Erratum

Abstract

Journal of Metamorphic GeologyVolume 21, Issue 9 p. 935-935 Free Access Erratum First published: 02 December 2003 https://doi.org/10.1046/j.1525-1314.2003.00494.xAboutSectionsPDF ToolsRequest permissionExport citationAdd to favoritesTrack citation ShareShare Give accessShare full text accessShare full-text accessPlease review our Terms and Conditions of Use and check box below to share full-text version of article.I have read and accept the Wiley Online Library Terms and Conditions of UseShareable LinkUse the link below to share a full-text version of this article with your friends and colleagues. Learn more.Copy URL Share a linkShare onFacebookTwitterLinked InRedditWechat Schlieren formation in diatexite migmatite: examples from the St Malo migmatite terrane, France, I. Milord and E. W. Sawyer. Journal of Metamorphic Geology, 21, 347362 Figure 9 of this paper was printed incorrectly. The arrow pointing at the upper panels (a)–(c) should read ‘plagioclase enrichment’. The arrow pointing at the lower panels (d)–(f) should read ‘biotite enrichment’. The panels were also rotated clockwise by 90°. The correct version is printed below. Figure 9Open in figure viewerPowerPoint Schematic model showing the development of schlieren in a diatexite magma that initially contains crystals of residual plagioclase and biotite. The relative sizes of plagioclase and biotite crystals are not drawn to scale for purposes of diagram clarity. Large blocky plagioclase crystals 2–6 (mm) are separated from smaller biotite grains (< 0.5–0.8 mm) during flow, the plagioclase-rich parts become the host (a to c) and the biotite-rich parts become the schlieren (d to f). (a) Stage with a small proportion of plagioclase crystals accumulated, although an SPO develops few grain interactions occur. (b) As more residual crystals are collected and crystallization of plagioclase advances, the crystal/melt ratio rises and more grain tiling occurs for plagioclase and for biotite (making the biotite clumps). (c) Sufficient plagioclase has been accumulated (both residual and magmatic crystals) that the host has reached the rigid percolation threshold (time t1) and quartz, biotite and plagioclase start to crystallize in the plagioclase framework. In the biotite-rich parts (d) the crystal/melt ratio rises slowly and an SPO develops but particle collisions are few. (e) As the number of particle interactions increases imbricate clumps and aggregates of biotite are formed, and eventually, as more melt is crystallized and melt begins to be expelled, the crystal/melt ratio passes the rigid percolation threshold at time t2. (f) Continued shearing of the biotite-rich domains between the more rigid, feldspar-rich domains causes loss of melt in the biotite schlieren and enables the particle locking threshold to be reached there and intracrystalline deformation of the biotite to occur. Reference Milord, I., Sawyer, E.W., 2003. Schlieren formation in diatexite migmatite: examples from the St Malo Migmatite terrane, France. Journal of Metamorphic Geology, 21, 347 – 362. Wiley Online LibraryCASWeb of Science®Google Scholar Volume21, Issue9December 2003Pages 935-935 FiguresReferencesRelatedInformation