HR: 1340h
AN: G33B-0049    [Abstracts]
TI: Generalization of Farrell's loading theory: Applications to mass flux measurement using geodetic tequniques
AU: * Guo, J
EM: guo.81@osu.edu
AF: Laboratory for Space Geodesy and Remote Sensing, Ohio State University, 275 Mendenhall,125 S Oval Mall, Columbus, OH 43210 United States
AU: Shum, C
EM: ckshum@osu.edu
AF: Laboratory for Space Geodesy and Remote Sensing, Ohio State University, 275 Mendenhall,125 S Oval Mall, Columbus, OH 43210 United States
AB: In the classical ocean tide loading theory of Longman (1962, 1963) and Farrell (1972), the ocean bottom pressure is assumed to balance the gravitational force of the mass of load, and the load Love numbers describing the deformation of the Earth include the contributions of both the gravitation of the mass of load and the ocean bottom pressure. Let us denote the ocean surface hight relative to the average position by h, the density of ocean water by ρ_w, and the gravity at the Earth's surface by g_R. In the ocean tide loading problem, the Earth is deformed by both the gravitation of a thin layer of mass with a surface density μ=ρ_w h and the pressure p=μ g_R at ocean bottom. This implies that the pressure is assumed to balance the gravity force of the mass of load, i.e. the ocean is approximately considered to be in hydrostatic equilibrium state. In the formulation, the Earth is assumed spherical, the mass of load is assumed located at the Earth's surface and the pressure is assumed exerted at the Earth's surface, too. We generalize the classical loading theory for two more complicated cases that require to consider the effects of gravitation and pressure separately. The first case is the atmospheric loading where the pressure is exerted at the Earth's surface, and the mass of load is distributed over the elevation of the atmospheric thickness. The second case is the loading of fast oceanic phenomina like tsunami where the assumption of hydrostatic equilibrium is no longer valid, i.e. the pressure-surface density relation p=μ g_R no longer hold, and both ocean surface height and ocean bottom pressure should be provided as data based on the modelling of the fast phemonina. Based on our formulation, we provide Green's functions for computing the indirect effect. The computation of the dirrect effect remains the same as previous work. The resulting work contributes toward interpretation of the geodetic measurements-mass fluxes relation.
DE: 1218 Mass balance (0762, 1223, 1631, 1836, 1843, 3010, 3322, 4532)
DE: 1220 Atmosphere monitoring with geodetic techniques (6952)
DE: 1222 Ocean monitoring with geodetic techniques (1225, 1641, 3010, 4532, 4556, 4560, 6959)
SC: Geodesy [G]
MN: Fall Meeting 2005