Strike-slip tectonics is concerned with the structures formed by, and the tectonic processes associated with other zones of lateral displacement within the Earth's crust or lithosphere, such as transform boundaries. It is one of the three main types of plate tectonic regime (and respective plate boundaries), the others being extensional tectonics (divergent boundary) and thrust tectonics (convergent boundary). Areas of strike-slip tectonics are associated with particular deformation styles including Riedel shears, flower structures and strike-slip duplexes. This type of tectonics is characteristic of several geological environments, including oceanic and continental transform faults, zones of oblique collision and the deforming foreland of a zone of continental collision.

Deformation styles

Development of Riedel shears in a zone of dextral shear
Development of Riedel shears in a zone of dextral shear
Flower structures developed along minor restraining and releasing bends on a dextral (right-lateral) strike-slip fault
Flower structures developed along minor restraining and releasing bends on a dextral (right-lateral) strike-slip fault

Riedel shear structures

In the early stages of strike-slip fault formation, displacement within basement rocks produces characteristic fault structures within the overlying cover. This will also be the case where an active strike-slip zone lies within an area of continuing sedimentation. At low levels of strain, the overall simple shear causes a set of small faults to form. The dominant set, known as R shears, forms at about 15° to the underlying fault with the same shear sense. The R shears are then linked by a second set, the R' shears, that forms at about 75° to the main fault trace.[1] These two fault orientations can be understood as conjugate fault sets at 30° to the short axis of the instantaneous strain ellipse associated with the simple shear strain field caused by the displacements applied at the base of the cover sequence. With further displacement, the Riedel fault segments will tend to become fully linked until a throughgoing fault is formed. The linkage often occurs with the development of a further set of shears known as 'P shears', which are roughly symmetrical to the R shears relative to the overall shear direction.[2] The somewhat oblique segments will link downwards into the fault at the base of the cover sequence with a helicoidal geometry.[3]

Flower structures

In detail, many strike-slip faults at surface consist of en echelon and/or braided segments, which in many cases were probably inherited from previously formed Riedel shears. In cross-section, the displacements are dominantly reverse or normal in type depending on whether the overall fault geometry is transpressional (i.e. with a small component of shortening) or transtensional (with a small component of extension). As the faults tend to join downwards onto a single strand in basement, the geometry has led to these being termed flower structure. Fault zones with dominantly reverse faulting are known as positive flowers, while those with dominantly normal offsets are known as negative flowers. The identification of such structures, particularly where positive and negative flowers are developed on different segments of the same fault, are regarded as reliable indicators of strike-slip.[4]

Strike-slip duplexes

Strike-slip duplexes occur at the step over regions of faults, forming lens-shaped near parallel arrays of horses. These occur between two or more large bounding faults which usually have large displacements.[5]

An idealized strike-slip fault runs in a straight line with a vertical dip and has only horizontal motion, thus there is no change in topography due to motion of the fault. In reality, as strike-slip faults become large and developed, their behavior changes and becomes more complex. A long strike-slip fault follows a staircase-like trajectory consisting of interspaced fault planes that follow the main fault direction.[6] These sub-parallel stretches are isolated by offsets at first, but over long periods of time, they can become connected by step overs to accommodate the strike-slip displacement.[5] In long stretches of strike-slip, the fault plane can start to curve, giving rise to structures similar to step overs.[7]

Right lateral motion of a strike-slip fault at a right step over (or overstep) gives rise to extensional bends characterised by zones of subsidence, local normal faults, and pull-apart basins.[5] On extensional duplexes, normal faults will accommodate the vertical motion, creating negative relief. Similarly, left stepping at a dextral fault generates contractional bends; this shortens the step overs which are displayed by local reverse faults, push-up zones, and folds.[7] On contractional duplex structures, thrust faults will accommodate vertical displacement rather than being folded, as the uplifting process is more energy-efficient.[7]

Strike-slip duplexes are passive structures; they form as a response to displacement of the bounding fault rather than by the stresses from plate motion.[6] Each horse has a length that varies from half to twice the spacing between the bounding fault planes. Depending on the properties of the rocks and the fault, the duplexes will have different length ratios and will develop on either major or subtle offsets, although it is possible to observe duplex structures that develop on nearly straight fault segments.[7] Because the motion of the duplexes may be heterogeneous, the individual horses can experience a rotation with a horizontal axis, which results in the formation of scissor faults. Scissor faults exhibit normal motion at one end of the horse and a thrust motion at the other end.[7] Because strike-slip duplexes structures have more horizontal motion than vertical motion, they are best observed on a map rather than a vertical projection and are a good indication that the main fault has a strike-slip motion.[5]

An example of strike-slip duplexes was observed in the Lambertville sill, New Jersey.[8] Flemington and the Hopewell faults, the two main faults in the region, experienced 3 km of dip-slip and over 20 km of strike-slip motions to accommodate regional extension. It is possible to trace the lensoidal structures which are interpreted as horses that form duplexes.[8] The lens structures observed in the 3M quarry are 180 meters long and 10 meters wide. The main duplex is 30 m in length and other smaller duplexes are also present.[8]

Geological environments associated with strike-slip tectonics

San Andreas Transform Fault on the Carrizo Plain
San Andreas Transform Fault on the Carrizo Plain

Areas of strike-slip tectonics are associated with:

Oceanic transform boundaries

Mid-ocean ridges are broken into segments offset from each other by transform faults. The active part of the transform links the two ridge segments. Some of these transforms can be very large, such as the Romanche fracture zone, whose active portion extends for about 300 km.

Continental transform boundaries

Transform faults within continental plates include some of the best-known examples of strike-slip structures, such as the San Andreas Fault, the Dead Sea Transform, the North Anatolian Fault and the Alpine Fault.

Lateral ramps in areas of extensional or contractional tectonics

Major lateral offsets between large extensional or thrust faults are normally connected by diffuse or discrete zones of strike-slip deformation allowing the transfer of the overall displacement between the structures.

Zones of oblique collision

In most zones of continent-continent collision, the relative movement of the plates is oblique to the plate boundary itself. The deformation along the boundary is normally partitioned into dip-slip contractional structures in the foreland with a single large strike-slip structure in the hinterland accommodating all the strike-slip component along the boundary. Examples include the Main Recent Fault along the boundary between the Arabian and Eurasian plates behind the Zagros fold and thrust belt,[9] the Liquiñe-Ofqui Fault that runs through Chile and the Great Sumatran fault that runs parallel to the subduction zone along the Sunda Trench.

The deforming foreland of a zone of continent-continent collision

The process sometimes known as indenter tectonics, first elucidated by Paul Tapponnier, occurs during a collisional event where one of the plates deforms internally along a system of strike-slip faults. The best known active example is the system of strike-slip structures observed in the Eurasian Plate as it responds to collision with the Indian Plate, such as the Kunlun fault and Altyn Tagh fault.[10]


  1. ^ Katz, Y.; Weinberger R.; Aydin A. (2004). "Geometry and kinematic evolution of Riedel shear structures, Capitol Reef National Park, Utah" (PDF). Journal of Structural Geology. 26 (3): 491–501. Bibcode:2004JSG....26..491K. doi:10.1016/j.jsg.2003.08.003. Retrieved 6 May 2011.[permanent dead link]
  2. ^ Tchalenko, J.S. (1970). "Similarities between Shear Zones of Different Magnitudes". Geological Society of America Bulletin. 81 (6): 1625–1640. Bibcode:1970GSAB...81.1625T. doi:10.1130/0016-7606(1970)81[1625:SBSZOD]2.0.CO;2.
  3. ^ Ueta, K.; Tani, K. 2001. Ground Surface Deformation in Unconsolidated Sediments Caused by Bedrock Fault Movements: Dip-Slip and Strike-Slip Fault Model Test and Field Survey. American Geophysical Union, Fall Meeting 2001, abstract #S52D-0682
  4. ^ Harding, T.P. 1990. Bulletin American Association of Petroleum Geologists. 74
  5. ^ a b c d Keary, P. (2009), Global Tectonics, vol. 3, ISBN 978-1-118-68808-3
  6. ^ a b Woodcock, Nigel (1986), "Strike-slip duplexes", Journal of Structural Geology, 8 (7): 725–735, Bibcode:1986JSG.....8..725W, doi:10.1016/0191-8141(86)90021-0
  7. ^ a b c d e Burg (1986), Strike-slip and oblique-slip tectonics (PDF)
  8. ^ a b c Laney, A. (1996), "Three-dimensional shuffling of horses in a strike-slip duplex: an example from the Lambertville sill, New Jersey", Tectonophysics, 258 (1–4): 53–70, Bibcode:1996Tectp.258...53L, doi:10.1016/0040-1951(95)00173-5
  9. ^ Talebian, M. Jackson, J. 2004. A reappraisal of earthquake focal mechanisms and active shortening in the Zagros mountains of Iran Geophysical Journal International, 156, pages 506–526
  10. ^ Tapponnier, P. & Molnar, P. 1979. Active faulting and Cenozoic tectonics of the Tien Shan, Mongolia and Baykal regions. Journal Geophysical Research, 84, B7, 3425 – 3459. Archived 2011-06-06 at the Wayback Machine