Adding volatiles: Convergent plate boundaries (arc lavas, continental margins,

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1 Melting of the mantle Increasing temperature: Intraplate igneous activity (OIB, continental basalts etc.) Decreasing pressure: Divergent plate boundaries (MORBs, rifts, back-arc basins etc.) Adding volatiles: Convergent plate boundaries (arc lavas, continental margins, etc.)

2 Plate Tectonic - Igneous Genesis 1. Mid-Ocean Ridges 5. Back-Arc Basins 2. Intracontinental Rifts 3. Island Arcs 4. Active Continental Margins 6. Ocean Island Basalts 7. Miscellaneous Intra- Continental t Activity it kimberlites, carbonatites, anorthosites...

3 Ocean-ocean Island Arc (IA) Ocean-continent Continental Arc or Active Continental lmargin (ACM) Figure Principal subduction zones associated with orogenic volcanism and plutonism. Triangles are on the overriding plate. PBS = Papuan-Bismarck-Solomon-New Hebrides arc. After Wilson (1989) Igneous Petrogenesis, Allen Unwin/Kluwer.

4 Structure of an Island Arc Figure Schematic cross section through a typical island arc after Gill (1981), Orogenic Andesites and Plate Tectonics. Springer-Verlag. HFU= heat flow unit (4.2 x 10-6 joules/cm 2 /sec)

5 Volcanic Rocks of Island Arcs Complex tectonic situation i and dbroad spectrum of volcanic products High proportion of fbasaltic andesite and andesite Most andesites occur in subduction zone settings Table Relative Proportions of Analyzed Island Arc Volcanic Rock Types Locality B B-A A D R Mt. Misery, Antilles (lavas) Ave. Antilles 2 17 ( 42 ) 39 2 Lesser Antilles ( 3 ) Nicaragua/NW Costa Rica W Panama/SE Costa Rica Aleutians E of Adak Aleutians, Adak & W Little Sitkin Island, Aleutians Ave. Japan (lava, ash falls) 2 14 ( 85 ) 2 0 Isu-Bonin/Mariana < 1 Kuriles < 1 Talasea, Papua Scotia from Kelemen (2003a and personal comunication). 2 after Gill (1981, Table 4.4) B = basalt B-A = basaltic andesite A = andesite, D = dacite, R = rhyolite Basalts are still very common and important!

6 Classification of Igneous Rocks Figure 2.3. A classification and nomenclature of volcanic rocks. After IUGS. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

7 Island Arc Petrogenesis Figure A proposed model for subduction zone magmatism with particular reference to island arcs. Dehydration of slab crust causes hydration of the mantle (violet), (ilt) which hih undergoes partial melting as amphibole (A) and phlogopite (B) dehydrate. From Tatsumi (1989), J. Geophys. Res., 94, and Tatsumi and Eggins (1995). Subduction Zone Magmatism. Blackwell. Oxford.

8 Island Arc Petrogenesis Altered oceanic crust begins to dehydrate at depths ~ 50 km or less, as chlorite, phengite, and other hydrous phyllosilicates decompose. Further dehydration takes place at greater depths as other hydrous phases become unstable, including amphibole at about 3 GPa. The slab crust is successively converted to blueschist, amphibolite, and finally anhydrous eclogite as it reaches about km depth. In most (mature) arcs, the temperature in the subducted crust is below the wet solidus for basalt, so the released water cannot cause melting, and most of the water is believed to rise into the overlying mantle wedge, where it reacts with the lherzolite to form a pargasitic amphibole and probably phlogopite (yellowish area) Slightly hydrous mantle immediately above the slab is carried downward by induced convective flow where it heats up, dehydrates, and melts at A (120 km) Fractional crystallization happens in the arc crust

9 Continental Arc Magmatism Figure Schematic diagram to illustrate how a shallow dip of the subducting slab can pinch out the asthenosphere from the overlying mantle wedge. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.

10 Continental Arc Magmatism Potential differences with respect to Island Arcs: Thick sialic crust contrasts greatly with mantle- derived partial melts more pronounced effects of contamination Low density of crust may retard ascent stagnation of magmas and more potential for differentiation Low melting point of crust allows for partial melting gp p g and crust-derived melts

11 Continental Arc Petrogenesis Figure Schematic cross section of an active continental margin subduction zone, showing the dehydration of the subducting slab, hydration and melting of a heterogeneous mantle wedge (including enriched sub-continental lithospheric mantle), crustal underplating of mantle-derived melts where MASH processes may occur, as well as crystallization of the underplates. Remelting of the underplate to produce tonalitic magmas and a possible zone of crustal anatexis is also shown. As magmas pass through the continental crust they may differentiate further and/or assimilate continental crust. Winter (2001) An Introduction to Igneous and Metamorphic Petrology.

12 Chapter 17: Continental Arc Magmatism Figure Pressure-temperature phase diagram showing the solidus curves for H 2 O-saturated and dry granite. An H 2 O-saturated granitoid just above the solidus at A will quickly intersect the solidus as it rises and will therefore solidify. A hotter, H 2 O-undersaturated granitoid at B will rise further before solidifying. Note: the pressure axis is inverted to strengthen the analogy with the Earth, so a negative dp/dt Clapeyron slope will appear positive. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice

13 Overall Conclusions and Andesite Petrogenetic Model: I Strong link between convergent plate boundaries and Calc- alkaline volcanism (and associated intrusives). Andesite is the dominant rock type found in most island arcs; more common in older, more mature arcs, such as Japan; while basalts and basaltic-andesite are more common on younger, less mature arcs, such as the Marianas. Volcanism is commonly aligned along a front that is between 100 to 200 km above the top of the subducting slab.

14 Overall Conclusions and Andesite Petrogenetic Model: II Most island arc lavas are extremely phenocryst rich; their bulk composition then do not likely represent true liquid compositions. Smooth Harker diagrams for all major elements. Implies common liquid-line of descent driven by fractional crystallization of SiO 2-poor and FeO-rich such as Ti- magnetite and amphibole. Sr-enrichment from seawater alteration of hydrated Sr-enrichment from seawater alteration of hydrated basaltic oceanic crust and Pb-enrichment from terrigenous sediments (1-3%).

15 Overall Conclusions and Andesite Petrogenetic Model: III Volatiles l from descending di slab are liberated into overlying mantle wedge. Initiates partial melting yielding water-bearing basalts. Basalts are enriched in the subduction component (LIL and LREE, Sr, Pb enriched). The basalts transit mantle wedge and in older arcs likely pond at MOHO, where they may melt the lower crust and differentiate by fractional crystallization. More evolved magmas (lower density) rise into mid-crust and periodically erupt. Some evidence for repeated basalt injections into midcrustal storage zones in the form of zoned crystals, variable Fe-Ti oxide-derived temperatures, and textures of mafic inclusions.

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