By Miles McPhee

At a time while the polar areas are present process fast and extraordinary switch, knowing exchanges of momentum, warmth and salt on the ice-ocean interface is important for realistically predicting the longer term nation of sea ice. by means of providing a size platform mostly unaffected through floor waves, drifting sea ice offers a different laboratory for learning features of geophysical boundary layer flows which are super tough to degree somewhere else. This booklet attracts on either wide observations and theoretical rules to increase a concise description of the influence of pressure, rotation, and buoyancy at the turbulence scales that keep an eye on exchanges among the ambience and underlying ocean whilst sea ice is current. a number of fascinating and specific observational information units are used to demonstrate various features of ice-ocean interplay starting from the influence of salt on melting within the Greenland Sea marginal ice sector, to how nonlinearities within the equation of kingdom for seawater impact blending within the Weddell Sea.

The book’s content material, built from a chain of lectures, could be applicable extra fabric for upper-level undergraduates and first-year graduate scholars learning the geophysics of sea ice and planetary boundary layers.

Miles McPhee plays geophysical study, involved in polar areas, either from McPhee study corporation and as associate valuable scientist on the college of Washington utilized Physics Laboratory. He has participated in additional that twenty box courses within the polar oceans of either hemispheres. Dr. McPhee additionally lectures on air-ice-sea interplay on the collage middle on Svalbard.

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Extra resources for Air-Ice-Ocean Interaction: Turbulent Ocean Boundary Layer Exchange Processes

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Tu , Su , p93 ) = ρ (Tl , Sl , p93 ) The difference between the density of the two-layer upper ocean and an ocean with uniform T and S equal to the upper layer values: δ ρ = ρ (T, S, p) − ρ (Tu , Su , p) is plotted in Fig. 12. If a parcel of water from the upper layer (square marker) is displaced downward across the interface, it will be heavier than its ambient surroundings and will continue downward. A parcel displaced across the interface from below (circle) will be lighter than its surroundings and will continue to rise.

86 ◦C and about 8 for T = 4 ◦ C. Thus for water close to freezing, density variation is almost exclusively a function of salinity, and temperature may often be treated as a passive scalar contaminant. , ρ (T, S, p = 0) or σ0 = ρ (T, S, p = 0) − 1000. The reason for this is clear: a well mixed layer with uniform T and S, will have a pressure induced vertical density gradient, but there is negligible work (besides friction) involved in moving a parcel from one level (pressure) to another. Yet there are idiosyncrasies associated with nonlinearities in the equation of state that make this less straightforward than it might at first appear.

5 Time series of the leading coefficients of the complex demodulation fitting for seven days in September, 1998. For V 0 , up is north. The inertial phasor represents the amplitude and phase of the clockwise rotating inertial velocity. 26) In March 1998, at the SHEBA project in the central Arctic, we observed an upwelling event apparently related to intense local ice deformation (McPhee et al. 2005). 2 During this time, we measured turbulent heat flux in the upper part of the boundary layer that was at least an order of magnitude greater than at any other time during the year-long deployment; enough to cause significant basal melting when the ice is normally at its coldest.

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