Download Air-Ice-Ocean Interaction: Turbulent Ocean Boundary Layer by Miles McPhee PDF

By Miles McPhee

At a time whilst the polar areas are present process fast and unheard of switch, realizing exchanges of momentum, warmth and salt on the ice-ocean interface is important for realistically predicting the long run country of sea ice. by way of supplying a size platform principally unaffected by means of floor waves, drifting sea ice offers a special laboratory for learning features of geophysical boundary layer flows which are tremendous tricky to degree somewhere else. This ebook attracts on either broad observations and theoretical rules to enhance a concise description of the impression of tension, rotation, and buoyancy at the turbulence scales that regulate exchanges among the ambience and underlying ocean whilst sea ice is current. a number of attention-grabbing and exact observational info units are used to demonstrate various elements of ice-ocean interplay starting from the impression of salt on melting within the Greenland Sea marginal ice region, to how nonlinearities within the equation of nation for seawater have an effect on blending within the Weddell Sea.

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3) In this case, the TKE balance comprises four terms. The first term on the left is the production rate of TKE by the interaction of turbulent stress with mean shear: PS = τ · ∂ U/∂ z. In shear flows as considered here, it is positive, meaning that the interaction of shear with Reynolds stress produces turbulence. A corresponding term with opposite sign occurs in the mean flow kinetic energy equation, which demonstrates mathematically how turbulence drains kinetic energy from the mean flow. 4) ρ If TKE buoyancy production is positive (buoyancy flux negative), the flux of positive density variations is downward and energy is added to turbulence by gravity.

The system is thermobarically unstable (see Akitomo 1999) limits mixing driven from the surface, forming a new, shallower near surface layer. 5 The fact remains that if melting at the ice/ocean interface is too weak or too slow to counteract the combined effects of surface buoyancy loss from cooling and the cabbeling/thermobaricity mechanism at the base of the mixed layer, then convection will continue (McPhee 2003). Once the ice cover is gone and the air remains cold, there is nothing except horizontal advection of ice or fresh water to quell deep mixing, and essentially a direct connection between the abyssal ocean and the atmosphere is established.

03 kg m−3 . In oceanography it is customary to compare water masses via a temperature-salinity diagram, as drawn in Fig. 11a. The T/S pairs representing characteristics of the two (idealized) layers from Fig. 10 are shown as symbols embedded in contours of σ0 . 63 psu) is shown in white. The double arrow indicates the increase in salinity needed to raise the potential density of the upper layer to that of the lower. All else being equal, the salt rejected from about 13 cm of additional ice growth (at the time the ice was about 35 cm thick) would accomplish this.

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