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Volume 2017 (2017), Article ID 9687325, 12 pages
Research Article

Fluid Flow and Heat Transport Computation for Power-Law Scaling Poroperm Media

1Advanced Seismic Instrumentation and Research, 1311 Waterside, Dallas, TX 75218-4475, USA
2St1 Deep Heat Ltd, Purotie 1, 00381 Helsinki, Finland

Correspondence should be addressed to Peter Leary

Received 22 February 2017; Accepted 20 August 2017; Published 19 October 2017

Academic Editor: Mohamed Fathy El-Amin

Copyright © 2017 Peter Leary et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.


In applying Darcy’s law to fluid flow in geologic formations, it is generally assumed that flow variations average to an effectively constant formation flow property. This assumption is, however, fundamentally inaccurate for the ambient crust. Well-log, well-core, and well-flow empirics show that crustal flow spatial variations are systematically correlated from mm to km. Translating crustal flow spatial correlation empirics into numerical form for fluid flow/transport simulation requires computations to be performed on a single global mesh that supports long-range spatial correlation flow structures. Global meshes populated by spatially correlated stochastic poroperm distributions can be processed by 3D finite-element solvers. We model wellbore-logged Dm-scale temperature data due to heat advective flow into a well transecting small faults in a Hm-scale sandstone volume. Wellbore-centric thermal transport is described by Peclet number ( = wellbore radius, = fluid velocity at , = mean crustal porosity, and = rock-water thermal diffusivity). The modelling schema is (i) 3D global mesh for spatially correlated stochastic poropermeability; (ii) ambient percolation flow calibrated by well-core porosity-controlled permeability; (iii) advection via fault-like structures calibrated by well-log neutron porosity; (iv) flow ~ 0.5 in ambient crust and ~ 5 for fault-borne advection.