Access the full text.
Sign up today, get DeepDyve free for 14 days.
Loading next page...
/lp/wiley/friction-overpressure-and-fault-normal-compression-2UzwLDbZJr
References (20)
-
L. Ping (1963)
MEASURING EXTREMELY LOW FLOW VELOCITY OF WATER IN CLAYSSoil Science, 95
-
McGuigan McGuigan, Israelachvili Israelachvili, Gee Gee, Homola Homola (1989)
Measurements of static and dynamic interactions of molecularly thin liquid films between solid surfacesMat. Res. Soc. Symp., 140
-
J. Israelachvili, P. McGuiggan, A. Homola (1988)
Dynamic Properties of Molecularly Thin Liquid FilmsScience, 240
-
B. Hanshaw, J. Bredehoeft (1968)
On the Maintenance of Anomalous Fluid Pressures: II. Source Layer at DepthGeological Society of America Bulletin, 79
-
Miller Miller, Low Low (1963)
Threshold gradient for water flow in clay systemsProc. Soil Sci. Am., 27
-
Zoback Zoback, Healy Healy (1989)
Overview of In‐situ stress measurements in the Cajon Pass scientific drill hole to a depth of 3.5 kin, (abstract)Eos Trans. AGU, 70
-
A. Sylvester (1988)
Strike-slip faultsGeological Society of America Bulletin, 100
-
Raymond Miller, P. Low (1963)
Threshold Gradient for Water Flow in Clay SystemsSoil Science Society of America Journal, 27
-
K. Shedlock, T. Brocher, S. Harding (1990)
Shallow structure and deformation along the San Andreas fault in Cholame Valley, California, based on high-resolution reflection profilingJournal of Geophysical Research, 95
-
N. Watts (1987)
Theoretical aspects of cap-rock and fault seals for single- and two-phase hydrocarbon columnsMarine and Petroleum Geology, 4
-
M. Zoback, M. Zoback, V. Mount, J. Suppe, J. Eaton, J. Healy, D. Oppenheimer, P. Reasenberg, L. Jones, C. Raleigh, I. Wong, O. Scotti, C. Wentworth (1987)
New Evidence on the State of Stress of the San Andreas Fault SystemScience, 238
-
Von Engelhardt Von Engelhardt, Tunn Tunn (1955)
The flow of fluids through sandstones. (Translated by P.A. Witherspoon from Heidelbeger Beltrage Zur Mineralogie und Petrographie 2,12–25, 1954)Illinois State Geol. Survey Cir., 194
-
A. Homola, J. Israelachvili, M. Gee, P. McGuiggan (1989)
Measurements of and Relation Between the Adhesion and Friction of Two Surfaces Separated by Molecularly Thin Liquid FilmsJournal of Tribology-transactions of The Asme, 111
-
D. Swartzendruber (1962)
Non‐Darcy flow behavior in liquid‐saturated porous mediaJournal of Geophysical Research, 67
-
Radney Radney, Byeflee Byeflee (1988)
Laboratory studies of the shear strength of montmoril onite (abstract)Eos Trans. AGU, 69
-
J. Lutz, W. Kemper (1959)
Intrinsic Permeability of Clay as Affected by Clay-Water InteractionSoil Science, 88
-
P. McGuiggan, J. Israelachvili, M. Gee, A. Homola (1988)
Measurements of Static and Dynamic Interactions of Molecularly Thin Liquid Films Between Solid SurfacesMRS Proceedings, 140
-
D. Lockner, J. Byerlee (1990)
An example of slip instability resulting from displacement-varying strengthpure and applied geophysics, 133
-
R. Chapman (1977)
Abnormal formation pressuresEarth-Science Reviews, 13
-
Watts Watts (1987)
Theoretical aspects of cap‐rock fluid seals for single and two phase hydrocarbon colummMarine and Petroleum Geology, 4
- Publisher
- Wiley
- Copyright
- Copyright © 1990 by the American Geophysical Union.
- ISSN
- 0094-8276
- eISSN
- 1944-8007
- DOI
- 10.1029/GL017i012p02109
- Publisher site
- See Article on Publisher Site
Abstract
More than twenty‐five years ago Miller and Low reported the existence of a threshold pore pressure gradient below which water would not flow through clay. Recent experimental observations of the shear strength of structured water on biotite surfaces have provided a physical basis for understanding this threshold gradient. The existence of this phenomenon has profound implications for the rheological properties of mature fault zones, such as the San Andreas, that contain large thicknesses of fault gouge. For example, a clay–filled fault zone about 1 km wide at the base of the seismogenic zone decreasing to zero width at the surface could support core fluid pressure equal to the maximum principal stress over the entire seismogenic zone. As a result, the fault would have near‐zero strength and the maximum principal stress measured on the flanks of the fault, would be oriented normal to the fault surface. Another consequence of the threshold gradient is that normal hydrostatic fluid pressures outside the fault zone could coexist with near‐lithostatic fluid pressures in the interior of the fault zone without the need for continual replenishment of the overpressured fluid. In addition, the pore pressure at any point should never exceed the local minimum principal stress so that hydrofracture will not occur.
Journal
Geophysical Research Letters – Wiley
Published: Nov 1, 1990