Detachment fold

A detachment fold occurs as layer parallel thrusting along a detachment fault develops without upward propagation of a fault; the accommodation of the strain produced by thrusting results in the folding of the overlying rock units. As a visual aid, picture a rug on the floor. By placing your foot on one end and pushing toward the other, the rug slides across the floor (detachment fault) and folds upward (detachment fold). Detachment faulting and folding may occur in either a compressional or extensional environment; though they serve the same purpose, they are controlled by different modes and thus are defined by these modes. Extensional detachment faulting is essentially defined by a low angle normal fault (dip-slip fault), while detachment folding and faulting in compressional settings result from the accommodation of strain. Figure 1, is a generalized representation of the geometry assumed by a detachment fault.

Figure 1. The general geometry of a detachment fold illustrating a layer parallel detachment fault undergoing shortening and the resulting geometry of a detachment fold.

Detachments in a Compressional Environment:

Definitions:

Detachment folding occurs as strain imposed on a mechanically weak layer or incompetent unit, such as shale or salt, or at the boundary between an incompetent and more competent unit, induces resistance from the units resulting in folding typically observed in the competent unit ^{[1, 2, 3]}. Once the resistance of these units is overcome with strain or the variation in strain between the units becomes great enough, a shearing motion known as a detachment fault may occur. Defined, a detachment fault may be located within an incompetent unit or at the boundary of an incompetent and a competent unit, which accommodates for strain differences between the units and allows displacement to occur in a planar field ^{[1, 2, 3, 4, 5]}. Detachment folding occurs in regions of thick-skinned deformation, where the basement is involved in deformation and thin-skinned deformation, where deformation occurs at relatively shallow depth in the crust.

Modes of Detachment Folding:

One of the principal ideas that should be recognized in each model is the law of conservation of volume, as conservation is a fundamental law in physics; it should also apply to geology. Two ways to maintain volume conservation are thickening of units and synclinal deflection of incompetent material; it is likely that both may occur.

Figure 2. A model of the law of conservation of volume by synclinal deflection; that is the area (given by A then a subscript) of the anticline should be equal to the area of shortening plus the synclinal deflection A1 = A2+A3+A4. Synclinal deflection below the origin (dotted line) is shown marked by the A3 and A4.

^[6] Contreras, J (2010) developed a model for low amplitude detachments using the conservation of mass equation. The results suggest the occurrence of layer thickening as an initial response to shortening and volume conservation. ^[7] Hayes and Hanks (2008) confirm layer thickening during the onset of folding, specifically their field data places the thickening at the hinges of folds rather than the limbs. When defining the geometry of detachment folding it may be necessary to define layer thickening as it has been recorded to affect the overall geometry ^[7]. Though variable limb thickness is assumed; over time, limb rotation and limb length become the dominant mechanisms for deformation, leading to an increase in fold amplitude ^[6].

Synclinal deflection, figure 2, is the result of folding where synclines, adjacent to an anticline in fold geometry, extend into the lower incompetent unit; these typically occur in regions of high wavelength and low amplitude ^[3]. The occupancy of this area causes displacement above the detachment in the form of material migration to the anticlinal core ^{[3, 8]}. Withdrawal from the regional position is dependent on thickness and viscosity differences between the competent and incompetent units as well as the ductile nature of the incompetent unit ^{[3, 8]}. ^[3] Mitra (2003), like ^[6] Contreras, recognized a transition from unit deflection and material migration, to limb rotation and limb lengthening.

Detachment Fold Evolution:

Though many models have been developed to help explain the kinematic evolution of single layer detachment faulting; ^{[7, 9, 10, 11, 12]} many models do not account for multiple layers, complex fold geometries ^[12] or differential strain through fold geometries or mechanically dissimilar stratigraphic units ^[13]. These models may not be good indicators of detachment folding on a large scale and are better suited to assist in interpreting fold geometries of detachment folds as their kinematic evolution is generally associated with single fold, single unit deformations. The definition of disharmonic folds (below) however, incorporates many types of symmetric folds over a larger area encompassing many geometries and attributes of the basic models and may be better suited to the application of these models.

Figure 3. Disharmonic folding of a detachment fold using a symmetric geometric fold as a model. As compression develops, space issues arise in the anticlinal core. To accommodate these space issues folding becomes tighter within the inner units, creating a disharmonic fold geometry.

By incorporating elementary fold geometries ^{[7, 9, 10, 11, 12]} under the term disharmonic fold detachment folds may then be classified into one of two categories; disharmonic folds or lift-off folds. Disharmonic folds, figure 3, are defined as detachment folds characterized by parallel geometries at the outer limbs and non-parallel interlimb geometries at stratigraphically distinct and lower units; caused by differential strain as a result of strain dissipation or change in mechanical stratigraphy, where the termination of folding typically results in a detachment ^{[2, 3, 12]}. Lift-off detachment folds are characterized by isoclinal folding in all units, with a tight isoclinal folded weak unit in the anticline and parallel geometries sometimes existing along the outer units ^{[3, 14]}. Present day examples detachment folding can be found in the Jura Mountains of Central Europe. This region compliments the idea of detachment fold evolution put forth by ^[3] Mitra, (2003) in that it encompasses many of the basic fold geometries and comprises both disharmonic and lift-off geometries.

Disharmonic and lift-off detachment folds are commonly assumed to form by separate modes of deformation; however, ^[3] Mitra (2003) in a unified kinematic model challenged these ideas by suggesting an evolution of detachment folding wherein progressive deformation yields a fold transition from disharmonic geometry to lift-off detachment folding. While most kinematic models are developed to yield the most simplistic geometries by placing boundary conditions within the model and limiting variables; the unified model incorporates: mechanical stratigraphy parameter ^[2],limb lengthening, limb rotation ^{[6, 9, 14]}, area balancing and anticlinal and synclinal deflection, to develop a system that uniformly demonstrates the evolution of detachment folding.

The evolution of detachment folding begins with the model assumption of a low-amplitude and short compressional environment with a mechanically dissimilar incompetent and competent unit. Folding initiates by shortening; limb lengthening and rotation and hinge migration, cause synclinal deflection below its original position accompanied by the flow of ductile material beneath the synclinal trough to the anticlinal core; resulting in increased amplitude of the anticlinal fold ^{[3, 4, 5, 6, 15]}.

Further compression dominated by hinge migration, yields tightening of folds and space accommodation issues within the anticlinal core; leading to the formation of disharmonic folds ^{[14, 16]}. ^[17] Epard and Groshong, (1994) recognize a similar pattern to disharmonic folding they label it second-order shortening. Basic models and experiments ^{[4, 6, 12, 18]} as well as concentric fold models ^{[9, 19]} fail to recognize disharmonic folds as they focus on single layer detachment folding, lack the resolution in experimental methods or, though the assumption of multiple units is made, restrict unit parameters which may cause disharmony through deformation. Continued shortening and excess material within the anticlinal core not only results in increased amplitude and disharmonic folds, but may lead to the onset of thrusts out of the folded synclinal or anticlinal regions. Through further deformation by limb rotation and through hinge migration, isoclinal folds eventually assume lift-off geometries ^{[3, 4]}. Thrust faults in the synclinal fold, if any formed, may also be rotated to assist in the formation of detached lift-off folds upon further tightening and rotation ^[3] (figure 4). Reference Mitra 2002 ^[4] and Mitra 2003 ^[3] for more detailed models of rotation and folding in detachment folds.

Detachment Faulting:

Figure 4. Schematic depicting faulting of a symmetric detachment fold. The result of continued limb rotation and compression is the formation of faults in the forelimb and backlimb of the fold. Eventually these faults reconnect with the detachment and a pop-up may occur.

It is documented in many cases that faulting may develop from detachment folding or through the kinematic mechanisms involved with folding ^{[3, 4, 6, 14, 15, 18, 20]}. In general, faulting may occur during fault slip and detachment folding in two ways. Firstly, faulting may be induced when progressive folding or tightening of a folded limb reaches its maximum fold geometry resulting in a transition from folding to shearing ^{[4, 12]}. Secondly, it has been suggested a fault may propagate into the anticlinal core if material flow and accommodation space are not at equilibrium ^[4]. The idea of insufficient material flow may not be as well addressed as faulting due to continued folding and rotation, but the grounds for such an argument lay within a strongly held belief of area conservation; without conservation faulting will likely compensate. The basic geometries of detachment faulting of a symmetric detachment fold are shown in figure 4. Refer to Mitra ^{[4, 15]} for an evolutionary model of faulted detachment folds in the asymmetric and symmetric settings.

Faulting may occur in a symmetric or asymmetric fold, yielding fault geometries that are both alike and dissimilar. Faulting in either setting is reliant on the lock-up and strain accumulation of a fold typically at its critical angle. Asymmetric folding develops in the forelimb (the limb furthest from the source of thrust) of the fold and may either absorb strain into or transmit strain through the stratigraphic units composing the fold ^[15]. A system that absorbs strain is recognized as a trishear zone ^[21] being triangular in shape; while a parallel deformation zone transmits shear across the units of the fold ^[15] and typically takes on the form of a parallelogram or is rectangular in geometry. These two deformation patterns may exist in a single fold and at some time during continued deformation may reconnect with the detachment. It is also the case that a backthrust may occur in an asymmetric fold geometry as shear across the forelimb due to rotation and migration of beds.

Symmetric faults were essentially covered previously under the name ‘lift-off’ folds, see figure 4. Progressive limb rotation and lock-up in a symmetric fold induces shear at both the forelimb and backlimb of the fold which may then result in faults on both limbs causing lift-off. Like the asymmetric fold faulting, as progressive slip along the basal detachment occurs, either the forelimb or backlimb (the limb closest to the source of thrust) thrust may reconnect with the basal detachment ^[15]. For a more robust definition of faulting reference Mitra 2002 ^{[4, 15]}.

References

1. Homza T and Wallace W. (1994). Geometric and kinematic models for detachment folds with fixed and variable detachment depths. Journal of Structural Geology, 17/4: 575-588.

2. Hayes M and Hanks C. (2008). Evolving mechanical stratigraphy during detachment folding. Journal of Structural Geology, 30: 548-564.

3. Mitra S. (2003). A unified kinematic model for the evolution of detachment folds. Journal of Structural Geology, 25: 1659-1673.

4. Mitra S. (2002). Structural models of faulted detachment folds. American Association of Petroleum Geologist Bulletin, 86/9: 1673-1694.

5. Stewart S. (1996). Influence of detachment layer thickness on style of thin-skinned shortening. Journal of Structural Geology, 18/10: 1271-1274.

6. Contreras, J. (2010). A model for low amplitude detachment folding and syntectonic stratigraphy based on the conservation of mass equation. Journal of Structural Geology, 32, 566-579.

7. Hardy, S. and Poblet, J. (1994). Geometric and numerical model of progressive limb rotation in detachment folds. Geology, 22, 371-374.

8. Wiltschko, D.V. and Chapple, W. M. (1977). Flow of weak rocks in Appalachian Plateau folds. American Association of Petroleum Geologists Bulletin, 61, 5, 653-669.

9. Dalstrom, C. D. C. (1990). Geometric constraints derived from the law of conservation of volume and applied to evolutionary models for detachment folding. American Association of Petroleum Geologists Bulletin, 75, 3, 336-344.

10. Suppe, J. (1983). Geometry and kinematics of fault-bend folding. American Journal of Science, 283, 684-721.

11. Mitchel, M. M. and Woodward, N. B. (1988). Kink detachment fold in the southwest Montana fold and thrust belt. Geology, 16, 162-165.

12. Poblet, J. and McClay, Ken. (1996). Geometry and kinematics of single-layer detachment folds. American Association of Petroleum Geologists Bulletin, 80, 7, 1085-1109.

13. Fischer, M. and Jackson, P. (1999). Stratigraphic controls on eformation patterns in fault-related folds: a detachment fold example from the Sierra Madre Oriental, northeast Mexico. Journal of Structural Geology, 21,613-633.

14. Hardy, S. and Finch, E. (2005). Discrete-element modeling of detachment folding. Basin Research, 17, 507-520.

15. Mitra, S. (2002). Fold-accommodation faults. American Association of Petroleum Geologists Bulletin, 86, 4, 671-693.

16. Mitra, S. and Namson, J. (1989). Equal-area balancing. American Journal of Science, 289, 563-599.

17. Epard, J. L. and Groshong, R. H., Jr. (1994). Kinematic model of detachment folding including limb rotation, fixed hinges and layer-parallel strain. Tectonophysics 247, 85-103.

18. Storti, F., Salvini, F., and McClay, K. (1997). Fault-related folding in sandbox analogue models of thrust wedges. Journal of Structural Geology, 19, 3-4, 583-602.

19. Dahlstrom, C. D. A. (1969). Balanced cross sections. Canadian Journal of Earth Sciences, 6, 743-757.

20. Bowsworth, W. (1983). Foreland deformation in the Appalachian Plateau, central New York: the role of small-scale detachment structures in regional overthrusting. Journal of Structural Geology, 6, 1-2, 73-81.

21. Zehnder, A. T. and Allmendinger, R. W. (2000). Velocity field for the trishear model. Journal of structural Geology, 22, 1009-1014.