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The data suggest that the order of trace-element incompatibility in oceanic basalts is Cs \u2248 Rb \u2248 (\u2248 Tl) \u2248 Ba(\u2248 W) > Th > U \u2248 Nb = Ta \u2248 K > La > Ce \u2248 Pb > Pr (\u2248 Mo) \u2248 Sr > P \u2248 Nd (> F) > Zr = Hf \u2248 Sm > Eu \u2248 Sn (\u2248 Sb) \u2248 Ti > Dy \u2248 (Li) > Ho = Y > Yb. This rule works in general and suggests that the overall fractionation processes operating during magma generation and evolution are relatively simple, involving no significant change in the environment of formation for MORBs and OIBs.<\/jats:p>\n \n In detail, minor differences in element ratios correlate with the isotopic characteristics of different types of OIB components (HIMU, EM, MORB). These systematics are interpreted in terms of partial-melting conditions, variations in residual mineralogy, involvement of subducted sediment, recycling of oceanic lithosphere and processes within the low velocity zone. Niobium data indicate that the mantle sources of MORB and OIB are not exact complementary reservoirs to the continental crust. Subduction of oceanic crust or separation of refractory eclogite material from the former oceanic crust into the lower mantle appears to be required. The negative europium anomalies observed in some EM-type OIBs and the systematics of their key element ratios suggest the addition of a small amount (\u2a7d1% or less) of subducted sediment to their mantle sources. However, a general lack of a crustal signature in OIBs indicates that sediment recycling has not been an important process in the convecting mantle, at least not in more recent times (\u2a7d2 Ga). Upward migration of silica-undersaturated melts from the low velocity zone can generate an enriched reservoir in the continental and oceanic lithospheric mantle. We propose that the HIMU type (\n eg<\/jats:italic>\n St Helena) OIB component can be generated in this way. 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