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Borehole breakout Created 2026-10-24 Updated 2026-11-05
A borehole breakout forms when the concentrated compressive stress around a drilled hole fractures and removes part of its wall. Opposed damaged sectors widen the originally circular hole. A borehole televiewer images the wall so that the enlargement and its orientation can be distinguished from an isolated natural fracture.
For an approximately vertical hole aligned with a principal stress direction, the long axis of the breakout follows the minimum horizontal compressive stress direction. The strongest tangential compression occurs there even though the distant horizontal compression in that direction is smaller. Inclined holes, pore pressure, drilling pressure and rock strength require a fuller model before orientations or magnitudes are inferred.[ref]
Well bore breakouts and in situ stress by Mark D. Zoback and others. Abstract: ultrasonic wall images and enlargement toward minimum horizontal compression
Borehole televiewer 2026-11-05
A borehole televiewer produces an oriented image of a borehole wall, often by scanning with acoustic pulses. Recorded echo amplitude and travel time reveal changes in wall reflectivity and radius as a function of depth and azimuth.
An enlarged cross-section can indicate borehole breakout, while fractures produce other characteristic traces. Inferring the surrounding stress requires a mechanical interpretation of those features; the image alone does not directly measure every stress component. Borehole conditions and tool orientation affect the result.
Mark D. Zoback 2026-11-05
Mark D. Zoback coauthored research using borehole breakouts to infer in-situ crustal stress. The orientation and shape of borehole-wall failure become informative through a mechanical model relating local stress concentration to the far-field stress.[ref]
Well bore breakouts and in situ stress by Mark D. Zoback and others. author list and the described study’s abstract or introductory account
Support for the left curve comes from high laboratory friction and substantial in situ differential stress; support for the right curve comes from low inferred fault traction, weak fault materials or high pore pressure. No single observation directly measures the whole plotted envelope.
For the left, stronger shallow-crust model:
- Many friction experiments on ordinary rocks give a coefficient of friction around 0.6–0.85. Together with approximately hydrostatic pressure, these values predict increasing frictional strength with depth.
- Deep-borehole measurements of stress and pore pressure in some continental settings indicate a crust close to frictional failure at appreciable differential stress. Jointly with appropriate fault orientations, these support a strong frictional upper crust.
For the right, weak shallow-layer model:
- On well-studied plate-boundary faults, low resolved shear stress inferred from the orientation of principal stresses relative to the active fault plane can support low effective traction.
- The absence of the expected localized long-term frictional heating anomaly can support weak sliding. Directly measured high pore pressure or very low-friction fault gouge would give a physical explanation. The heat-flow and stress evidence is particularly developed for the San Andreas Fault; it is an analogue argument, not an observation that the entire Cascadia upper crust follows that curve.[ref]Stress orientations at intermediate angles to the San Andreas Fault, California by Jeanne L. Hardebeck and Andrew J. Michael. 2004, introduction and discussion of strong and weak fault models
To discriminate, measure the strength-controlling quantities through depth and across both faults and their surroundings. Obtain borehole stress, pore pressure and temperature profiles where feasible; use borehole breakouts and hydraulic tests to constrain effective stress. Recover fault and host rocks and test their friction and material creep at relevant fluid conditions. The right curve specifically predicts an end to the shallow weakening near its sharp rise: investigate changes in permeability of a porous medium, alteration and fault gouge with depth, rather than testing only a surface sample.
Combine those measurements with heat flux transects, magnetotelluric sounding for conductive fluids, accurate earthquake depths and focal mechanisms, and GNSS or InSAR observations of deformation. The latter can help constrain the depth distribution of locking and postseismic relaxation, but neither locking nor seismicity alone gives absolute strength. Earthquake stress drop is a change in stress, not the pre-event stress. Low heat flux can also reflect heat transport or transient weakening; high electrical conductivity can have causes other than free water. A joint explanation of all these data is needed to choose between the models locally.