1. Term Paper Guide Find an oceanic or relevant atmospheric phenomenon you are interested in (e.g., ENSO, PDO, AMO, TAV, IOD, NAO, hurricane activity, regional flood or drought, monsoon, etc) Describe the general pattern, life cycle, or probable mechanisms of the phenomenon you choose based on class material and/or literature Examine the real-time oceanic evolution through the NOAA briefings from August to November 2011 Write a 2-4 page report (double space) in a research paper style to address the evolution of the chosen phenomenon during this period (a set of questions to be addressed is given in next slide) New ideas or approaches are encouraged

2. Questions to be addressed: Is 2011 a typical year for the phenomenon you have chosen? What is the evidence for that? What phase are we in during the past four months? What are the main factors driving the development or persistence or the phenomenon? What do you expect about its development in the coming winter and spring? Is the information from the briefing adequate for you to trace the developing event? Are the course materials useful in understanding the phenomenon?

3. FIGURE 7.12 Vorticity. (a) Positive and (b) negative vorticity. The (right) hand shows the direction of the vorticity by the direction of the thumb (upward for positive, downward for negative). From Talley et al. (2011, DPO)

4. FIGURE 7.13 Sverdrup balance circulation (Northern Hemisphere). Westerly and trade winds force Ekman transport, creating Ekman pumping and suction and hence Sverdrup transport. See also Figure S7.12. From Talley et al(2011, PDO)

5. For most of the basin Question What causes the strong narrow currents on the west side of the ocean basin? The westward Intensification

7. Quasi-geostrophic vorticity equation where Boundary conditions on a solid boundary L (1) No penetration through the wall (used for the case of no horizontal diffusion) (2) No slip at the wall along the boundary L n is the unit vector perpendicular to the boundary L

8. Stommel’s Model Rectangular ocean of constant depth Surface stress is zonal and varies with latitude only Steady ocean state Simple friction term as a drag to current Vorticity balance: Sverdrup balance +friction Flow patterns in this ocean for three conditions: (1)non-rotating ocean (f=0) (2)f-plane approximation (f=constant) (3)  -plane approximation (f=f o +  y)

9. f-plane  -plane

10. Wind stress (  ) + friction (  ) =0 ÷ Negative vorticity generation  Positive vorticity generation

11. Westerly winds in north, easterly winds in south Ekman effect drives the water to the center, Increase sea level generates anticyclonic geostrophic currents Internal friction (or bottom Ekman layer) generate downslope cross-isobaric flow, which balance the wind-driven Ekman transport

12. The  effect Generate negative vorticity  Generate positive vorticity 

13. In the west, water flows northward Wind stress (  ) + Planetary vorticity (  ) + Friction (  ) = 0 In the east, water flows southward Wind stress (  ) + Planetary vorticity (  ) + Friction (  ) = 0 Friction (W) > Friction (E)

14. Non-rotation Ocean, f=0

16. Quasi-geostrophic vorticity equation where Boundary conditions on a solid boundary L (1) No penetration through the wall (used for the case of no horizontal diffusion) (2) No slip at the wall along the boundary L n is the unit vector perpendicular to the boundary L

17. Non-dimensionalize Quasi- Geostrophic Vorticity Equation Define non-dimensional variables based on independent scales L and  o The variables with primes, as well as their derivatives, have no unit and generally have magnitude in the order of 1. e.g.,

18. Note that U has not been decided yet.

21. Non-dmensional vorticity equation Define the following non-dimensional parameters,, nonlinearity., bottom friction.,, lateral friction., If we choose we haveSverdrup relation

22. Interior (Sverdrup) solution If  <<1,  S <<1, and  M <<1, we have the interior (Sverdrup) equation:  (satistfying eastern boundary condition) Example: Let, Over a rectangular basin (x=0,1; y=0,1) (satistfying western boundary condition).

23. Westward Intensification It is apparent that the Sverdrup balance can not satisfy the mass conservation and vorticity balance for a closed basin. Therefore, it is expected that there exists a “ boundary layer ” where other terms in the quasi-geostrophic vorticity is important. This layer is located near the western boundary of the basin. Within the western boundary layer (WBL),, for mass balance In dimensional terms, The Sverdrup relation is broken down., the length of the layer  <<L The non-dimensionalized distance is

24. The Stommel model Bottom Ekman friction becomes important in WBL.,  S <<1. (Since the horizontal friction is neglected, the no-slip condition can not be enforced. No-normal flow condition is used). Interior solution at x=0, 1; y=0, 1. No-normal flow boundary condition

25. Let, we have Re-scaling in the boundary layer: Take into As  =0,  =0. As ,  I

26. The solution foris,.  A=-B , ( can be the interior solution under different winds) For,,.,.,

27. The dynamical balance in the Stommel model In the interior, Vorticity input by wind stress curl is balanced by a change in the planetary vorticity f of a fluid column.(In the northern hemisphere, clockwise wind stress curl induces equatorward flow).  In WBL,  Since v>0 and is maximum at the western boundary, the bottom friction damps out the clockwise vorticity., Question: Does this mechanism work in an eastern boundary layer?