Penetration of deformation‐driven meteoric water into ductile rocks: Isotopic and model observations from the Southern Alps, New Zealand

Upton, Phædra; Koons, P. O.; Chamberlain, C. Page

doi:10.1080/00288306.1995.9514680

Cited by 61 publications

(58 citation statements)

References 45 publications

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“…Large along-strike temperature anomalies cause pore fluid density and viscosity variations that influence fluid-rock interactions and provide a mechanism for deeper fluid convection, even though heat transport by fluids in low-permeability deeper rocks may be minor. Mineralogical evidence from near the Alpine Fault confirms that boiling occurs in the upper and mid-crust 31 and that meteoric fluids circulate through the entire seismogenic zone 32 .…”

Section: Letter Researchmentioning

confidence: 92%

Extreme hydrothermal conditions at an active plate-bounding fault

Sutherland

Townend

Toy

et al. 2017

Nature

110

174

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Section: Letter Researchmentioning

confidence: 92%

Extreme hydrothermal conditions at an active plate-bounding fault

Sutherland

Townend

Toy

et al. 2017

Nature

110

174

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“…Pattison & Harte 1988;Symmes & Ferry 1995;Johnson et al 2003), and water may infiltrate from adjacent units that have a higher temperature solidus, or along pervasive dilatant fractures, or in shear zones, or perhaps regionally where there is generally strong focusing into specific layers (e.g. Sibson 1986;Wickham & Taylor 1987;McCaig et al 1990;Upton et al 1995;Selbekk et al 2000;Johnson et al 2001;Connolly & Podladchikov 2004;Slagstad et al 2005;White et al 2005;Berger et al 2008;Florian et al 2008;Ward et al 2008;Rubatto et al in press). Given the limited porosity of high-grade subsolidus crust (Yardley 2009), deformation-enhanced permeability is likely required to facilitate fluid infiltration (e.g.…”

Section: (A) the Melting Process And Its Consequencesmentioning

confidence: 99%

The spatial and temporal patterning of the deep crust and implications for the process of melt extraction

Brown

2010

Phil. Trans. R. Soc. A.

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Volumetrically significant melt production requires crustal temperatures above approximately 800• C. At the grain scale, the former presence of melt may be inferred based on various microstructures, particularly pseudomorphs of melt pores and grainboundary melt films. In residual migmatites and granulites, evidence of melt-extraction pathways at outcrop scale is recorded by crystallized products of melt (leucosome) and residual material from which melt has drained (melanosome). These features form networks or arrays that potentially demonstrate the temporal and spatial relations between deformation and melting. As melt volume increases at sites of initial melting, the feedback between deformation and melting creates a dynamic rheological environment owing to localization and strain-rate weakening. With increasing temperature, melt volume increases to the melt connectivity transition, in the range of 2-7 vol% melt, at which point melt may escape in the first of several melt-loss events, where each event represents a batch of melt that left the source and ascended higher in the crust. Each contributing process has characteristic length and time scales, and it is the nonlinear interactions and feedback relations among them that give rise to the dissipative structures and episodicity of melt-extraction events that are recorded as variations in the spatial and temporal patterning of the crust. Focused melt flow occurs by dilatant shear failure of low-melt fraction rocks creating melt-flow networks that allow accumulation and storage of melt, and form the link for melt flow from grain boundaries to veins allowing drainage to crustal-scale ascent conduits. Preliminary indications suggest that anatectic systems are strongly self-organized from the bottom up, becoming more ordered by decreasing the number and increasing the width of ascent conduits from the anatectic zone through the overlying subsolidus crust to the ductile-to-brittle transition zone, where the melt accumulates in plutons.

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“…The overall structure of the Southern Alps is moderately well understood on the 50-100 km scale (Wellman 1979;Findlay & Sporli 1984;Koons 1989;). Likewise, tectonically induced hydrothermal systems which accompany the rise of the Southern Alps are documented on a regional scale and have been integrated into structural models (Holm et al 1989;Koons & Craw 1991a, b;Upton et al 1995). However, the details of structural evolution and associated fluid flow on the kilometre scale are less well understood.…”

Section: Introductionmentioning

confidence: 99%

Structure and fluid migration in a late Cenozoic duplex system forming the Main Divide in the central Southern Alps, New Zealand

Cox¹,

Craw²,

Chamberlain³

1997

New Zealand Journal of Geology and Geophysics

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The Alpine Schist immediately west of the Main Divide of the Southern Alps is a west-dipping duplex system consisting of an imbricated stack of rock slabs, each c. 250-1000 m thick. The imbricated stack has low grade, little deformed pumpellyite-actinolite facies semischists at the base, overlain by progressively higher grade and more deformed schists. The structurally highest slab mapped consists of multiply-deformed biotite zone schist. The duplex lies on the hanging wall of the northwest-dipping Main Divide Fault Zone, which separates semischist from structurally underlying greywacke. Rock slabs are internally disrupted by faults subparallel to layering, and consist of lozenge-shaped blocks of 10-100 m. Fault zones separating rock slabs consist of <50 cm thick zones of weakly lithified cataclasite and soft gouge. Slickensides on fault surfaces plunge northwest. The duplex formed during late Cenozoic rise of the Southern Alps.Four generations of postmetamorphic veins cut rock slabs of the duplex system. The earliest veins contain quartz, chlorite, calcite, and sulphides and lie subparallel to foliation in the higher grade slabs only. A distinctive set of openspace-filling fissure veins in a lower greenschist facies slab contains euhedral quartz, adularia, bladed calcite, and chlorite. The whole duplex system is cut by steeply dipping shears and fractures containing quartz and ankerite infilling and breccia cementation. Late stage iron oxy-hydroxidecoated fractures, generally steeply dipping, cut all rock slabs. Pyrite and, locally, arsenopyrite accompanies quartz and ankerite veins in extensional sites of steeply dipping late stage fractures, and gold contents up to 850 ppb occur. This G96031Received 2 September 1996; accepted 9 May 1997 gold mineralisation occurred within c. 1 km of the surface and had epithermal affinities.Hydrothermal fluids mineralising the various fractures range in temperature between 350°C and near-ambient temperatures. The quartz-adularia-calcite veins formed at 0.5-2.5 km depth before duplex formation, and later veins formed at shallower levels after duplex formation. Vein carbonates have δ 18 O(SMOW) between 11.4 and26.1%o, and Δ 13 C(PDB) between -0.6 and -11.4%o. Calculated isotopic ratios for the mineralising fluids show little evidence for meteoric origin. The fluid may be meteoric water which has undergone isotopic exchange with host rocks, metamorphic water, or a mixture of these, and mineralisation occurred during rise of the fluids from depth.

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Penetration of deformation‐driven meteoric water into ductile rocks: Isotopic and model observations from the Southern Alps, New Zealand

Cited by 61 publications

References 45 publications

Extreme hydrothermal conditions at an active plate-bounding fault

Extreme hydrothermal conditions at an active plate-bounding fault

The spatial and temporal patterning of the deep crust and implications for the process of melt extraction

Structure and fluid migration in a late Cenozoic duplex system forming the Main Divide in the central Southern Alps, New Zealand

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