{"@context":{"@vocab":"https://cir.nii.ac.jp/schema/1.0/","rdfs":"http://www.w3.org/2000/01/rdf-schema#","dc":"http://purl.org/dc/elements/1.1/","dcterms":"http://purl.org/dc/terms/","foaf":"http://xmlns.com/foaf/0.1/","prism":"http://prismstandard.org/namespaces/basic/2.0/","cinii":"http://ci.nii.ac.jp/ns/1.0/","datacite":"https://schema.datacite.org/meta/kernel-4/","ndl":"http://ndl.go.jp/dcndl/terms/","jpcoar":"https://github.com/JPCOAR/schema/blob/master/2.0/"},"@id":"https://cir.nii.ac.jp/crid/1362262945426730624.json","@type":"Article","productIdentifier":[{"identifier":{"@type":"DOI","@value":"10.1029/91jb01204"}},{"identifier":{"@type":"URI","@value":"https://api.wiley.com/onlinelibrary/tdm/v1/articles/10.1029%2F91JB01204"}},{"identifier":{"@type":"URI","@value":"https://agupubs.onlinelibrary.wiley.com/doi/pdf/10.1029/91JB01204"}}],"dc:title":[{"@value":"The equation of state of a molten komatiite: 1 Shock wave compression to 36 GPa"}],"description":[{"type":"abstract","notation":[{"@value":"<jats:p>The equation of state (EOS) of an initially molten (1550°C) komatiite (27 wt % MgO) was determined in the 5–36 GPa pressure range via shock wave compression. Shock wave velocity<jats:italic>U<jats:sub>s</jats:sub></jats:italic>and particle velocity<jats:italic>U<jats:sub>p</jats:sub></jats:italic>(kilometers/second) follow the linear relationship<jats:italic>U<jats:sub>s</jats:sub></jats:italic>= 3.13(±0.03) + 1.47(±0.03)<jats:italic>U<jats:sub>p</jats:sub></jats:italic>. Based on a calculated density at 1550°C, 0 bar of 2.745±0.005 g/cm<jats:sup>3</jats:sup>, this<jats:italic>U<jats:sub>s</jats:sub></jats:italic>‐<jats:italic>U<jats:sub>p</jats:sub></jats:italic>relationship gives the isentropic bulk modulus<jats:italic>K<jats:sub>S</jats:sub></jats:italic>= 27.0 ± 0.6 GPa, and its first and second isentropic pressure derivatives,<jats:italic>K</jats:italic>′<jats:sub>S</jats:sub>= 4.9 ±0.1 and<jats:italic>K</jats:italic>″<jats:sub>S</jats:sub>= −0.109 ± 0.003 GPa<jats:sup>−1</jats:sup>. The calculated liquidus compression curve agrees within error with the static compression results of Agee and Walker (1988) to 6 GPa but is less dense than their extrapolated values at higher pressures. We determine that olivine (Fo<jats:sub>94</jats:sub>) will be neutrally buoyant in komatiitic melt of the composition that we studied near 8.2 GPa. Clinopyroxene would also be neutrally buoyant near this pressure. Liquidus garnet‐majorite may be less dense than this komatiitic liquid in the 20–24 GPa interval; however, pyropic‐garnet and perovskite phases are denser than this komatiitic liquid in their respective liquidus pressure intervals to 36 GPa. Liquidus perovskite may be neutrally buoyant near 70 GPa. At 40 GPa, the density of shock‐compressed molten komatiite would be approximately equal to the calculated density of an equivalent mixture of dense solid oxide components. This observation supports the model of Rigden et al. (1989) for compressibilities of liquid oxide components. Using their theoretical EOS for liquid forsterite and fayalite, we calculate the densities of a spectrum of melts from basaltic through peridotitic that are related to the experimentally studied komatiitic liquid by addition or subtraction of olivine. At low pressure, olivine fractionation lowers the density of basic magmas, but above 13–14 GPa this trend is reversed. All of these basic to ultrabasic liquids are predicted to have similar densities at 13–14 GPa, and this density is approximately equal to the density of the bulk (preliminary reference Earth model) mantle in this pressure range. This suggests that melts derived from a peridotitic mantle may be inhibited from ascending from depths greater than 400 km.</jats:p>"}]}],"creator":[{"@id":"https://cir.nii.ac.jp/crid/1382262945426730626","@type":"Researcher","foaf:name":[{"@value":"Gregory H. Miller"}]},{"@id":"https://cir.nii.ac.jp/crid/1382262945426730624","@type":"Researcher","foaf:name":[{"@value":"Edward M. Stolper"}]},{"@id":"https://cir.nii.ac.jp/crid/1382262945426730625","@type":"Researcher","foaf:name":[{"@value":"Thomas J. Ahrens"}]}],"publication":{"publicationIdentifier":[{"@type":"PISSN","@value":"01480227"},{"@type":"PISSN","@value":"http://id.crossref.org/issn/01480227"}],"prism:publicationName":[{"@value":"Journal of Geophysical Research: Solid Earth"}],"dc:publisher":[{"@value":"American Geophysical Union (AGU)"}],"prism:publicationDate":"1991-07-10","prism:volume":"96","prism:number":"B7","prism:startingPage":"11831","prism:endingPage":"11848"},"reviewed":"false","dc:rights":["http://onlinelibrary.wiley.com/termsAndConditions#vor"],"url":[{"@id":"https://api.wiley.com/onlinelibrary/tdm/v1/articles/10.1029%2F91JB01204"},{"@id":"https://agupubs.onlinelibrary.wiley.com/doi/pdf/10.1029/91JB01204"}],"createdAt":"2008-02-06","modifiedAt":"2024-02-22","relatedProduct":[{"@id":"https://cir.nii.ac.jp/crid/1360004229800540160","@type":"Article","resourceType":"学術雑誌論文(journal article)","relationType":["isReferencedBy"],"jpcoar:relatedTitle":[{"@value":"Equation of state for silicate melts: A comparison between static and shock compression"}]},{"@id":"https://cir.nii.ac.jp/crid/1360017282443923328","@type":"Article","resourceType":"学術雑誌論文(journal article)","relationType":["isReferencedBy"],"jpcoar:relatedTitle":[{"@value":"Hadean mantle oxidation inferred from melting of peridotite under lower-mantle conditions"}]},{"@id":"https://cir.nii.ac.jp/crid/1360285706175326976","@type":"Article","resourceType":"学術雑誌論文(journal article)","relationType":["isReferencedBy"],"jpcoar:relatedTitle":[{"@value":"Equation of state of silicate melts with densified intermediate-range order at the pressure condition of the Earth’s deep upper mantle"}]},{"@id":"https://cir.nii.ac.jp/crid/1360848657065301760","@type":"Article","resourceType":"学術雑誌論文(journal article)","relationType":["isReferencedBy"],"jpcoar:relatedTitle":[{"@value":"Density contrast between silicate melts and crystals in the deep mantle: An integrated view based on static-compression data"}]},{"@id":"https://cir.nii.ac.jp/crid/1390001204381615488","@type":"Article","resourceType":"学術雑誌論文(journal article)","relationType":["isReferencedBy"],"jpcoar:relatedTitle":[{"@language":"en","@value":"Melting Relations and Equation of State of Magmas at High Pressure: Applications to Geodynamics"},{"@language":"ja","@value":"マントル物質の融解とマグマの密度　：　そのマントルダイナミクスへの適用"},{"@value":"Bowen賞受賞記念 マントル物質の融解とマグマの密度--そのマントルダイナミクスへの適用"},{"@language":"ja-Kana","@value":"Bowenショウ ジュショウ キネン マントル ブッシツ ノ ユウカイ ト マグマ ノ ミツド ソノ マントル ダイナミクス エノ テキヨウ"}]},{"@id":"https://cir.nii.ac.jp/crid/2051996266990517248","@type":"Article","resourceType":"学術雑誌論文(journal article)","relationType":["isReferencedBy"],"jpcoar:relatedTitle":[{"@value":"Experimental simulations of shock textures in BCC iron : implications for iron meteorites"}]}],"dataSourceIdentifier":[{"@type":"CROSSREF","@value":"10.1029/91jb01204"},{"@type":"CROSSREF","@value":"10.1002/2013gl058328_references_DOI_Is0jRNrj7B429rCWcsTbFjiei36"},{"@type":"CROSSREF","@value":"10.1038/s41561-023-01169-4_references_DOI_Is0jRNrj7B429rCWcsTbFjiei36"},{"@type":"CROSSREF","@value":"10.1007/s00269-013-0571-y_references_DOI_Is0jRNrj7B429rCWcsTbFjiei36"},{"@type":"CROSSREF","@value":"10.4131/jshpreview.18.360_references_DOI_Is0jRNrj7B429rCWcsTbFjiei36"},{"@type":"CROSSREF","@value":"10.1186/s40645-022-00482-7_references_DOI_Is0jRNrj7B429rCWcsTbFjiei36"},{"@type":"CROSSREF","@value":"10.1016/j.epsl.2010.04.021_references_DOI_Is0jRNrj7B429rCWcsTbFjiei36"}]}