Kink-Bands and Related Geological Structures

Anderson, T. B.

doi:10.1038/202272a0

Cited by 69 publications

(36 citation statements)

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“…Both sets plot in the same part of the diagram and suggest a slight to moderate volume increase due to kink band development. Although such a volume increase (dilation) is often accommodated by the development of fractures and veins (Anderson, 1964;Ramsay and Huber, 1987), our examples do not show evidence for this. Possibly, much of the dilation occurred at relatively low fluid pressures, under conditions unfavourable for quartz precipitation, resulting in a less obvious extension (e.g.…”

Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 53%

“…On the kink band triangle of Srivastava et al (1998), with added curves of expected volume change (Anderson, 1964;Ramsay and Huber, 1987), only minor differences are observed between the four kink band sets (Fig. 12).…”

Section: North Dobrogea Orogen (Romania)mentioning

confidence: 95%

“…Fig. 8 shows the kink band data plotted on a kink band triangle of Srivastava et al (1998), on which we added curves of expected volume change due to kink band development (Anderson, 1964;Ramsay and Huber, 1987). There is no significant difference between both kink band sets in terms of internal geometry.…”

Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 99%

“…This does not imply, however, that these structures have a brittle nature. Also the presence of fractures along kink band boundaries, resulting from the accommodation of thickness changes due to kink band development or from later failure along the kink band boundary (Anderson, 1964;Dewey, 1966;Ramsay and Huber, 1987), is no argument for a brittle origin. In this respect, it is worth considering that experiments only resulted in kink bands at high confining pressures, much higher than those leading to shear fracture development (e.g.…”

Section: Uncertainties Regarding Kink Bands: Brittle or Ductile Origimentioning

confidence: 99%

“…Paterson and Weiss, 1962;Ramsay, 1962;Anderson, 1964;Cobbold et al, 1971). Even if a direct link between kink band geometry and palaeostress is assumed, the question can be raised whether the pre-existing local anisotropy may have influenced the (far-field) stress directions (cf.…”

Section: Introductionmentioning

confidence: 99%

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Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Debacker

Seghedi

Belmans

et al. 2008

Journal of Structural Geology

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a b s t r a c tKink bands within two slate belts, the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania), reveal similar problems with respect to linking kink band geometries to expected palaeostress directions. In the North Dobrogea Orogen, the two opposite kink band sets of two different systems of conjugate kink bands develop for a wide variety of cleavage orientations. In the Anglo-Brabant Deformation Belt, the occurrence of the two opposite kink band sets of a conjugate kink band system opposes the expected occurrence. In both cases, this can be attributed to stress deflection along a pre-existing anisotropy. Moreover, the presence of kink bands in the North Dobrogea Orogen with curving kink axes (and curving kink band boundaries) also puts doubt on the direct relationship between kink band geometry and stress. The idea of stress deflection along a pre-existing anisotropy and the strong control of the pre-existing anisotropy on the kink band geometry and orientation has important implications for the use of kink bands as regional palaeostress indicators. Depending on the relative intensity and relative orientation of the pre-existing fabrics (here bedding and cleavage), different mechanisms of kink band development may operate. Depending on the mechanism, different solutions in terms of inferred palaeostress direction may exist.

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Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 53%

Section: North Dobrogea Orogen (Romania)mentioning

confidence: 95%

Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 99%

Section: Uncertainties Regarding Kink Bands: Brittle or Ductile Origimentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

See 3 more Smart Citations

Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Debacker

Seghedi

Belmans

et al. 2008

Journal of Structural Geology

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Succession and structure in the Llwyd Mawr Syncline, Caernarvonshire north Wales

Робертс

1967

Geological Journal

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A succession of strata ranging in age from Upper Cambrian to Valentian is described. They occupy ground in, and adjacent to, the Llwyd M a w syncline. Most of the rocks arc marine but during midCaradocian (Soudleyan) times a rhyolitic ignimbrite sheet was emplaced and rests disconformably on Llanvirn slates. It has a remanant thickness of 2300 ft and is a single cooling unit. A second volcanic episode (Lower Longvillian) produced 600 ft of bedded pyroclastic rocks with only subordinate ignimbrites. MidCaradocian minor intrusions of rhyolite occur as domes and sills in aswciation with the volcanic rocks. Minor intrusions of dolerite and micro-tonalite are probably of Caledonian age.T h e phases of movement am recognized within the main end-Silurian Caledonian movements. The first movement phase, PI, produced the main fold architecture and the dominant associated axial-planar cleavage, SI. The folds, which possess a Caledonoid trend, usually stand vertically. but rarely they verge slightly to the southcast. They are periclinal in styk. The sccond movement phase, Fz, was weak and produced a sporadically distributed set of opcn folds and associated axial-planar crenulation cleavage, Sz, of Caledonoid strike. The axial-planes dip gently to the southeast quadrant. Folds of the third movement phase, F3, plunge northwest and the associated axial-planar crenulation cleavage, SJ, dips steeply to the northcast. The F3 folds produce a pronounced arcuation in the trace of the FI structures from an azimuth of 60" in the northwest to 10" in the south of the area. INTRODUmIONThe area occupied by the Llwyd Maw syncline (Fig. 1) lies immedi'ately west of MoelHebog and covers 46 square miles. The ground extends southward from the Vale of Nantlle to the coast at Criccieth. Much of the terrain is rugged in the north where the degree of exposure varies from excellent to good, but it falls progressively southward and exposure becomes poor. The extent of the thick drift cover in the southwest has made interpretation of the geology uncertain; consequently this area is described as "eonjectural" on the accompanyhg geological map (Pl. 16).The sedimentary rocks exposed range in age from Cambrian (Lingula Flags : Ffestiniog Beds) to Sdurian (Valentian). Igneous rocks include a spectacular development of welded tuf€ of mid-caradocian age, the Llwyd M a w ignimbrite, together with a series of ash-fall tuffs and penecontemporaneous rhyolite intrusions. In addition dolerites and a microtonalite are present which are closely related to the end-Silurian movements of the Caledonian orogcny.The area was examined by Sedgwick (1831-2) and the rocks were briefly described (1843). Sdwyn mapped the area for the Geological Survey and it received mention in Ramsay's memoir on North W a l e s (1866, 1881). Fearnsides (1910) described a MITOW strip of country in the southeast and Harper (1947, 1956)

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The origin and development of kink‐bands in a foliated body

Dewey

1969

Geological Journal

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Although the deformation of foliated rocks by kink and glide mechanisms has been studied in detail in recent years, fundamental differences of opinion have emerged, particularly as a result of experimental work. Most theories concerning the relationship of kink-bands to stress-fields are empirically based. Evidence on whether kink-bands are the result. of a shear couple and on limiting factors for external rotation is presented. It is concluded that kink-bands are zones of externally rotated foliation bounded by kink-planes which develop parallel to planes of high shearing stress at infinitesimal strain.Quoique la dkformation de roches feuilletkes par mkhanismes de glissement et de "kink" mdchanismes, fait ttC ttudiCe en dttail au cours des dernitres anntes, des difftrences fondamentales d'opinion ont vu le jour, en particulier en consequence du travail exptrimental. La plupart des thkories concernant la relation des "Kink-bands" aux champs de tension sont bastes empiriquement. Des informations sur soit que les "Kink-bands" sont le rtsultat d'un couple de cisaillement et sur des facteurs de limite pour la rotation externe sont pr6sentCes. II en est conch que les "Kinkbands" sont des zones de foliation tournte externement, limittes par des "Kink-plans" qui se developpent parallelement B des plans h haut cisaillement avec tension infinitCsimale.Obwohl die Verformung schiefriger Gesteine durch "kink and glide"-Mechanismen wahrend der letzten Jahre bis in Einzelheiten hinein erforscht worden ist, haben sich grundsatzlich voneinander abweichende Meinungen gebildet, die sich auf experimentelle Untersuchungen stiitzen. Die meisten Theorien iiber das Verhaltnis von "kink-bands" gegenuber Druckfeldern sind empirisch begriindet. In dieser Abhandlung werden zwingende Tatsachen dariiber veroRentlicht, ob "kink-bands" die Folge eines Scherdruckpaares und einschrankender Faktor fur eine 3uOere Drehung sind. Es wird gefolgert, daO "kink-bands" Zonen von SuOerlich gedrehter Schieferung sind, umgeben von "kink"-Flachen, die sich parallel zu Ebenen hohen Scherdruckes unter unendlich geringer Spannung entwickeln. STATEMENT OF THE PROBLEMThe nature and inception of kink-bands in foliated rocks have received considerable attention during the last five years. Donath (1961;1964a; 1964b), Paterson and Weiss (1962;1966) and Borg and Handin (1966) were concerned largely with the experimental deformation of foliated pelites, whereas Anderson (1 964), Marshall (1964;1966), and Dewey (1965;1966) described naturally-occurring kink-bands and suggested mechanisms for their origin and development. As a result of these investigations divergent opinions have. been expressed concerning three main aspects of kinking. The problems are: (1) whether kink-bands are the result of the operation of a shear couple parallel to kink-planes or whether they develop by kink-plane migration from a point or line source? (2) what determines the inclination of kink-planes to foliation ? and (3) what determines the amount of external rotation within kink-bands ? It i...

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Kink-Bands and Related Geological Structures

Cited by 69 publications

References 7 publications

Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Succession and structure in the Llwyd Mawr Syncline, Caernarvonshire north Wales

The origin and development of kink‐bands in a foliated body

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