By James P. Verdon
This thesis offers a powerful precis of the aptitude to take advantage of passive seismic the way to display screen the sequestration of anthropogenic CO2 in geologic reservoirs. It brings jointly leading edge learn in detailed components – seismology and geomechanics – and contains either info research and numerical modelling. the information come from the Weyburn-Midale venture, that's at present the biggest Carbon catch and garage (CCS) venture on the earth. James Verdon’s effects convey how passive seismic tracking can be utilized as an early caution process for fault reactivation and most sensible seal failure, that may bring about the get away of CO2 on the surface.
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Extra info for Microseismic Monitoring and Geomechanical Modelling of CO2 Storage in Subsurface Reservoirs
D) shows the error surface and cluster analysis. A good result will have one clearly defined error minimum picked splitting analysis windows. An F-test is used to normalised this surface such that a value of 1 represents the 95% confidence interval. The cluster analysis is also displayed to the right of this panel. The upper cluster analysis panel shows the results (ψ and δVS ) of the splitting measurement for each of the splitting analysis windows. The lower cluster analysis panel maps the results for each window in ψ − δVS space, highlighting the clusters identified by SHEBA.
When computing BN and BTh , μr = C66 11 r r r r r when computing BT v , μ = C44 and λ + 2μ = C33 ). Kfl and μfl are the bulk and shear moduli of the fluid (usually, μfl = 0), and ξ and a are the scalar density and average aspect ratio of the fracture set. The fracture density is a non-dimensional term given by the number of fractures in a volume and their average radius, ξ = Nr3 /V . For the assumption of isolated fractures made by Hudson (1981) to be valid, either the pore space and fractures must be hydraulically isolated (this is unrealistic for reservoir rocks), or the frequency of the propagating wave must be high enough that there is no time for the pressure gradient to be equalised.
The splitting parameters ψ and δVS for each raypath are calculated using the Christoffel equation. , Al-Harrasi et al. 2010). Because there will also be uncertainty regarding the event location, and therefore the angle of wave propagation through the rock, I also add noise of ±10◦ to the inclinations and azimuths of the synthetic data—this is done after the splitting operators have been computed. This then represents the ‘observed’ dataset, which I use to invert for the initial model parameters.
Microseismic Monitoring and Geomechanical Modelling of CO2 Storage in Subsurface Reservoirs by James P. Verdon