Sentence examples for pore pressurization from inspiring English sources

Before a pore pressurization, optimally oriented faults are assumed to be close to shear failure condition regardless of depth since earthquake swarms are ongoing beneath the volcano (< 6 km in depth).

For all the cases (A D), very local and shallow pore pressure reduction of about 0.1 MPa occurs above the obstruction, with pressurization below the obstruction.

Three-dimensional stress and pore pressure distributions around a hydraulic fracture are numerically calculated to analyze the potential for formation failure resulting from pressurization of the hydraulic fracture.

While the pressurization in Cases A and B is ~0.1 MPa, pressurization reaches several MPa in most parts of the model space in the lower-permeability Cases C and D. This might be an overestimate, as the pore pressure changes in these calculations are comparable to the lithostatic load.

The excess pore water pressure at the base of the landslide may be produced by grain-crushing (Gerolymos and Gazetas 2007), dilatancy (Savage and Iverson 2009), effective stress (Luna and Remaitre 2012), and thermal pressurization (Vardoulakis 2000; Goren and Aharonov 2007; De Blasio and Elverhøi 2008; Goren and Aharonov 2009).

We do not consider evolution of the effective normal stress such as thermal pressurization of pore fluid (Mitsui and Hirahara 2009) for simplicity.

The shorter weakening distance is most likely due to pressurization of pore fluid by shear-enhanced compaction, and probably not by shear heating because almost no temperature rise takes place during slip weakening (Figure 3a).

We adopt a hypothesis that dynamically thermal pressurization of pore fluid (hereinafter called TP) in the fault zone played a key role in the release of stress (Mitsui et al., 2012).

We assume a dynamic weakening mechanism (dynamic thermal pressurization of pore fluid, hereinafter called TP) on the fault plane to represent nonlinear weakening friction, and take into account the shear stress changes before the Tohoku earthquake, due to the four M 7-class earthquakes that occurred during 2003 2011.

For example, once the coseismic slip evolves in a fluid-saturated fault, thermal pressurization of pore fluid (e.g., Mitsui and Hirahara, 2009) can operate as a dynamic process to promote seismic slip even on a weak fault with a low absolute level of stress.

The other is the thermal pressurization of pore fluid (TP) via frictional heating, heat flow, and fluid flow, i.e., the law of energy conservation, the Fourier law, the law of mass conservation, and the Darcy law (Sibson, 1973; Lachenbruch, 1980; Mase and Smith, 1987; Bizzarri and Cocco, 2006).