Shock metamorphism of ordinary chondrites

Stöffler, D.; Keil, K.; Edward, Scott

doi:10.1016/0016-7037(91)90078-j

Cited by 1,128 publications

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“…A few melt pockets had also observed in the samples (Figure 3). The formation of the melt pockets is not related an equilibrium shock pressure and temperature experienced by whole rock, and it should be attributed to localized spikes of pressure and temperature appearing in shocked polycrystalline rocks [29,30].…”

Section: Discussionmentioning

confidence: 91%

“…This shock pressure range could correspond to a post-shock temperature range from 300 to 900°C for crystalline quartzo-feldspathic rocks [24]. The shock heating is related to the adiabatic decompression of shocked rocks [29]. A few melt pockets had also observed in the samples (Figure 3).…”

Section: Discussionmentioning

confidence: 99%

“…Shock wave propagating throughout grain boundaries of polycrystalline rocks can causes reflection and refraction and localized stress and temperature concentration at the interfaces [29]. As enough pulses are applied, rutile experiences detachments of clasts.…”

Section: Discussionmentioning

confidence: 99%

“…It is well accepted that some shock-produced high-pressure minerals are formed during decompression, for instance, coesite [29], which is obviously correlated to shock heating. A recent investigation in the shocked gneiss from the Xiuyan crater revealed the fact that dendritic coesite crystallizes from shock-produced silica melt in a pressure range from 2.5 to 13 GPa [19].…”

Section: Discussionmentioning

confidence: 99%

“…A recent investigation in the shocked gneiss from the Xiuyan crater revealed the fact that dendritic coesite crystallizes from shock-produced silica melt in a pressure range from 2.5 to 13 GPa [19]. The shock-melting of quartz requires a peak shock pressure up to 50 GPa [24,29]. The crystallization of coesite from shock-produced silica melt provides important evidence that high-pressure mineral was formed during decompression with elevated temperature.…”

Section: Discussionmentioning

confidence: 99%

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High-pressure polymorph of TiO2-II from the Xiuyan crater of China

Chen

Xie

et al. 2013

Chin. Sci. Bull.

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Abundant TiO 2 -II, a high-pressure polymorph of titanium dioxide, was found in the gneiss fragments of impact-produced breccias from the Xiuyan crater. Rutile in the gneiss was severely fragmented and fine-grained clasts less than 2 m in size had been transformed to TiO 2 -II. Irregular thin layered TiO 2 -II is also observed in coarse-grained rutile fragments, where the TiO 2 -II layers distributes along fractures and cracks in rutile. About 30 percent of rutile in the gneiss had been transformed to TiO 2 -II. Fine grains of TiO 2 -II display light bluish grey to light yellow brown in plane-polarized reflected light. Crystallographic investigation shows that TiO 2 -II has an orthorhombic structure with space group Pbcn. The cell parameters are a=4.543(1) Å, b=5.491(9) Å and c=4.895(2) Å. Its empirical formula calculated on the basis of two oxygen atoms can be written as (Ti 0.985 Fe 0.008 Nb 0.006 -Si 0.003 Zr 0.001 ) 1.003 O 2 , or simply formula TiO 2 . According to the shock effects of quartz and feldspars, the peak shock pressure and post-shock temperature in the TiO 2 -II-bearing gneiss are estimated to be between 35 and 43 GPa and 300-900°C, respectively. The finding of TiO 2 -II in the shock-metamorphosed gneiss provides another mineral physics evidence for shock origin of the Xiuyan crater. Rutile, a titanium dioxide, is a common accessory mineral in various types of rocks. At high pressure, rutile can be transformed into high-pressure polymorphs of TiO 2 -II (-PbO 2 ), baddeleyite, orthorhombic I and cotunnite phases with increasing pressure [1]. High-pressure polymorphs of baddeleyite, orthorhombic-I and cotunnite-type TiO 2 reverse to TiO 2 -II on decompression. TiO 2 -II is the only highpressure polymorph that can be recovered experimentally at ambient conditions [2]. i  - had been firstly synthesized by static compression experiment [3]. A number of static compression experiments succeed in the transition of rutile to TiO 2 -II at pressure range between 4 and 12 GPa and temperature between 400 and 1500°C [3][4][5][6][7]. Shock-loading experiments revealed that rutile transforms to i  - at peak shock pressure from 20 to 100 GPa [8][9][10]. The formation of natural TiO 2 -II could be related to highpressure endogenic geological processes or bolide impact events. Occurrence of natural TiO 2 -II had been previously reported in ultrahigh-pressure metamorphic rocks [11,12], mantle-derived rocks [13], terrestrial impact structures [14][15][16], and tektite [17]. However, the mineralogical features and the formation conditions of natural TiO 2 -II still needs to be further investigated because of the very limited material that had been found.The Xiuyan crater is a recently confirmed impact structure in China. The target rocks of the crater were shock-metamorphosed, from which impact-produced breccia, coesite, planar deformation features in quartz have been identified [18][19][20]. In this paper, we report the occurrence and mineralogical features of TiO 2 -IIin the impact-produced breccias

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Section: Discussionmentioning

confidence: 91%

Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

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High-pressure polymorph of TiO2-II from the Xiuyan crater of China

Chen

Xie

et al. 2013

Chin. Sci. Bull.

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Maskelynite formation via solid‐state transformation: Evidence of infrared and X‐ray anisotropy

et al. 2015

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We present the results of a combined study of shocked labradorite from the Lonar crater, India, using optical microscopy, micro-Raman spectroscopy, nuclear magnetic resonance (NMR) spectroscopy, high-energy X-ray total scattering experiments, and micro-Fourier transform infrared (micro-FTIR) spectroscopy. We show that maskelynite of shock class 2 is structurally more similar to fused glass than to crystalline plagioclase. However, there are slight but significant differences-preservation of original preimpact igneous zoning, anisotropy at infrared wavelengths, X-ray anisotropy, and preservation of some intermediate range order-which are all consistent with a solid-state transformation from plagioclase to maskelynite.

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The effect of hydrostatic pressure up to 1.61 GPa on the Morin transition of hematite‐bearing rocks: Implications for planetary crustal magnetization

Bezaeva

Demory

Rochette

et al. 2015

Geophysical Research Letters

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We present new experimental data on the dependence of the Morin transition temperature (TM) on hydrostatic pressure up to 1.61 GPa, obtained on a well‐characterized multidomain hematite‐bearing sample from a banded iron formation. We used a nonmagnetic high‐pressure cell for pressure application and a Superconducting Quantum Interference Device magnetometer to measure the isothermal remanent magnetization (IRM) under pressure on warming from 243 K to room temperature (T0). IRM imparted at T0 under pressure in 270 mT magnetic field (IRM270mT) is not recovered after a cooling‐warming cycle. Memory effect under pressure was quantified as IRM recovery decrease of 10%/GPa. TM, determined on warming, reaches T0 under hydrostatic pressure 1.38–1.61 GPa. The pressure dependence of TM up to 1.61 GPa is positive and essentially linear with a slope dTM/dP = (25 ± 2) K/GPa. This estimate is more precise than previous ones and allows quantifying the effect of a pressure wave on the upper crust magnetization, with special emphasis on Mars.

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Shock metamorphism of ordinary chondrites

Cited by 1,128 publications

References 51 publications

High-pressure polymorph of TiO2-II from the Xiuyan crater of China

High-pressure polymorph of TiO2-II from the Xiuyan crater of China

Maskelynite formation via solid‐state transformation: Evidence of infrared and X‐ray anisotropy

The effect of hydrostatic pressure up to 1.61 GPa on the Morin transition of hematite‐bearing rocks: Implications for planetary crustal magnetization

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