This implies that, in general, when estimating geoelectric fields during a magnetic storm, one cannot expect a simple 1D model of the conductivity distribution of the subsurface to apply to a wider physiographic region.
A numerical formalism developed for compilation of the model, allows for its further refinement by incorporation of regional 3D conductivity distributions inferred from the real electromagnetic data.
The Laplace-transform finite-difference method is used to numerically model discrete fracture network flow, with sufficient flexibility to consider arbitrary fracture geometries and conductivity distributions.
SMAP, US Array and Geoscience Australia conductivity datasets are originally available as "true" 3D conductivity distributions.
We have interpolated it onto our model grid to form a 3D conductivity distribution.
Here, jext is the extraneous (impressed) current, time-harmonic dependency is e -iwt, μ 0 is the magnetic permeability of free space, (i = sqrt { - 1},omega = 2pi /T) is the angular frequency, T is the period of the variations, σ r, ϑ, ϕ is the conductivity distribution in the model, and ϑ and ϕ are co-latitude and longitude respectively.
In contrast, retrieval of the saturated hydraulic conductivity distribution allows the CATHY model to reproduce the integrated hydrological response of LEO for all sensor configurations investigated.
a code to compute the EM field in a spherical model of the Earth with a 3-D conductivity distribution.
The plots for MNB36 further show a much larger difference in (Z_{xx}) and (Z_{yy}), indicating that the subsurface conductivity distribution is more representative of a 3-dimensional conductivity model.
This model (Kauffman et al. 2001) was then updated using MODFLOW-2005 (Harbaugh 2005) and the hydraulic conductivity distribution was further refined by comparing observed and simulated groundwater age distributions.
