T jpo, 2011, in press he origin of along-shelf pressure gradient in the Middle Atlantic Bight
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(b) (c)
(d) Figure 10. Results from the idealized simulation of warm-core rings, at (a and b) day 1200 and (c and d) day 1610 (see text). Panels (a) and (c) show surface current trajectories superimposed on sea surface height (SSH) in color. Panels (b) and (d) show the SSH contours; yellow line indicates zero and negative regions are shaded in grey. Dark, white (a & c) and grey (b & d) contours indicate the 50m, 200m and 1000m isobaths. 
(a) (b) (c) (d) (e) (f) Figure 11. From top to bottom: surface current anomalies (vectors) superimposed on shadings of SSH, CPVF and -JEBAR (denoted by “CJBAR” on plots) anomalies. Left columns (a, c & e) are weighted composites for the positive phase (PP) of ASPG anomaly (Fig.9c), and right (b, d & f) for the negative phase (NP). The shading scale for SSH (m) is shown to the right of “(b)”, and that for CPVF and –JEBAR (s-2) to the right of “(d)”. Black and white contours indicate the 50m, 200m and 1000m isobaths. It is readily shown that the max/min of CPVF correspond to max/min of approximately 0.05 m s-1, positive onshore across the 1000 m-isobath. 1 This same formula was used in Oey et al. (2006), but the coefficient for |ua| 2 was erroneously rounded off to 0.0002. 2 Other experiments were also conducted for checking consistencies, and were used also to derive equation (2) below. Those summarized in Table 1 suffice, however, for explaining the contributions of various forcing to ASPG. 3 A more complicated function may give a better “fit” but this is not attempted. The goal here is to summarize in a succinct way the response due to each of the different forcing. 4 Statistically, CLSW leads GS by about 11 months, which seems to agree with Rossby and Benway (2000) that strong CLSW can cause a southward shift of the Gulf Stream one year later. However, this is false as Rossby and Benway were looking at inter-annual rather than seasonal time scales. 5 The result is unchanged if N-EKE includes all points north of the Gulf Stream, except that the peak in Fig.8b is less prominent and the various correlations (below) degrade slightly. Also, if and warm and cold rings as well as Gulf Stream meanders are included, the largest EKE is then in summer (Zhai et al. 2008). 6 Another way is to write the vorticity equation using Salmon’s [1992] 2-layer planetary geostrophic equations [see Appendix in Oey et al. 2010] which yield for the CPVF JEBAR balance: U.(f/H) g’k.[(h12/2)×(1/H)] where g’ = reduced gravity and h1 = upper-layer depth. The vector χ may be identified with g’h12/2 which points from cold to warmer anomalies. Directory: ftp -> lyo -> chiming ftp -> Tr-41. 4-03-05-024 Telecommunications ftp -> Message Race Detection for Web Services by an smt-based Analysis ftp -> A proposal submitted to the ftp -> National reports on data buoy activities ftp -> Louisiana barrier island comprehensive monitoring program (bicm) Volume 1: Barrier Shoreline Post-Storm Assessment ftp -> Jcomm expert team on chiming -> Boemre 2008 Extended Hindcast Calculation of Gulf of Mexico Circulation: Model Development, Comparisons with Observations Download 1.87 Mb. Share with your friends:
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