High temperature flow and dynamic recrystallization in carrara marble

Schmid, Stefan M.; Paterson, M. S.; Boland, J. N.

doi:10.1016/0040-1951(80)90077-3

Cited by 324 publications

(218 citation statements)

References 16 publications

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“…2c. For comparison, Schmid et al (1977) and Schmid et al (1980) obtained the constants n 1 = 7.6, B 1 = 10 -13.51 for high temperature of Carrara marble and n 2 =1.7, B 2 = 10 -3.10 for Solnhofen limestone, assuming a grain size exponent of 3, which are in close agreement.…”

Section: Aggregate Strengthmentioning

confidence: 72%

Strain localization during high temperature creep of marble: The effect of inclusions

et al. 2014

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The deformation of rocks in the Earth's middle and lower crust is often localized in ductile shear zones. To better understand the initiation and propagation of high-temperature shear zones induced by the presence of structural and material heterogeneities, we performed deformation experiments in the dislocation creep regime on Carrara marble samples containing weak (limestone) or strong (novaculite) second phase inclusions. The samples were mostly deformed in torsion at a bulk shear strain rate of ≈ 1.9x10 -4 s -1 to bulk shear strains γ between 0.02 and 2.9 using a Paterson-type gas deformation apparatus at 900°C temperature and 400 MPa confining pressure. At low strain, twisted specimens with weak inclusions show minor strain hardening that is replaced by strain weakening at γ > 0.1 -0.2.Peak shear stress at the imposed conditions is about 20 MPa, which is ≈8% lower than the strength of intact samples. Strain progressively localized within the matrix with increasing bulk strain, but decayed rapidly with increasing distance from the inclusion tip.Microstructural analysis shows twinning and recrystallization within this process zone, with a strong crystallographic preferred orientation, dominated by {r} and (c) slip in .Recrystallization-induced weakening starts at local shear strain of about 1 in the process zone, corresponding to a bulk shear strain of about 0.1. In contrast, torsion of a sample containing strong inclusions deformed at similar stress as inclusion-free samples but do not show localization. The experiments demonstrate that the presence of weak heterogeneities initiates localized creep at local stress concentrations around the inclusion tips. Recrystallizationinduced grain size reduction may only locally promote grain boundary diffusion creep. Accordingly, the bulk strength of the twisted aggregate is close to or slightly below the lower (isostress) strength bound, determined from the flow strength and volume fraction of matrix and inclusions.

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Section: Aggregate Strengthmentioning

confidence: 72%

Strain localization during high temperature creep of marble: The effect of inclusions

et al. 2014

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“…Grain boundary migration took place but only where required to retain approximately equiaxed grainshapes (Bell and Etheridge, 1976;Etheridge and Kirby, 1983). The absence of significant softening under some experimental conditions, especially those involving subgrain rotation may be consistent with this microstructural model (Schmid et al, 1980;Kirby and Etheridge, 1983).…”

Section: Continued Deformation After Substantial Recrystallizationmentioning

confidence: 53%

“…The phenomenon of subgrain rotation, whereby the misorientation across sub-boundaries increases with strain until high-angle boundaries are formed, was first alluded to by Hobbs (1968), and has been widely inferred (largely from optical observations) for a number of minerals (White, 1973(White, , 1977Poirier and Nicolas, 1975;Bell and Etheridge, 1976;Schmid et al, 1980;Etheridge and Kirby, 1983). It has been concluded that dislocations enter sub-boundaries faster than they can be annihilated during straining, giving rise to progressively higher boundary misorientations.…”

Section: The Nucleation Stagementioning

confidence: 99%

“…In some metals and many minerals, however, the misorientation between subgrains increases with creep strain, eventually resulting in substantial recrystallization. This mechanism of dynamic recrystallization has become known as subgrain rotation, and has been widely recognized in quartz (Hobbs, 1968;White, 1973White, , 1976White, , 1977Bell and Etheridge, 1976), olivine (Poirier and Nicolas, 1975), pyroxene , calcite (Schmid et al, 1980) and feldspar (White, 1975).…”

Section: Introductionmentioning

confidence: 99%

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Dynamic Recrystallization in a Naturally Deformed Albite

Gerald

Etheridge

Vernon

1982

Texture, Stress, and Microstructure

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Coarse-grained, deformed albite occurs in veins within a blueschist from the Cazadero region, California. In some grains, deformation and recrystallization are concentrated in narrow shear zones less than 50/m wide. We have examined the substructural progression across these zones by transmission electron microscopy (TEM), in an attempt to determine the details ofthe dynamic recrystallization mechanism. The misorientation across subgrain and recrystallized grain boundaries has been determined by analysis of electron diffraction patterns.Dynamic recrystallization apparently proceeded by the following stages: 1) the formation of a well-ordered substructure from a more tangled, cell-like array, 2) increasing misorientation between subgrains, 3) rapid growth of subgrains at a misorientation between 3 and 5 to produce new "'grains" with straighter grain boundaries and lower internal dislocation densities and 4) continued deformation and rotation of the recrystallized grains with local grain-boundary migration to maintain relatively equiaxed shapes. The ultimate recrystallized structure in the narrow deformation zones consists of grains misoriented by between 5 and at least 30 , most of them containing a well-developed substructure.The combination of subgrain growth and rotation explains a number of features common to dynamically recrystallized minerals. The smaller subgrains present prior to growth and also within recrystallized grains form a population distinct from the larger subgrains and recrystallized grains ofapproximately equal size, which are those observed in an optical microscope. The smaller subgrains are visible only in TEM. Individual recrystallized grains may .remain through substantial straining, rotating in response to dislocation and sub-boundary motion within them, thus preserving and even enhancing the crystallographic fabric (texture). The retention of an initial recrystallized grain population throughout significant continuing deformation may explain the absence of strain softening in some recent experimental studies.

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“…7). For Yule marble, the laws for "T" orientation (unfavourable for twinning) were used aecording to the equations formulated by SCHMID et al (1979). There is a transition from an exponential flow law (low temperature plasticity, LTP) to power law creep (PLC) with a very high stress exponent (7.7) at a differential stress of 1.4 kbar.…”

Section: Relation Between Microstructure and Fabric Parameters; Infermentioning

confidence: 99%

Microstructure and fabric transitions in calcite tectonites from the Sierra Alhamilla (Spain)

Behrmann

1983

Geol Rundsch

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ZusammenfassungEine Anzahl yon Marmoren aus der Sierra Alhamilla (Spanien), intensiv deformiert unter natfidichen Bedingungen bei ca. 300 ~ C, zeigt ausgepr/igte Variationen in Mikrostruktur und Gefiige. Es kann gezeigt werden, dal3 die Entwicklung von bevorzugten Kristallorientierungen und Formanisotropien im Korngefiige erheblich yon der rekristallisierten KorngrSBe abh/ingt. Dies wird als Ausdruck der relativen Aktivit/it verschiedenet Deformationsmechanismen interpretiert. Superplastizit~it scheint eine relativ scharf definierte Obergrenze ffir Korugr6Ben yon 10---15/zm zu besitzen, hn Bereich des Potenzgesetz-Flief3ens wird die Verformung feinkSnriger Aggregate wahrseheinlich yon Diffusion, die yon grobkSrnigen yon Dislokationsmeehanismen bestimmt. Der 13bergangs-bereich zwischen beiden Mechanismen umfaBt einen KorngrSl3enunterschied yon etwa 80 #m. AbstractA suite of marble specimens from the Sierra Alhamilla (Spain), deformed to large strains under natural conditions at about 300 ~ C shows distinct variations in microstructnre and fabrics. It can be demonstrated that the development of crystallographic preferred orientations and grain shape fabrics are strongly dependent on recrystallized grain size. This is interpreted to reflect the relative importance of various deformational mechanisms. Superplasticity seems to have a sharp upper grain size limit at 10--15 #m. Within the power law creep regime, deformation in fine grained aggregates is probably dominated by diffusional, in coarser ones by dislocation mechanisms. The transition is a gradual one, and may span a grain size range of 30 #m.

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High temperature flow and dynamic recrystallization in carrara marble

Cited by 324 publications

References 16 publications

Strain localization during high temperature creep of marble: The effect of inclusions

Strain localization during high temperature creep of marble: The effect of inclusions

Dynamic Recrystallization in a Naturally Deformed Albite

Microstructure and fabric transitions in calcite tectonites from the Sierra Alhamilla (Spain)

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