Ekman layer
The Ekman layer is the layer in a fluid where there is a force balance between pressure gradient force, Coriolis force and turbulent drag. It was first described by Vagn Walfrid Ekman.
Contents
 History 1

Mathematical formulation 2
 Boundary conditions 2.1
 Solution 2.2

Experimental observations of the Ekman layer 3
 Laboratory demonstrations 3.1
 In the atmosphere 3.2

In the ocean 3.3
 Instrumentation 3.3.1
 Observations 3.3.2
 See also 4
 References 5
 External links 6
History
Ekman developed the theory of the Ekman layer after Fridtjof Nansen observed that ice drifts at an angle of 20°40° to the right of the prevailing wind direction while on an Arctic expedition aboard the Fram. Nansen asked his colleague, Vilhelm Bjerknes to set one of his students upon study of the problem. Bjerknes tapped Ekman, who presented his results in 1902 as his doctoral thesis.^{[1]}
Mathematical formulation
The mathematical formulation of the Ekman layer can be found by assuming a neutrally stratified fluid, with horizontal momentum in balance between the forces of pressure gradient, Coriolis and turbulent drag.
 \begin{align} fv &= \frac{1}{\rho_o} \frac{\part p}{\part x}+K_m \frac{\part^2 u}{\part z^2}, \\ fu &= \frac{1}{\rho_o} \frac{\part p}{\part y}+K_m \frac{\part^2 v}{\part z^2}, \\ 0 &= \frac{1}{\rho_o} \frac{\part p}{\part z}, \end{align}
where \ u and \ v are the velocities in the \ x and \ y directions, respectively, \ f is the local Coriolis parameter, and \ K_m is the diffusive eddy viscosity, which can be derived using mixing length theory.
Boundary conditions
There are many regions where an Ekman layer is theoretically plausible; they include the bottom of the atmosphere, near the surface of the earth and ocean, the bottom of the ocean, near the sea floor and at the top of the ocean, near the airwater interface.
Each of the different regions will have different boundary conditions. We will consider boundary conditions of the Ekman layer in the upper ocean:^{[2]}
 \text{at } z = 0 : \quad A \frac{\part u}{\part z} = \tau^x \quad \text{and} \quad A \frac{\part v}{\part z} = \tau^y,
where \ \tau^x and \ \tau^y are the components of the surface stress, \ \tau , of the wind field or ice layer at the top of the ocean and \ u_g and \ v_g are the geostrophic flows in the \ x and \ y directions – as \ z \to \infty : u \to u_g, v \to v_g.
Solution
These differential equations can be solved to find:
 \begin{align} u &= u_g + \frac{\sqrt{2}}{fd}e^{z/d}\left [\tau^x \cos(z/d  \pi/4)  \tau^y \sin(z/d  \pi/4)\right ], \\ v &= v_g + \frac{\sqrt{2}}{fd}e^{z/d}\left [\tau^x \sin(z/d  \pi/4) + \tau^y \cos(z/d  \pi/4)\right ], \\ d &= \sqrt{2 K_m/f}. \end{align}
This variation of horizontal velocity with depth (z) is referred to as the Ekman spiral, diagrammed above and at right.
By applying the continuity equation we can have the vertical velocity as following
 w = \frac{1}{f\rho_o}\left [\left (\frac{\partial \tau^x}{\partial x} + \frac{\partial \tau^y}{\partial y} \right )e^{z/d}\sin(z/d) + \left (\frac{\partial \tau^y}{\partial x}  \frac{\partial \tau^x}{\partial y} \right )(1e^{z/d}\cos(z/d))\right ].
Note that when vertically integrated the volume transport associated with the Ekman spiral is to the right of the wind direction in the Northern Hemisphere.
Experimental observations of the Ekman layer
There is much difficulty associated with observing the Ekman layer for two main reasons: the theory is too simplistic as it assumes a constant eddy viscosity, which Ekman himself anticipated,^{[3]} saying“  It is obvious that \ \left[\nu \right] cannot generally be regarded as a constant when the density of water is not uniform within the region considered  ” 
and because it is difficult to design instruments with great enough sensitivity to observe the velocity profile in the ocean.
Laboratory demonstrations
The bottom Ekman layer can readily be observed in a rotating cylindrical tank of water by dropping in dye and changing the rotation rate slightly.[1] Surface Ekman layers can also be observed in rotating tanks.[2]
In the atmosphere
In the atmosphere, the Ekman solution generally overstates the magnitude of the horizontal wind field because it does not account for the velocity shear in the surface layer. Splitting the boundary layer into the surface layer and the Ekman layer generally yields more accurate results.^{[4]}
In the ocean
The Ekman layer, with its distinguishing feature the Ekman spiral, is rarely observed in the ocean. The Ekman layer near the surface of the ocean extends only about 10 – 20 meters deep,^{[4]} and instrumentation sensitive enough to observe a velocity profile in such a shallow depth has only been available since around 1980.^{[2]} Also, wind waves modify the flow near the surface, and make observations close to the surface rather difficult.^{[5]}
Instrumentation
Observations of the Ekman layer have only been possible since the development of robust surface moorings and sensitive current meters. Ekman himself developed a current meter to observe the spiral that bears his name, but was not successful.^{[6]} The Vector Measuring Current Meter ^{[7]} and the Acoustic Doppler Current Profiler are both used to measure current.
Observations
The first documented observations of an Ekmanlike spiral were made in the Arctic Ocean from a drifting ice flow in 1958.^{[8]} More recent observations include:
 The 1980 Mixed Layer Experiment^{[9]}
 Within the Sargasso Sea during the 1982 Long Term Upper Ocean Study ^{[10]}
 Within the California Current during the 1993 Eastern Boundary Current experiment ^{[11]}
 Within the Drake Passage region of the Southern Ocean ^{[12]}
 North of the Kerguelan Plateau during the 2008 SOFINE experiment ^{[13]}
Common to several of these observations spirals were found to be 'compressed', displaying larger estimates of eddy viscosity when considering the rate of rotation with depth than the eddy viscosity derived from considering the rate of decay of speed.^{[10]}^{[11]}^{[12]}^{[13]}
See also
References
 ^ CushmanRoisin, Benoit (1994). "Chapter 5  The Ekman Layer". Introduction to Geophysical Fluid Dynamics (1st ed.). Prentice Hall. pp. 76–77.
 ^ ^{a} ^{b} Vallis, Geoffrey K. (2006). "Chapter 2 – Effects of Rotation and Stratification". Atmospheric and Oceanic Fluid Dynamics (1st ed.). Cambridge, UK: Cambridge University Press. pp. 112–113.
 ^ Ekman, V.W. (1905). "On the influence of the earth's rotation on ocean currents". Ark. Mat. Astron. Fys. 2 (11): 1–52.
 ^ ^{a} ^{b} Holton, James R. (2004). "Chapter 5 – The Planetary Boundary Layer". Dynamic Meteorology. International Geophysics Series 88 (4th ed.). Burlington, MA: Elsevier Academic Press. pp. 129–130.
 ^ Santala, M. J.; Terray, E. A. (1992). "A technique for making unbiased estimates of current shear from a wavefollower". DeepSea Res. 39 (3–4): 607–622.
 ^ Rudnick, Daniel (2003). "Observations of Momentum Transfer in the Upper Ocean: Did Ekman Get It Right?". NearBoundary Processes and their Parameterization (Manoa, Hawaii: School of Ocean and Earth Science and Technology).
 ^ Weller, R.A.; Davis, R.E. (1980). "A vectormeasuring current meter". DeepSea Res. 27 (7): 565–582.
 ^ Hunkins, K. (1966). "Ekman drift currents in the Arctic Ocean". DeepSea Res. 13: 607–620.
 ^ Davis, R.E.; de Szoeke, R.; Niiler., P. (1981). "Part II: Modelling the mixed layer response". DeepSea Res. 28 (12): 1453–1475.
 ^ ^{a} ^{b} Price, J.F.; Weller, R.A.; Schudlich, R.R. (1987). "WindDriven Ocean Currents and Ekman Transport". Science 238: 1534–1538.
 ^ ^{a} ^{b} Chereskin, T.K. (1995). "Direct evidence for an Ekman balance in the California Current". Journal of Geophysical Research 100: 18261–18269.
 ^ ^{a} ^{b} Lenn, Y; Chereskin, T.K. (2009). "Observation of Ekman Currents in the Southern Ocean". Journal Of Physical Oceanograph 39: 768–779.
 ^ ^{a} ^{b} Roach, C.J.; Phillips, H.E.; Bindoff, N.L.; Rintoul, S.R. (2012). "Anomalous Ekman Transport Near Kerguelen Island". Proceedings of the 18th Australasian Fluid Mechanics Conference.
External links
 Bottom Ekman layer lab demonstration
 Surface Ekman layer lab demonstration
