Deformation of partially molten granite: a review and comparison of experimental and natural case studies

Rosenberg, Claudio

doi:10.1007/s005310000164

Cited by 108 publications

(75 citation statements)

References 77 publications

(173 reference statements)

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“…Melt topology also reflects grain-scale melt migration pathways [Marchildon and Brown, 2001;Rosenberg, 2001]. Sawyer [2001] reviewed criteria for recognition of former presence of melt on grain scale in deformed rocks.…”

Section: Melt Topologymentioning

confidence: 99%

“…A typical feature of some rapidly quenched melting experiments is the development of melt pools with cuspate margins [Jurewicz and Watson, 1984] or thin melt films along crystal faces [Daines and Kohlstedt, 1997]. Melt phase crystallized as albite, quartz or K-feldspar grains at triple point junctions or at crystal faces in residual aggregates have been commonly reported from natural examples and interpreted in terms of melt topology in partially molten granite [e.g., Brown et al, 1999;Rosenberg and Riller, 2000;Marchildon and Brown, 2001;Rosenberg, 2001].…”

Section: Melt Topologymentioning

confidence: 99%

“…The melt could have been produced by in situ melting reaction or by infiltration from external sources, which is reflected by the melt composition under estimated PT conditions and possible reaction textures [Sawyer, 2001]. Another important issue is the melt volume produced and volume change of the melting reaction, as both these variables control the embrittlement of rock at dynamic conditions during breakdown reactions of some hydrous phase and/or at sufficient heating rates [Connolly et al, 1997;Rosenberg, 2001;Rushmer, 2001;Holyoke and Rushmer, 2002]. These data have critical impact on the described melt topology, deformation mechanisms and rheology of studied orthogneiss and will be further discussed.…”

Section: Melt Producing Reaction and Melt Volume Estimatesmentioning

confidence: 99%

“…[3] Melt bearing microstructures in deformed rocks can be also used for reconstruction of grain-scale melt migration pathways, because deformation and melt extraction are coupled [Brown and Rushmer, 1997;Rosenberg and Handy, 2000;Rosenberg, 2001]. A typical feature of deformation experiments at low melt volumes is the preferential distribution of melt along grain boundaries oriented at low angle to principal compressive stress direction [Dell' Angelo et al, 1987;Daines and Kohlstedt, 1997;Gleason et al, 1999;Rosenberg and Handy, 2000].…”

Section: Introductionmentioning

confidence: 99%

“…This is due to two reasons: (1) Natural melt-bearing microstructures equilibrated at high-grade conditions are likely to be overprinted by subsequent static or dynamic recrystallization [Rosenberg and Riller, 2000;Rosenberg, 2001]. (2) High finite strains, slow creep rates and high homologous temperatures necessary to introduce high-temperature melt-enhanced deformation mechanisms (e.g., diffusion creep or dislocation climb accommodated GBS [Boullier and Gueguen, 1975]) cannot be attained using conventional experimental facilities.…”

Section: Introductionmentioning

confidence: 99%

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Extreme ductility of feldspar aggregates—Melt‐enhanced grain boundary sliding and creep failure: Rheological implications for felsic lower crust

Závada

Schulmann²,

Konopásek

et al. 2007

J. Geophys. Res.

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[1] High-grade orthogneisses from granulite-bearing lower crustal unit show extreme finite strains of both K-feldspar and plagioclase with respect to weakly deformed quartz aggregates. K-feldspar aggregate in the most intensely deformed sample shows interstitial grains of quartz and albite, which also mark some intragranular fractures within K-feldspar grains. Both interstitial grains and fractures are oriented mostly perpendicular to the sample stretching lineation. Quartz and albite grains within K-feldspar bands are interpreted as crystallized from interstitial melt and the petrology study shows that the melt was produced by a metamorphic reaction in plagioclase-mica bands. Thermodynamic Perple_X modeling shows that melt volume increase was negligible and melt amount was too small to generate considerable melt overpressure for calculated PT conditions. It is therefore suggested that dilation of K-feldspar aggregates and fracturing of its grains represent a final creep failure state, which resulted from the cavitation process accompanying grain boundary sliding controlled diffusion creep. The consequence of cavitation-driven dilation of K-feldspar aggregates is the local underpressure resulting in infiltration of melt from plagioclase bands. Analogy with metallurgy experiments shows that the cavitation process, exclusively developed in cryptoperthitic K-feldspar, can be attributed to its lower purity compared to more pure plagioclase. Contrasting rheological behavior of feldspars with respect to quartz prior to fracturing is attributed to different deformation mechanisms. Feldspars appear weaker due to grain boundary sliding accommodated by coupled melt-enhanced diffusion creep along grain boundaries and dislocation creep within grains, in contrast to quartz deforming via grain boundary migration accommodated dislocation creep.Citation: Závada, P., K. Schulmann, J. Konopásek, S. Ulrich, and O. Lexa (2007), Extreme ductility of feldspar aggregates-Meltenhanced grain boundary sliding and creep failure: Rheological implications for felsic lower crust,

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Section: Melt Topologymentioning

confidence: 99%

Section: Melt Topologymentioning

confidence: 99%

Section: Melt Producing Reaction and Melt Volume Estimatesmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Extreme ductility of feldspar aggregates—Melt‐enhanced grain boundary sliding and creep failure: Rheological implications for felsic lower crust

Závada

Schulmann²,

Konopásek

et al. 2007

J. Geophys. Res.

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Strain partitioning along the anatectic front in the Variscan Montagne Noire massif (southern French Massif Central)

et al. 2015

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We decipher late-orogenic crustal flow characterized by feedback relations between partial melting and deformation in the Variscan Montagne Noire gneiss dome. The dome shape and finite strain pattern of the Montagne Noire Axial Zone (MNAZ) result from the superimposition of three deformations (D1, D2 and D3). The early flat-lying S1 foliation is folded by D2 upright ENE-WSW folds and transposed in the central and southern part of the MNAZ into steep D2 high-strain zones consistent with D2 NW-SE horizontal shortening, in bulk contractional coaxial deformation regime that progressively evolved to noncoaxial dextral transpression. The D2 event occurred under metamorphic conditions that culminated at 0.65 ± 0.05 GPa and 720 ± 20°C. Along the anatectic front S1 and S2 foliations are transposed into a flat-lying S3 foliation with top-to-NE and top-to-SW shearing in the NE and SW dome terminations, respectively. These structures define a D3 transition zone related to vertical shortening during coaxial thinning with a preferential NE-SW to E-W directed stretching. Depending on structural level, the metamorphic conditions associated with D3 deformation range from partial melting conditions in the dome core to subsolidus conditions above the D3 transition zone. We suggest that D2 and D3 deformation events were active at the same time and resulted from strain partitioning on both sides of the anatectic front that may correspond to a major rheological boundary within the crust.

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Particle‐Based Modeling of Pull‐Apart Basin Development

Liu

Konietzky

2018

Tectonics

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A scale‐independent modeling approach based on the discrete element method has been established to investigate the development of pull‐apart basins. The main findings can be summarized as follows. Thirty degree underlapping models produce pull‐apart basins that evolve from spindle‐shaped through lazy‐Z‐shaped to rhomboidal and stretched rhomboidal basin. Ninety degree nonoverlapping and 150° overlapping models generate rhomboidal pull‐apart basins without going through spindle‐shaped and lazy‐Z‐shaped stages. The shape of a pull‐apart basin is the consequence of both the initial strike‐slip fault geometry and its various evolution stages. Rhomboidal basins, which have larger basin length than the amount of motion, form in overlapping systems and do not progress through the spindle‐shaped and lazy‐Z‐shaped stages such as the Dead Sea basin. Rhomboidal basins with cross‐basin faults tend to form in underlapping systems. All the numerical models show nearly the same trend for maximum principal stress versus relative extension εx* (horizontal opening divided by fault separation). Peak stress and onset of crack propagation are observed for εx* of ~0.035. The relative extension to form the first depression is ~0.155. Therefore, for a pull‐apart to form in nature, the displacement and time needed to form the first cracks and depression area can be estimated from the corresponding εx* and the slip rate of the strike‐slip faults. The time needed to form the first depression can be considered as the minimum age of initiation for the pull‐apart basin. This method to deduce the starting age of pull‐apart basin development can be used for basins which are still active.

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Deformation of partially molten granite: a review and comparison of experimental and natural case studies

Abstract: Experimental and natural investigations of partially molten granite are compared and reviewed.

Cited by 108 publications

References 77 publications

Extreme ductility of feldspar aggregates—Melt‐enhanced grain boundary sliding and creep failure: Rheological implications for felsic lower crust

Extreme ductility of feldspar aggregates—Melt‐enhanced grain boundary sliding and creep failure: Rheological implications for felsic lower crust

Strain partitioning along the anatectic front in the Variscan Montagne Noire massif (southern French Massif Central)

Particle‐Based Modeling of Pull‐Apart Basin Development

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