Ekman spiral explained

The Ekman spiral is an arrangement of ocean currents: the directions of horizontal current appear to twist as the depth changes.^[1] The oceanic wind driven Ekman spiral is the result of a force balance created by a shear stress force, Coriolis force and the water drag. This force balance gives a resulting current of the water different from the winds. In the ocean, there are two places where the Ekman spiral can be observed. At the surface of the ocean, the shear stress force corresponds with the wind stress force. At the bottom of the ocean, the shear stress force is created by friction with the ocean floor. This phenomenon was first observed at the surface by the Norwegian oceanographer Fridtjof Nansen during his Fram expedition. He noticed that icebergs did not drift in the same direction as the wind. His student, the Swedish oceanographer Vagn Walfrid Ekman, was the first person to physically explain this process.^[2]

Bottom Ekman spiral

In order to derive the properties of an Ekman spiral a look is taken at a uniform, horizontal geostrophic interior flow in a homogeneous fluid. This flow will be denoted by

\vec{u} = (\bar{u},\bar{v}) , where the two components are constant because of uniformity. Another result of this property is that the horizontal gradients will equal zero. As a result, the continuity equation will yield, (\partial w)/(\partial z) = 0 . Note that the concerning interior flow is horizontal, so w = 0 at all depths, even in the boundary layers. In this case, the Navier-Stokes momentum equations, governing geophysical motion can now be reduced to:^[3] \begin{align} - fv & =- (1)/(\rho _{0}) (\partial p)/(\partial x) + \nu _{E} (\partial ^{2} u)/(\partial z ^{2}) , \\[ 5 pt] fu & =- (1)/(\rho _{0}) (\partial p)/(\partial y) + \nu _{E} (\partial ^{2} v)/(\partial z ^{2}) , \\[ 5 pt] 0 & =- (1)/(\rho _{0}) (\partial p)/(\partial z) , \end{align}

Where

f is the Coriolis parameter, \rho _{0} the fluid density and \nu _{E} the eddy viscosity, which are all taken as a constant here for simplicity. These parameters have a small variance on the scale of an Ekman spiral, thus this approximation will hold. A uniform flow requires a uniformly varying pressure gradient. When substituting the flow components of the interior flow, u = \bar{u} and v = \bar{v} , in the equations above, the following is obtained:\begin{align} - f\bar{v} & =- (1)/(\rho _{0}) (\partial p)/(\partial x) = constant \\[ 5 pt] f\bar{u} & =- (1)/(\rho _{0}) (\partial p)/(\partial y) = constant \end{align}

Using the last of the three equations at the top of this section, yields that the pressure is independent of depth.

\begin{align} - f(v - \bar{v}) & = \nu _{E} (\partial ^{2} u)/(\partial z ^{2}) \\[ 5 pt] f(u - \bar{u}) & = \nu _{E} (\partial ^{2} v)/(\partial z ^{2}) \end{align} u = \bar{u} + A e ^{λ} and v = \bar{v} + B e ^{λ} will suffice as a solution to the differential equations above. After substitution of these possible solutions in the same equations, \nu ^{2λ} _{E} ^{4} + f ^{2} = 0 will follow. Now, λ has the following possible outcomes:λ = \pm ( 1 \pm i)\sqrt{ (f)/(2 \nu _{E}) }

Because of the no-slip condition at the bottom and the constant interior flow for

z \gg d , coefficients A and B can be determined. In the end, this will lead to the following solution for \vec{u}(z) :\begin{align} u & = \bar{u}\left[ 1 - e ^{-z/d} \cos\left( (z)/(d) \right)\right] - \bar{v}e ^{-z/d} \sin\left( (z)/(d) \right), \\[ 5 pt] v & = \bar{u} e ^{-z/d} \sin\left( (z)/(d) \right) + \bar{v}\left[ 1 - e ^{-z/d} \cos\left( (z)/(d) \right)\right], \end{align}

Here,

d = \sqrt{ (2 \nu _{E})/(f) }. Note that the velocity vector will approach the values of the interior flow, when the z takes the order of d . This is the reason why d is defined as the thickness of the Ekman layer. A number of important properties of the Ekman spiral will follow from this solution:

• When

z → { 0 } , it appears that the flow has a transverse component with respect to the interior flow, which differs 45 degrees to the left on the northern hemisphere, f> 0 , and 45 degrees to the right on the southern hemisphere, f< 0 . Note that, in this case, the angle between this flow and the interior flow is at its maximum. It will decrease for increasing z .

• When

(z)/(d) takes the value of \pi , the resulting flow is in line with the interior flow, but will be increased with e ^{-\pi} , with respect to the interior flow.

• For higher values of

(z)/(d) , there will be a minimal transverse component in the other direction as before. The exponential term will go to zero for z\gg d , resulting in \vec{u} = (\bar{u},\bar{v}) . Because of these properties, the velocity vector of the flow as a function of depth will look like a spiral.

Surface Ekman spiral

\vec{\tau} = (\tau _{x,\tau} _{y)} is exerted along a water-surface with an interior flow \vec{u} = (u,v) beneath. Again, the flow is uniform, has a geostrophic interior and is homogeneous fluid. The equations of motion for a geostrophic flow, which are the same as stated in the bottom spiral section, can be reduced to:\begin{align} - f(v - \bar{v}) & = \nu _{E} (\partial ^{2} u)/(\partial z ^{2}) \\[ 5 pt] f(u - \bar{u}) & = \nu _{E} (\partial ^{2} v)/(\partial z ^{2}) \\ \end{align}

The boundary conditions for this case are as follows:

• Surface

(z = 0 ) : \rho _{0\nu} ^{E (\partial u)/(\partial z)} = \tau _{x} and \rho _{0\nu} ^{E (\partial v)/(\partial z)} = \tau _{y}

• Towards interior

(z → { -inf ty}) : u = \bar{u} and v = \bar{v}

With these conditions, the solution can be determined:

\begin{align} u & = \bar{u} + (\sqrt{ 2)/() }e^\left[\tau_x \cos\left(\frac{z}{d} - \frac{\pi}{4}\right) - \tau_y \sin\left(\frac{z}{d} - \frac{\pi}{4}\right)\right] \\[5pt] v & = \bar + \frace^\left[\tau_x \sin\left(\frac{z}{d} - \frac{\pi}{4}\right) + \tau_y \cos\left(\frac{z}{d} - \frac{\pi}{4}\right)\right]\end

Some differences with respect to the bottom Ekman spiral emerge. The deviation from the interior flow is exclusively dependent on the wind stress and not on the interior flow. Whereas in the case of the bottom Ekman spiral, the deviation is determined by the interior flow. The wind-driven component of the flow is inversely proportional with respect to the Ekman-layer thickness

d . So if the layer thickness is small, because of a small viscosity of the fluid for example, this component could be very large. At last, the flow at the surface is 45 degrees to the right on the northern hemisphere and 45 degrees to the left on the southern hemisphere with respect to the wind-direction. In case of the bottom Ekman spiral, this is the other way around.

Observations

The equations and assumptions above are not representative for the actual observations of the Ekman spiral. The differences between the theory and the observations are that the angle is between 5–20 degrees instead of the 45 degrees as expected^[4] and that the Ekman layer depth and thus the Ekman spiral is less deep than expected. There are three main factors which contribute to the reason why this is, stratification,^[5] turbulence and horizontal gradients. Other less important factors which play a role in this are the Stokes drift,^[6] waves and the Stokes-Coriolis force.^[7]

Notes and References

1. Web site: US Department of Commerce . National Oceanic and Atmospheric Administration . The Ekman Spiral - Currents: NOAA's National Ocean Service Education . 2024-02-07 . oceanservice.noaa.gov . EN-US.
2. Ekman, V. W. 1905. On the influence of the Earth's rotation on ocean currents. Arch. Math. Astron. Phys., 2, 1-52. http://empslocal.ex.ac.uk/people/staff/gv219/classics.d/Ekman05.pdf
3. Book: Cushman-Roisin, Benoit . Beckers . Jean-Marie . Introduction to Geophysical Fluid Dynamics . ACADEMIC PRESS . 2009 .
4. Stacey, M. W., S. Pond, and P. H. LeBlond, 1986: A wind-forced Ekman spiral as a good statistical fit to low-frequency currents in coastal strait. Science, 233, 470–472
5. Price, J. F., and M. A. Sundermeyer, 1999: Stratified Ekman layers. J. Geophys. Res., 104, 20467–20494.
6. van den Bremer TS, BreivikØ. 2017 Stokes drift.Phil.Trans.R.Soc.A376:20170104.http://dx.doi.org/10.1098/rsta.2017.0104
7. Jeff A. Polton, David M. Lewis, and Stephen E. Belcher, 01 Apr 2005: The Role of Wave-Induced Coriolis–Stokes Forcing on the Wind-Driven Mixed Layer. Journal of Physical Oceanography, Volume 35: Issue 4, 444–457