Structure of the Otago schists

Wood, B. L.

doi:10.1080/00288306.1963.10423606

Cited by 55 publications

(32 citation statements)

References 11 publications

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“…The indication of modest induration during the early deformation is consistent with recumbent structures at a high level in the orogenic belt, perhaps formed by gravity tectonics. Recumbent folds, which predate the metamorphism, occur in Otago (Wood 1963, Means 1966, the Alpine Schists (Grindley 1963), and in the Torlesse rocks of the Lord Range, Westland.…”

Section: Tectonicsmentioning

confidence: 99%

“…Parts of the schist belt are also known in some detail (Grindley 1963, Wood 1963, Means 1963, Brown 1968, but, by contrast, the nonschistose Permian-Jurassic rocks of the Torlesse Facies have been largely neglected, and apart from pioneer studies in the Mt Cook region (Lillie 1962a, 1962b, Lillie and Gunn 1964, Waterhouse 1966, the structure and distribution of rock types within Torlesse Supergroup terrains remains virtually unknown.…”

Section: Introductionmentioning

confidence: 99%

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Stratigraphy and structure of the Torlesse Supergroup (Triassic-Jurassic) in the foothills of the southern Alps near Hawarden (S60–61), Canterbury

Bradshaw

1972

New Zealand Journal of Geology and Geophysics

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Section: Tectonicsmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Stratigraphy and structure of the Torlesse Supergroup (Triassic-Jurassic) in the foothills of the southern Alps near Hawarden (S60–61), Canterbury

Bradshaw

1972

New Zealand Journal of Geology and Geophysics

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“…Although differences exist in detail, a general similarity of interpretation holds. All w;orkers agree that deformation was polyphase, with large scale recumbent folds being produced, perhaps during the first phase (Wood 1963, Means 1963, and probably during the second (Brown 1968, Means 1966). An axial-plane foliation was produced during both phases (Wood 1963;Brown 1963;Means 1966).…”

Section: Comparison With Other Workmentioning

confidence: 81%

Stratigraphic, structural, and metamorphic relationships in the Dansey Pass area, Otago, New Zealand

Bishop

1974

New Zealand Journal of Geology and Geophysics

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In the Dansey Pass area, greywacke, semischist, and schist on the north-eastern margin of the Otago schist arc show a progressive increase in metamorphic grade from prehnite-pumpellyite to greenschist facies, or in terms of textural development, from non-foliated greywacke of textural zone 1 to laminated schist of textural zone 3B. Locally a stratigraphic sequence some 15000 m thick can be recognised, in which the metamorphic grade increases towards the top.The rocks have been affected by four periods of folding. The earliest phase, probably initially penecontemporaneous with the later stages of sedimentation, resulted in steeply dipping strata, overturned throughout extensive areas. Phase II folding may have commenced as the early phase progressed, as early Phase II structures show evidence of soft sediment deformation, although other evidence indicates that Phase II continued until welt into the metamorphic event. Isograds and isotects are not folded by Phase II structures, however, indicating that Phase II deformation was completed before the early Cretaceous metamorphic climax.Following metamorphism, post-metamorphic folds in both the foliation and in isogradic and isotectic surfaces formed on the outer edge of the schist belt, and were accompanied by important pre-peneplanation fault movements leading to deposition of the fanglomeratic middle-to-Iate-Cretaceous Kyeburn Formation in a major fault-angle depression. Deposition of the Kyeburn Formation was followed by regional peneplanation in the late Cretaceous and early Tertiary, before a thin veneer of middle Tertiary sediments was laid down.Plio-Pleistocene deformation during the Kaikoura Orogeny was dominated by faulting in the basement rocks, with locally strong folding of the covering strata. Large scale gentle warping of the foliation may have occurred at this time. The fault pattern seems to indicate vertical uplift rather than lateral shortening or Extension, and the rejuvenation of older faults, commonly with a reversal in the sense of movement, suggests a potentially reversible process is a necessary requirement of the fundamental mechanism.

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“…4). These structures were first described in detail for the Otago region by Wood (1963) and Means (1963Means ( , 1966, and folds of comparable style occur in many parts of the Otago Schist (Brown 1968;Turnbull 1981;Craw 1985;Mortimer 1993a). These structures are commonly viewed as having formed in a continuum of progressive development of macroscopic structures (e.g., Means 1966;Brown 1968;Turnbull 1981;Craw 1985;Cox 1991).…”

Section: Late Metamorphic Foldsmentioning

confidence: 99%

“…This metamorphic belt is structurally complex at all scales, particularly in the central portion of the Otago Schist. Structural continuity on a regional scale has commonly been assumed, for simplicity, when studying the belt as a whole (Wood 1963(Wood , 1978Suggate et al 1978;Mortimer 1993a,b). However, more recent work has shown that postmetamorphic structural discontinuities were important in the evolution of the geometry of the belt (Craw 1998;Mortimer 2000;Deckert et al 2002;Forster & Lister 2003).…”

Section: Introductionmentioning

confidence: 99%

Structural and lithological continuity and discontinuity in the Otago Schist, Central Otago, New Zealand

MacKenzie

Craw

2005

New Zealand Journal of Geology and Geophysics

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The Otago Schist in Central Otago has undergone complex late metamorphic and post-metamorphic deformation during uplift and exhumation. Two late metamorphic structural generations can be recognised and these may be genetically related. The earlier Manorburn Generation has been widely recognised and described previously. This generation has fold axes subparallel to a prominent syn-metamorphic quartz rodding lineation. A later generation, herein named Poolburn Generation, has folds which superficially resemble Manorburn Generation, but has fold axes that are at a high angle to the quartz rodding lineation. Both generations occur in mappable fold zones (kilometre-scale) that are generally not vergence boundaries, and some minor relative displacement may occur across fold zones. Fold zones occur within structurally and lithologically uniform schist domains. Abrupt changes in lithological sequences and orientations of structural elements such as Manorburn and Poolburn Generation fold axes and quartz rodding lineations occur at post-metamorphic faults which separate different schist domains. Central Otago schist can be subdivided on the regional scale (tens of kilometres) into at least nine schist domains whose structural and lithologic continuity is disrupted by fault discontinuities. The domains and bounding discontinuities developed during Late Jurassic and Early Cretaceous uplift. Syn-metamorphic compressive ductile deformation evolved to localised fold zones in the early stages of this uplift. Subsequently, regional extension caused juxtaposition of domains with different textural zones, and schists from slightly different structural levels. The Caples/Torlesse Terrane boundary is a composite feature, and different segments formed at different stages through the transition from ductile compression to brittle extensional deformation.

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Structure of the Otago schists

Cited by 55 publications

References 11 publications

Stratigraphy and structure of the Torlesse Supergroup (Triassic-Jurassic) in the foothills of the southern Alps near Hawarden (S60–61), Canterbury

Stratigraphy and structure of the Torlesse Supergroup (Triassic-Jurassic) in the foothills of the southern Alps near Hawarden (S60–61), Canterbury

Stratigraphic, structural, and metamorphic relationships in the Dansey Pass area, Otago, New Zealand

Structural and lithological continuity and discontinuity in the Otago Schist, Central Otago, New Zealand

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