Stability and P–V–T equation of state of KAlSi3O8-hollandite determined by in situ X-ray observations and implications for dynamics of subducted continental crust material

Nishiyama, Norimasa; Rapp, Robert P.; Irifune, Tetsuo; Sanehira, T.; Yamazaki, Daisuke; Funakoshi, K.

doi:10.1007/s00269-005-0037-y

Cited by 49 publications

(49 citation statements)

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“…Previous studies have generally reached good agreements on the phase relations of the composition KAlSi 3 O 8 up to the pressure of 128 GPa (Urakawa et al 1994;Yagi et al 1994;Tutti et al 2001;Akaogi et al 2004;Sueda et al 2004;Nishiyama et al 2005;Liu 2006;Ferroir et al 2006;Yong et al 2006;Liu and El Goresy 2007;Hirao et al 2008;Liu et al 2010). First, Or (KAlSi 3 O 8 ) breaks down to a three-phase assemblage (wadeitetype K 2 Si 4 O 9 + kyanite-type Al 2 SiO 5 + SiO 2 ) at around 6 GPa and 600-1400 °C.…”

Section: Introductionmentioning

confidence: 88%

“…Finally, Holl-II possibly remains thermodynamically stable up to 128 GPa. Mainly due to its unquenchable nature during decompression, Holl-II was difficult to detect within experimental products generated by traditional high-P quench methods, so that some discrepancy in the phase transition from Holl-I to Holl-II was reported (Tutti et al 2001;Sueda et al 2004;Nishiyama et al 2005;Ferroir et al 2006).…”

Section: Introductionmentioning

confidence: 97%

“…As demonstrated by some high-P experiments up to about 24 GPa (Irifune et al 1994), the proportion of its high-P form, mainly KAlSi 3 O 8 -hollandite, could volumetrically account for one third of the phase assemblages of the subducted upper continental crust composition, so that its importance in the geodynamic process in the deep interior of the Earth cannot be overestimated. Orthoclase (Or; KAlSi 3 O 8 ) is one of the major end-members in the feldspar family, and its high-P behavior is of great interest to many investigators (e.g., Yamada et al 1984;Zhang et al 1993;Urakawa et al 1994;Yagi et al 1994;Tutti et al 2001;Akaogi et al 2004;Sueda et al 2004;Nishiyama et al 2005;Liu 2006;Ferroir et al 2006;Yong et al 2006;Liu and El Goresy 2007;Hirao et al 2008;Liu et al 2009). …”

Section: Introductionmentioning

confidence: 99%

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A first-principles study of the phase transition from Holl-I to Holl-II in the composition KAlSi3O8

Deng

Liu

Hong

et al. 2011

American Mineralogist

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The phase relation and structural evolution of Holl-I and Holl-II in the composition KAlSi 3 O 8 at 0 K have been investigated by the first-principles method up to 130 GPa. Holl-I and Holl-II are polymorphs of KAlSi 3 O 8 stable at low pressures and high pressures, respectively. The transition pressure is determined at ∼23(5) GPa, in agreement with recent experimental observations. All experimentally observed major changes associated with this phase transition such as the deviation of the γ-angle from 90°, splitting of the a-and b-axes, as well as its P-V evolution, are successfully simulated. By evaluating the effect of different Al/Si substitution mechanisms on the computing cell of Holl-I, we have found: (1) different Al/Si substitution mechanisms do not result in apparent difference in the minimized cohesive energies, suggesting a possible random distribution of Al and Si; (2) different Al/ Si substitution mechanisms lead to different powder X-ray diffraction features, which, compared to the experimentally observed powder X-ray diffraction data, implies that local non-random distribution of Al and Si exists to some extent in the Holl-I structure; and (3) the phase transition from Holl-I to Holl-II might be associated with a change in the distribution pattern of Al and Si in the structure. From the simulated compression data, we have derived K 0 = 174 GPa and V 0 = 244.82 Å 3 for Holl-I, and K 0 = 168 GPa and V 0 = 244.8 Å 3 for Holl-II (K 0 ′ fixed at 4). The larger K 0 of Holl-I is probably related to the more stable squared open tunnel delimited by the rigid tetragonal octahedral framework, which is gradually deformed by compression in Holl-II after the phase transition from Holl-I to Holl-II.

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Section: Introductionmentioning

confidence: 88%

Section: Introductionmentioning

confidence: 97%

Section: Introductionmentioning

confidence: 99%

See 1 more Smart Citation

A first-principles study of the phase transition from Holl-I to Holl-II in the composition KAlSi3O8

Deng

Liu

Hong

et al. 2011

American Mineralogist

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“…hollandite, majorite, respectively) and carbon (e.g. Nishiyama et al, 2005, Tappert et al, 2005Wirth et al 2007) within the mantle transition zone as originally suggested by Ringwood (1967;, Anderson (1979), Nicolaysen (1985a;, Irufine and Ringwood (1993), and recently 'revived' (e.g. Shen and Blum, 2003;Blum and Shen, 2004;Tappert et al, 2005 a, b).…”

Section: Circum-gondwana Subduction Flanking Southern Africa During Gmentioning

confidence: 99%

The Kalahari Epeirogeny and climate change: differentiating cause and effect from core to space

Wit

2007

South African Journal of Geology

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Southern Africa's high Kalahari plateau and its flanking mountain ranges formed over an extended period of ~200 million years through vertical tectonic processes different from those at convergent plate boundaries. We refer to this as the Kalahari epeirogeny. Episodic uplift and erosion during the Kalahari epeirogeny is inferred from thermo-chronology and from stratigraphy of sediment accumulated around its continental margin. A total thickness of 2 to 7 km of rock (of which basalt was a major component) was eroded from the subcontinent's surface during two punctuated episodes of exhumation, in the early-Cretaceous and in the mid-Cretaceous. Major exhumation was over by the end of the Cretaceous, and the rate of erosion decreased by more than an order of magnitude to remove less than 1 km thickness of rock during the Cenozoic. Cosmogenic dating shows that erosion rates today are almost an order of magnitude less still.The cause for the Kalahari epeirogeny remains elusive, but three striking observations stand out: (i) major exhumation occurred during the late Mesozoic break-up of Gondwana; (ii) large scale basaltic magmatism closely match two accelerated episodes of exhumation: first along the west coast (~132 Ma, Etendeka large igneous province [LIP], associated with vast amounts of underplating along this entire passive margin), and the second flanking the sheared south coast margin (~90 Ma, Agulhas oceanic LIP). Yet exhumation that might have accompanied the vast Karoo LIP (~180 Ma) is not readily detected; (iii) the two main regional episodes of accelerated exhumation and coastal sediment accumulation are near synchronous with two regional 'spikes' of kimberlite intrusions: >450 kimberlites at ~90 Ma, and >200 kimberlites at ~120 Ma. Southern Africa is underlain by an anomalous warm region in the lowermost ~1500 km of the mantle that is linked to core to mantle heat loss. This warm region was inherited from a large Cretaceous thermo-chemical anomaly in the mantle created during long-lived subduction beneath Gondwana. Associated Mesozoic kimberlite genesis and basaltic magmatism may have been sufficient to cause volatile/heat-induced density changes in the lithospheric mantle of southern Africa to sustain the Kalahari plateau. In addition, such changes may have been induced by tectonic uplift and decompressional melting resulting from far-field collision processes between Africa and Europe, and/or final continental lithosphere decoupling between the Falkland plateau and southern Africa. CO 2 released into the ocean-atmosphere system during the Kalahari epeirogeny contributed to the global mid-Cretaceous hot-house conditions. However, because the CO 2 -consumption rate associated with basalt weathering is about eight times that of granite, atmospheric CO 2 was also efficiently sequestrated during the rapid erosion of Karoo basalt. Thus, the Kalahari epeirogeny also may have catalysed the onset of long-term global Cenozoic cooling.

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“…We use reported phase relations: jadeite ⇔ CF-type phase + stishovite (Kawai and Tsuchiya 2012a), grossular garnet ⇔ Cor + Ca-pv (Akaogi et al 2009;Kawai and Tsuchiya 2012b), stishovite ⇔ α-PbO 2 phase (Tsuchiya et al 2004), and K-hollandite I ⇔ II (Nishiyama et al 2005;Kawai and Tsuchiya 2012c). Since the high P-T dissociation boundary of grossular garnet and the phase transition boundary of K-hollandite have not been studied theoretically to date, we apply Clapeyron slopes determined experimentally (Akaogi et al 2009;Nishiyama et al 2005) to the static transition pressures obtained by theoretical studies Tsuchiya 2012b, 2013). They show that while the phase transition pressures of post-spinel, post-grossular, post-jadeite, and K-hollandite along a normal geotherm are 23.3, 23.6, 23.7, and 28.3 GPa, respectively, and those along a slab geotherm are 24.4, 23.6, 22.1, and 24.5 GPa, respectively ( Fig.…”

Section: Modeling Density and Seismic Velocity For Sediment And Averamentioning

confidence: 99%

Elasticity of Continental Crust Around the Mantle Transition Zone

Kawai

Tsuchiya

2015

The Earth's Heterogeneous Mantle

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The fate and amount of granitic materials subducted into the deep mantle are still under debate. The density, elastic property, and phase stability of granitic materials in the mantle pressures are key to clarifying them. Here, we modeled highpressure properties of the granitic assemblage by using ab initio mineral physics data of grossular garnet, K-hollandite, jadeite, stishovite, and calcium ferrite (CF)-type phase. We find that the ongoing subducting granitic assemblage, such as sediments and average upper crust rocks, is much denser than pyrolite in the pressure range from 9 GPa (~270 km), at which coesite undergoes a phase transition to stishovite, to around 27 GPa (~740 km). Above this pressure, granitic material becomes less dense than a pyrolite. This indicates that the granitic assemblage becomes gravitationally stable at the base of the mantle transition zone (MTZ). Results suggest a possibility that the granitic materials could accumulate around the 740 km depth if carried into the depth deeper than 270 km and segregated at some depth. Comparison of the velocities between granitic and pyrolitic materials shows that granitic materials can produce substantial velocity anomalies in the MTZ and the uppermost lower mantle (LM). Seismic observations such as anomalously fast velocities, especially for the shear wave, around the 660-km discontinuity, the complexity of 660-km discontinuity, and the scatterers in the uppermost LM could be associated with the subducted granitic materials.

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Stability and P–V–T equation of state of KAlSi3O8-hollandite determined by in situ X-ray observations and implications for dynamics of subducted continental crust material

Cited by 49 publications

References 31 publications

A first-principles study of the phase transition from Holl-I to Holl-II in the composition KAlSi3O8

A first-principles study of the phase transition from Holl-I to Holl-II in the composition KAlSi3O8

The Kalahari Epeirogeny and climate change: differentiating cause and effect from core to space

Elasticity of Continental Crust Around the Mantle Transition Zone

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