. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography / dt HIDALGO 1961 If 2i°30' I I 20°00' If 18°30' '// 17°00' J 100 200 300 (a) H0= 425 ,-<\ ' n *\ /7 // /aLAWNOS 1968 - h i / 2I°30' 11 / 20°00 f —m°30\ / T / 17° 00 J / is i •; -~ , 100 200 300 400. 100 200 300 DISTANCE FROM H0 (Km) (b)H0=375 (c)HQ=375 Fig. 6. Geostrophic baroclinic transports computed from Eq. (1) for March 1961, April-May 1968 and for the numerical model. The thicker lines of panel (c) were computed from the results of the
. Collected reprints / Atlantic Oceanographic and Meteorological Laboratories [and] Pacific Oceanographic Laboratories. Oceanography / dt HIDALGO 1961 If 2i°30' I I 20°00' If 18°30' '// 17°00' J 100 200 300 (a) H0= 425 ,-<\ ' n *\ /7 // /aLAWNOS 1968 - h i / 2I°30' 11 / 20°00 f —m°30\ / T / 17° 00 J / is i •; -~ , 100 200 300 400. 100 200 300 DISTANCE FROM H0 (Km) (b)H0=375 (c)HQ=375 Fig. 6. Geostrophic baroclinic transports computed from Eq. (1) for March 1961, April-May 1968 and for the numerical model. The thicker lines of panel (c) were computed from the results of the non-topographic model, and the thinner lines from the topographic model. A vorticity equation for each layer is formed from these equations. Prediction equations for H and H' are ob- tained from the vorticity equation by making the geostrophic approximation in each layer. The geo- strophic constraint eliminates internal gravity waves. Moreover, the use of a rigid-lid condition on the sea surface (H-\-H'—D, independent of t) eliminates surface gravity waves. The prediction equations for the baroclinic and barotropic modes, with B=—H+H'-D, P' (6) p'-p P (7) are respectively dH r f+/-i r f+n €V2—+eHJ\ H, \+HJ\ B, dt L H J L H J L H' J g dtl H H' J el \H H'J H'A (8) and dB r f'+/-i m'+f\dH V—+H'J\ B,— \+J )— dt L E' J g\ H I dt /r (r-n a r (r-r ^r ,i a +KVY . I H' H' J g\- H' H' The relative vortices are given by r=f'+-V2£T / (9) (10) and f The Jacobians are used in the form J(A,B)- d/ dA\ d/ -Ib—)—( dy\ dx/ dx\ dA\ A—), by) (ID (12) for reasons discussed below. The finite-difference analogues of Eqs. (8) and (9) were taken as those given by Wert and Reid (1972). In summary, centered difference forms are used for the time and space derivatives. The nonlinear instabilities caused by the advective terms are suppressed by the use of the form of the Jacobian given in Eq. (12) (Arakawa, 1966). The DuFort-Frankel scheme (Smith, 1965) was used to represen
Size: 1442px × 1734px
Photo credit: © The Book Worm / Alamy / Afripics
License: Licensed
Model Released: No
Keywords: ., bookcentury1900, bookcollectionamericana, booksponsorlyrasismemb
