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Oregon_PT_Table_1_010213.xlsxExcel 2007 spreadsheet75KPrimitive basalt sample compositions, their calculated depths, and temperatures of last equilibration with the mantle and original reference information. Sample compositions from Diamond Crater [Till et al., 2012], some of those from Jordan Valley Volcanic Field [Shoemaker and Hart, 2002; Bondre, 2006], some from the High Cascades region [Schmidt et al., 2008], Crater Lake Volcanic Center [Bacon, 1990; Bacon et al., 1997], Mt. Bailey volcano [Barnes, 1992], Mt. Shasta volcano [Baker et al., 1994; Elkins-Tanton et al., 2001], Medicine Lake volcano [Baker et al., 1991; Bacon et al., 1997; Elkins-Tanton et al., 2001; Donnelly-Nolan et al., 2008; Donnelly-Nolan, 2010], and Lassen Volcanic Field [Bacon et al., 1997] have been previously published. The remaining major element compositions were measured by techniques indicated by reference number. Sample references in the table are as follows: [1a] WK Hart, unpublished data, analyzed by XRF at Franklin and Marshall College, [1b] WK Hart, unpublished data, analyzed by Direct Current Argon Plasma Atomic Emission Spectrometry (DCP-AES) at Miami University, Ohio, [2] RW Carlson, unpublished data, analyzed by XRF at Washington State University, [3] JM Donnelly-Nolan, unpublished data, analyzed by XRF at Washington State University, [4] Schmidt et al., 2008, [5] Barnes, 1992, [6] Bacon et al., 1997, [7] Elkins-Tanton et al., 2001, [8] Till et al., 2012, [9] Shoemaker and Hart, 2002, [10] Bondre, 2006, and [11] Baker et al., 1994. Samples analyzed by X-ray Fluorescence at Washington State University GeoAnalytical Lab and at Franklin and Marshall College followed techniques detailed at by Johnson et al. [1999] and Mertzman [2000] respectively, and samples analyzed by DCP-AES at Miami University followed the procedures outlined in Katoh et al. [1999]. Note that the totals listed are the original analytical totals reflecting a variety of types of reported Fe concentrations (e.g., total as Fe2+, total as Fe3+, and Fe2+ by titration) and that all samples are reported here with total Fe expressed as FeO. The pressure and temperature of melt segregation were calculated using the thermometer and barometer of Till et al. [2012]. The temperature and pressure estimates for the 33 CAB samples in italics were corrected for the effect of H2O as described in the text. Sample pressures were converted to depth using crustal density profiles from regional seismic refraction experiments [Zucca et al., 1986; Cox, 2011].
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