direction, in degrees, of the Ekman transport. According to the traditional model, in a completely homogeneous ocean (
kz = constant), the average displacement of the waters occurs at 90° concerning the wind direction.
However, considering the characteristics of the current study, a non-constant turbulent viscosity profile in the water column, it is observed that with greater stratification (
Figure 7a–c), the movement of the Ekman layer takes a direction towards 80° of deviation with depths greater than 200 m. In contrast, for a more homogeneous water column (
Figure 7d–f), as expected, the deviation tends rapidly toward 90° for water columns greater than 200 m deep. The local maximums observed for all latitudinal regions move to the left or the shallower waters at higher latitudes (
Figure 7a–c).
Comparing the results of the highly stratified water columns and the less stratified ones, it can be seen for all latitudes that the latter has the local maxima slightly more to the right or towards deeper waters. These local maxima coincide with the regions where the maximum current velocities and in the Ekman spiral occur below the ocean surface.
Results presented in
Figure 8 show that for latitudes near the equator, the deviation caused by the Coriolis force influences to a lesser degree. Curves for multiple values of the turbulent viscosity coefficient
kz0 were evaluated despite keeping similar behaviors for all cases.
Unlike what would be expected in the traditional Ekman model (kz is independent of depth), which is not the most realistic consideration due to mixing in a stable water column, the obtained result is more minor than neutral stability. The mixed layer can be thinner than the Ekman depth, and kz will change rapidly at the bottom of the mixed layer because mixing is a function of stability. Mix generation through a stable layer is much less than mixing through a neutral stability layer.
Figure 8 shows the level, in meters below sea level, at which the maximum velocity is presented for different depths, remembering that the water column has been divided vertically into thin layers at a step of ∆
z = 0.5 m.
In contrast to what is established in the classical Ekman model, where the magnitude of the velocity (speed) decreases from its maximum on the surface to lower levels in the column until it reaches zero velocity at the bottom, in the numerical development of this study, it was found that, for latitudes close to the equator (
Figure 8c), and values of the turbulent viscosity coefficient on the surface
kz01 = 0.001 m
2/s,
kz02 = 0.01 m
2/s, and
kz03 = 0.1 m
2/s, the behavior of the velocity of the Ekman spiral grows towards depths of −30, −60, and −160 m, where the maximum velocity in the spiral is close to −6, −22, and −68 m, respectively. Later, a sharp decrease in the maximum velocity is observed towards the surface. For the same values of the turbulent viscosity coefficient on the surface
kz0, the velocity of the Ekman spiral increases towards depths of −20, −50, and −80 m for 40° and 70°, as shown in
Figure 8b,c. The maximum velocity in the spiral is close to −4, −12, and −38 m, for a latitude of 40°. For regions of latitude 70°, the velocity of the Ekman spiral grows towards depths from −10, −30, and −80 m, where the maximum velocity in the spiral is close to −4, −10, and −30 m, respectively. Later, a sharp decrease is observed in the maximum velocity towards the surface.
It should be noted that this behavior takes place in a highly stratified water column. Following what was previously mentioned about the turbulent viscosity profiles of
Figure 4, it occurs for all latitudinal regions considered, with the fact that the further away from the tropics it is, the depth of the maximum velocities rises a few meters towards the surface.
In
Figure 8, it is observed that the maximum velocity occurs below the surface at specific depths. This is observed for highly stratified profiles (see
Figure 4), where the turbulent viscosity coefficient profile presents its maximum at
zm = 0.1 h. It causes, at a certain depth, more significant mixing to be generated by turbulence, i.e., greater turbulent viscosity, which then falls sharply to its inflection point at
zh = 0.2 h. It is crucial to bear in mind that the Coriolis effect is lower towards the tropics (
Figure 8a), which responds that, towards these latitudes (10° latitude), the impact of wind velocity predominates over the layer. It is transmitted to consecutive layers.
In
Figure 9, latitude 10° was selected with a water profile depth of 160 m and a turbulent viscosity coefficient of
kz03 = 0.1 m
2/s to be analyzed. It is observed that it presents its maximum velocity at approximately 68 m at this latitude and water column depth. For this reason,
Figure 9 intends to show the development of the velocities in this water column by comparing a homogeneous sea state, i.e., the classic Ekman model, with a high stratification model.
In this graph, the maximum velocity corresponds to the more considerable separation between the velocity vectors
u and
v, i.e., if an imaginary horizontal line is drawn, the most significant magnitude of velocity will occur at the depth at which these intersection points are most distant.
Figure 9a shows the velocity profile
u and
v for the analytical development, with continuous blue and red lines. Purple and yellow circles represent numerical solutions for
u and
v velocity, respectively. The solution is obtained for an utterly homogeneous state, where the maximum velocity is presented on the surface, as the classical theory shows. In
Figure 9b, in the development of a highly stratified profile, the maximum velocity occurs below the surface.
This behavior responds to the
kz profile in
Figure 4. There is a very confined layer of turbulent mixing on the surface, which prevents velocity development. A velocity increases below this layer, as long as the background boundary layer is far enough to favor this result.
The behavior described for a latitude of 10°, in
Figure 9, is similar for higher latitudes. However, the maximum velocities in the selected analysis occur in deeper waters due to the Coriolis action. Finally,
Figure 10 is presented to show the difference between the Ekman spiral obtained with the classical model (left) and the modified model (right). Results are selected for a defined height of 1000 m and latitude 40°24′56.29″.