Air-sea interaction occurs over a wide spectrum of scales ranging from millimeters (spray droplets and air bubbles) to hundreds of kilometers (synoptic scale storms) and even larger (global climate). The coupling among water waves and atmospheric turbulence is one of the important components of air-sea interaction. Wind generated waves influence the flux of momentum and scalars at the air-sea interface and represent a visible signature of coupling between the atmosphere and ocean. Also, the fundamental difference between atmospheric boundary layers over land and over water derives from the scale and mobility of the water surface. An outstanding question in wind-wave interaction is the impact of swell on the atmospheric planetary boundary layer (PBL). Swell dominated wave fields occur after the passage of storm fronts and can propagate long distances without significant dissipation, e.g., see estimates in Cohen and Belcher (1999). In the open ocean, the wave height variance is typically dominated by swell (i.e., by old waves) and as a result it is difficult to measure and isolate the contributions of young (short) waves to the roughness and surface stress. The impact of swell on surface drag parameterizations is correspondingly unsettled. A recent study by Donelan et al. (1997) suggests that swell influences are strong and that wind-swell alignment is an important factor for the measured drag coefficients (e.g., they report that the drag increases by a factor of 3 for swell opposing the wind). Thus, the surface stress depends on at least three factors, wind speed, wave age, and swell. The coupling between light winds following fast running swell is of particular interest here. Harris (1966) first reported the formation of a wave-driven wind in a laboratory wave tank. Later, Holland et al. (1981) and other observational campaigns noted an increase in surface winds in the presence of swell. Since then a growing body of experimental evidence has documented
[1]
J. Edson.
Investigations of flux-profile relationships in the marine atmospheric surface layer during CBLAST
,
2004
.
[2]
C. Fairall,et al.
Wind Stress Vector over Ocean Waves
,
2003
.
[3]
J. McWilliams,et al.
Turbulent flow over water waves in the presence of stratification
,
2002
.
[4]
Anna Rutgersson,et al.
Use of conventional stability parameters during swell
,
2001
.
[5]
C. Fairall,et al.
Upward Momentum Transfer in the Marine Boundary Layer
,
2001
.
[6]
Hans Bergström,et al.
A case study of air‐sea interaction during swell conditions
,
1999
.
[7]
Mark A. Donelan,et al.
On momentum flux and velocity spectra over waves
,
1999
.
[8]
S. Belcher,et al.
Turbulent shear flow over fast-moving waves
,
1999,
Journal of Fluid Mechanics.
[9]
Stephen E. Belcher,et al.
TURBULENT FLOW OVER HILLS AND WAVES
,
1998
.
[10]
Mark A. Donelan,et al.
The Air–Sea Momentum Flux in Conditions of Wind Sea and Swell
,
1997
.
[11]
C. Mastenbroek,et al.
Impact of waves on air-sea exchange of sensible heat and momentum
,
1996
.
[12]
Michael Tjernström,et al.
The Near-Neutral Marine Atmospheric Boundary Layer with No Surface Shearing Stress: A Case Study
,
1994
.
[13]
J. McWilliams,et al.
A subgrid-scale model for large-eddy simulation of planetary boundary-layer flows
,
1994
.
[14]
C. Moeng.
A Large-Eddy-Simulation Model for the Study of Planetary Boundary-Layer Turbulence
,
1984
.
[15]
D. L. Harris,et al.
The Wave-Driven Wind
,
1966
.