@article{oai:nipr.repo.nii.ac.jp:00003865,
 author = {カワイ, シンイチ and ナカワ, マサヨシ and KAWAI, Shinichi and NAKAWO, Masayoshi},
 journal = {Proceedings of the NIPR Symposium on Polar Meteorology and Glaciology},
 month = {Nov},
 note = {P(論文), We have developed a scheme for two and three dimensional ice sheet dynamics with the model considered by Mahaffy, assuming the basal sliding velocity to be zero. Mahaffy's model is given by ∂h/∂t=b-&xdtri;・q and q=-ck&xdtri;h, or c&xdtri;・(-k&xdtri;h)=b-∂h/∂t, where c={(2A)/(n+2)} (ρg)^n and k (x, y, t)=(&xdtri;h・&xdtri;h)^<(n-1)/2> (h-z_0)^<n+2>. We can lead the dimensionless form, in which c=1. In the two dimensional model, let Ω_1=[-x_1,x_1] which is the land area, and Ω_2=[-x_2,-x_1) ∪ (x_1,x_2], which is the sea area, where 0<x_1<x_2. We assume that q in Ω_2 is m times larger than in Ω_1 and that the initial shape of h is symmetric about x=0. Let 0&le;x&le;n&xutri;x, q_<i, k>=q((i-1/2) &xutri;x, k&xutri;t) (i=0,1,..., n+1) and h_<i, k>=h (i&xutri;x, k&xutri;t)(i=0,1,..., n), z_<0i>=z_0 (i&xutri;x) (i=0,1,..., n). Then q_<i, k> and h_<i, k> are placed alternately. The finite difference representations of Mahaffy's model are q_<i, k>=-{(h_<i, k> -h_<i-1,k>)/&xutri;x}^n{(h_<i, k>+h_<i-1,k>)/2+(z_<oi>+z_<oi>^-_1)/2}^<n+2> and h_<i, k+1>=h_<i, k>+&xutri;t{b-(q_<i+1,k>-q_<i, k>)/&xutri;x}. If i&xutri;x &isins; Ω_2,mq_<i, k> is used instead of q_<i, k>. Boundary conditions are q_<0,k>=(-1)^n q_<1,k> and h_<n, k>=0. In the three dimensional model, let Ω be the region of interest and ∂Ω be the boundary of Ω. For both sides of Mahaffy's model, we multiply the weighting function W_l and integrate in the interior region Ω and apply Green's theorem, &lmoust;_Ω k&xdtri;h・&xdtri;W_ldΩ-&lmoust;_<∂Ω>k (∂h/∂n) W_ldГ=&lmoust;_Ω(b-∂h/∂t) W_ldΩ, where ∂h/∂n=&xdtri;h・n in which n is the outer normal vector of ∂Ω. We divided the region Ω into N small regions Ω^e. Let M be the number of nodes and assign a number from 1 to M to each node. Let h^^^^ be the approximation of h. [numerical formula] where N_m (x, y) are basis functions which are 1 at the node m and 0 in small regions which do not include the node m. We take N_1 as the weighting function. Let k=k(h), b=b(h), K_<l, m> (h)=&lmoust;_Ω k{(∂N_m/∂x)(∂N_l/∂x)+(∂N_m/∂y)(∂N_l/∂y)}dΩ-&lmoust;_<∂Ω>k(∂N_m/∂n) N_ldГ, C_<l, m>=&lmoust;_ΩN_mN_ldΩ, &fnof;_l(h)=&lmoust;_ΩbN_ldΩ, K=(K_<l, m>)_<l, m=1,..., M, > C=(C_<l, m>)_<l, m=1,..., M> and f=(&fnof;_<1,..., >&fnof;_M)^T. Then we can write the integral equation as K(h)h+C(∂h/∂t)=f(h). We apply the backward difference method over time, and define h^<(n)>=h(n&xutri;t), K(h^<(n)>)h^<(n)>+C{(h^<(n)>-h^<(n-1)>)/&xutri;t}=f(h^<(n)>). When h^<(n-1)> is solved, h^<(n)> can be solved by an iterative method, substituting an initial value into h^<(n)>. [numerical formula] and K_<l, m> (h) are defined when using Ω^e instead of Ωin K_<l, m> (h) C_<l, m> and &fnof;_l (h) respectively. Then [numerical formula], and [numerical formula]. Here, [numerical formula] if l, m &notin; Ω^e. Letting [numerical formula], [numerical formula] and [numerical formula], we calculate K^e, C^e and f^e for each e at first, then find K, C and f. The two dimensional scheme was applied to the Shirase drainage basin, and the three dimensional to the entire Antarctic ice sheet. The results seem to be satisfactory, although further improvements are to be carried out.},
 title = {DEVELOPMENT OF A COMPUTER SIMULATION SCHEME FOR TWO AND THREE DIMENSIONAL ICE SHEET DYNAMICS MODELS},
 volume = {8},
 year = {1994}
}