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where I•=•/Vol2/2•:. Repeating he xample in the appendix; i.e., where/•=5 km,/2=5 km V0=7 cm/yr, T•=I.0, To=0.0, and •:= 10 -6 m 2 s 'z, we find that Tin=0.73. This shows that such a high velocity impinging on a stationary region can lead to high temperatures at the interface. In contrast, the mantle flow in a subduction zone impinges on a moving slab; it is the downward advection of cold lithosphere by the subducting slab that is critical in reducing the interface temperatue in this region. The above error does not affect any of the results or conclusions in the body of the paper, since the body of the paper is independent of Appendix A. In section A.2 of Appendix A, the axis convention should read "the x axis is perpendicular to the slab (negative out into the wedge)". Figure 7c has a younger oceanic plate than Figure 7d, so it is not strictly an enlargement of Figure 7d, as stated in the figure caption. The temperatures in the regions of interest, the slabwedge interface and the mantle wedge, are virtually unaffected by the age of the subducting plate as stated in the paper. The temperature of the subducting plate though does depend upon its age, but since the temperatures in the slab were subsolidus, their exact values had no bearing on the discussion of magmatism and the conclusions. We would like to acknowledge K. Bose, who pointed out the convention error in Appendix A.2 and the error in the figure caption of Figure 7.