The use of porphyroblasts to resolve the history of macro-scale structures: an example from the Robertson River Metamorphics, North-Eastern Australia

Cihan, M.; Parsons, Andrew J.

doi:10.1016/j.jsg.2005.02.004

Cited by 23 publications

(34 citation statements)

References 30 publications

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“…At the onset of the Mesoproterozoic large tracts of central and eastern Australia underwent a period of orogenesis (circa 1620 and 1580 Ma) (Figure 10). The orogenic history is preserved in the Arunta Inlier (Chewings Orogeny), Curnamona Province (Olarian Orogeny), Gawler Craton (Kararan Orogeny), Mount Isa Inlier (Isan Orogeny) and Georgetown Inlier (Jana Orogeny) [ Betts et al , 2006; Blenkinsop et al , 2008; Cihan et al , 2006; Cihan and Parsons , 2005; Collins et al , 1995; Daly et al , 1998; Forbes et al , 2004, 2007; Gibson et al , 2008; Giles et al , 2006b; Hand et al , 2007; MacCready , 2006a; O'Dea et al , 1997b, 2006; Potma and Betts , 2006; Rubatto et al , 2001; Vry et al , 1996] (Figures 1 and 10). The circa 1610–1560 Ma Chewings Orogeny [ Collins and Shaw , 1995] is characterized by early thin‐skinned deformation and nappe emplacement during north directed thrusting [ Teyssier et al , 1988], followed by the development of upright, shallowly plunging folds with ∼east‐west trending axial traces [ Collins and Shaw , 1995].…”

Section: End‐member Tectonic Modelsmentioning

confidence: 99%

“…Time‐space diagram with the age and style of orogenesis throughout eastern Australian Proterozoic geological provinces [ Bell , 1983; Betts et al , 2000; Binns , 1964; Blake , 1987; Blewett and Black , 1998; Blewett et al , 1998; Boger and Hansen , 2004; Cihan et al , 2006; Cihan and Parsons , 2005; Clark et al , 2006a, 2006b; 1986, 1987; Collins and Shaw , 1995; Collins et al , 1995; Connors and Page , 1995; Daly et al , 1998; Davis et al , 2001; De Jong and Williams , 1995; Etheridge and Cooper , 1981; Forbes and Betts , 2004; Forbes et al , 2004, 2005, 2007; Ganne et al , 2005; Gibson and Nutman , 2004; Gibson et al , 2004; Giles et al , 2006a, 2006b; Giles and Nutman , 2002, 2003; Hills , 2004; Hobbs et al , 1984; Laing et al , 1978; Lewthwaite , 2001; Lister et al , 1999; Loosveld , 1992; MacCready , 2006a, 2006b; MacCready et al , 1998, 2006; Marjoribanks et al , 1980; McLean and Betts , 2003; O'Dea et al , 2006; O'Dea and Lister , 1995; O'Dea et al , 1997a; Oliver et al , 1998; Foster and Rubenach , 2006; Page et al , 2005a; Page and Laing , 1992; Potma and Betts , 2006; Raetz et al , 2002; Reinhardt , 1992; Reinhardt and Rubenach , 1989; Rubenach , 1992; Rubena...…”

Section: End‐member Tectonic Modelsmentioning

confidence: 99%

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Mesoproterozoic plume‐modified orogenesis in eastern Precambrian Australia

et al. 2009

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Tectonic models for the latest Paleoproterozoic to earliest Mesoproterozoic evolution of eastern Australia (circa 1620–1500 Ma) are diverse and either emphasize plume or plate margin activity, neither of which satisfactorily explains all geological observations. The dichotomy is largely attributed to geochemical, spatial and temporal data that suggest voluminous A‐type felsic magmas are plume related, whereas distribution of arc‐related magmas and intense orogenic overprint suggest plate margin activity. The salient geological events include arc‐related magmatism at circa 1620–1610 Ma followed by a magmatic hiatus coincident with north‐south crustal shortening (1610–1590 Ma) and a magmatic flare‐up of A‐type felsic magmas throughout the Gawler Craton (circa 1595–1575 Ma). These magmas form the oldest component of a northward younging hot spot track that extends to the Mount Isa Inlier. At circa 1590–1550 Ma, arc magmatism resumed along the northern margin of the Gawler Craton and the rest of eastern Australia records a 90° shift in the regional shortening direction related to activity along the eastern margin of the Australian continent. A plume‐modified orogenic setting satisfies all of the spatial and temporal relationships between magma generation and orogenic activity. In this model, the Gawler Craton and the adjacent subduction zone migrated over a mantle plume (circa 1620–1610 Ma). Resultant flat subduction caused transient orogenesis (1610–1595 Ma) in the overriding plate. Slab delamination and thermal assimilation of the plume and the subducting slab caused a switch to crustal extension in the overriding plate, resulting in extensive mantle‐derived and crustal melting in the Gawler Craton (1595–1575 Ma).

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Section: End‐member Tectonic Modelsmentioning

confidence: 99%

Section: End‐member Tectonic Modelsmentioning

confidence: 99%

Mesoproterozoic plume‐modified orogenesis in eastern Precambrian Australia

et al. 2009

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“…SSITs appear so obviously a product of rotation of the porphyroblast within a foliation as progressive shearing occurred that no one considered the possibility that this might not be the case until the 1980s. However, a technique for quantitatively measuring the axes of SSITs was developed (Hayward, 1990;Bell, Forde & Wang, 1995) and a large amount of data has now been published on the orientation of spiral axes around folds (Bell & Hickey, 1997;Hickey & Bell, 2001;Bell & Chen, 2002;Timms, 2004), around oroclines (Bell & Mares, 1999;Yeh & Bell, 2004) and along and across orogens (Bell & Bruce, 2006;Bell, Hickey & Upton, 1998;Bell, Ham & Hickey, 2003, Bell, Ham & Kim, 2004Bell et al 2005;Cihan, 2004;Cihan & Parsons, 2005). He also generated a non-coaxial strain field diagram that mimicked asymmetric crenulation cleavages and straight to slightly sigmoidal inclusion trails that are common in so many porphyroblasts.…”

Section: E Alpine Top-to-the-s Shearing During Main Menderes Metammentioning

confidence: 99%

Extensional v. contractional origin for the southern Menderes shear zone, SW Turkey: tectonic and metamorphic implications

Bozkurt

2006

Geol. Mag.

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The southern Menderes Massif in southwest Turkey consists mainly of orthogneisses and overlying Palaeozoic-Middle Paleocene schists and marbles. The contact between the two distinct rock types is almost everywhere structural, herein named the southern Menderes shear zone: a S-facing, high-angle ductile shear zone that separates metamorphic rocks of differing grade. Although there is a consensus that the shear zone was associated with top-to-the-S-SSW shearing and is of Tertiary age, its origin and nature have been highly debated over the last decade. Some claim the contact is a thrust fault, while others have argued for an extensional shear zone. Integration of field and microstructural data (the identification of different fabrics, associated kinematics and overprinting relationships) with fissiontrack thermochronology and the P-T paths of the rocks above and below the shear zone, supports the conclusion that the southern Menderes shear zone is an extensional shear zone and not a thrust. The data are consistent with a model that the exhumation and cooling of the southern Menderes Massif occurred after a period of extensional deformation. Pervasive top-to-the-N-NNE high-temperature-mediumpressure ductile shear structures (D 2 deformation) overprint an early HP event (D 1 deformation). The subsequent top-to-the-S-SSW greenschist shear band foliation (D 3 deformation) developed mostly around the orthogniess-schist contact and forms the most characteristic features of the massif. The topto-the-N-NNE structures are attributed to the main Alpine constructional deformation that developed during back-thrusting of the Lycian nappes during the latest Palaeogene collision between the Sakarya continent and the Anatolide-Tauride platform across the Neotethyan Ocean. The top-to-the-S-SSW structures are interpreted to be the result of the exhumation of the massif during the activity of the southern Menderes shear zone. The presence of these two distinct fabrics with differing kinematics suggests that the southern Menderes shear zone operated as a top-to-the-N-NNE thrust fault during early Alpine contractional deformation but was later reactivated with an opposite sense of movement (top-to-the-S-SSW) during subsequent Oligocene-Miocene extensional collapse.

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“…Only interpretations of the origin of variably oriented and spiral-shaped inclusion trails have been used to suggest porphyroblasts rotate signifi cantly during ductile deformation of rocks. Data that are independent of the interpretation of the origin of such microstructures, such as foliation intersection/infl ection axes (FIA) preserved in porphyroblasts (e.g., Bell and Mares, 1999;Cihan and Parsons, 2005;Sayab, 2005;Rich, 2006;Yeh, 2007), indicate that they do not. None of these FIA successions, matched by progressively younger ages when dated using monazite (Bell and Welch, 2002;I.…”

Section: References Citedmentioning

confidence: 99%