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Elephant Mtn; 25. Basin City; 26. Martindale; 27. Goose Island; 28. Lower Monwnental; 29. Steens Mtn; 30. High-AI basalts of the Oregon Plateau; 31. Snake River Plain olivine tholeiites. Data from: Helmke and Haskin (1973). Swanson et al. (1979). Swanson and Wright (1981). Carlson et al. (1981). Leeman (1982). Carlson (1984). Hart (1984). Hart and Carlson (1986). McDougal (1976). Hooper et al. (1984). 3; Morris and Han, 1983). S. , 1984; Prestvik and Goles, 1985). This depletion is most obvious in the Grande Ronde, Wanapum, and some Saddle Mountains basalts and becomes more pronounced as the level of incompatible element enrichment increases.

The abrupt com~ositional changes between the many subgroups are typically accompanied by increases in 87 Sri 6Sr (Fig. 6) and in the LIL/HFS ratios. This suggests the formation of a new reservoir fed by magma from a source of different composition. As the variation between sources is best explained by variable proportions of a crustal component, then the most obvious model would include increasing contributions to the source from subducted crust. This type of contamination has been proposed by Carlson (1984) in explanation of the isotope data, but Carlson's model also includes a substantial degree of assimilation as the magma passes through the continental crust on the way to the surface.

Dike swarms for the individual basalt units are shown by the groups of parallel lines. The CJ swann corresponds to the location of feeder dikes for the Imnaha. Grande Ronde. and most Wanapum flows; the swann labeled PG is the Monument Valley swann supplying the Picture Gorge basalts; and the area labeled SM is the location of the Steens Mountain horst. Major structural features shown include the axis of the Blue Mountains anticline (BM) and the Olympic-Wallowa lineament (OWL). , Hooper, this volume).

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