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The fscommand() is a global function. The fscommand() controls global properties of the entire movie.



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Instead of the heat balance approach as described above, Equation 2.2 can be derived directly from Equation 2.3 by replacement of the derivatives with the respective nite difference approximations. The nite difference approximation for the time derivative is as shown in Equation 2.4. The second order derivative in the x-dimension can be approximated as follows: T T Ti +1 - Ti Ti - Ti -1 T - 2Ti + Ti -1 2 T T x + x Dx Dx = = i +1 2 x x Dx Dx x Dx 2 Note that in the nite difference approximation for the second order derivative as shown above, the temperature gradients are evaluated from the temperature difference between node i and each of the adjacent nodes at the two sides of node i. This scheme is, therefore, called a central-in-space difference scheme. Since Equation 2.2 relates the change in the temperature at node i to the temperatures at the nodes at both sides of node i, it applies only to the interior nodes within a slab of material. Boundary conditions The nite difference equation for the outermost slice of a slab of material can also be derived from the heat balance approach. Using Te to denote the sol-air temperature or environmental temperature of the surrounding, the convective and radiant heat ux at the surface can be described by: qo = ho (Te - Ts ) (2.6)





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Applying the conditional survival to the group of existing customers uses a join. Each customer is joined to the conditional survival for days 365 through 730.

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sion in the Taupo volcanic zone of New Zealand (Fig. 9.31). Further support for extension comes from the subsidence of remnant arcs as their dynamic support is removed after the development of backarc basins, earthquake focal mechanism solutions, and the segmented geometry of normal faults and spreading ridges, which also characterize continental rifts (Section 7.2) and mid-ocean ridges. The Woodlark Rift (Fig. 7.39b), which records the transition from rifting to sea oor spreading above a Neogene subduction zone (Section 7.8.2), illustrates this segmentation especially well. In general, the composition of the crust in oceanic backarc basins is broadly similar to that of other ocean basins, although in some cases layer 1 is unusually thick. Net accretion rates are similar to those deduced for mid-ocean ridges, and range from approximately 160 mm a 1 in the northern Lau basin (Bevis et al., 1995) to 70 mm a 1 in the East Scotia Sea (Thomas et al., 2003) and 20 35 mm a 1 in the Mariana Trough (Mart nez et al., 2000). The crust in these settings commonly shows substantial thinning by normal faulting, although the total crustal thickness also depends upon the rate of

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