Arc Magmatism Reading Winter Chapter 16 Island Arc

Arc Magmatism Reading: Winter, Chapter 16

Island Arc Magmatism • Activity along arcuate volcanic island chains along subduction zones • Distinctly different from the mainly basaltic provinces – Composition more diverse and silicic – Basalt generally occurs in subordinate quantities – More explosive than the quiescent basalts – Strato-volcanoes are the most common volcanic landform

• Igneous activity is related to convergent plate situations that result in the subduction of one plate beneath another • The initial petrologic model: – Oceanic crust is partially melted – Melts rise through the overriding plate to form volcanoes just behind the leading plate edge – Unlimited supply of oceanic crust to melt

Ocean-ocean Island Arc (IA) Ocean-continent Continental Arc or Active Continental Margin (ACM) Figure 16 -1. Principal subduction zones associated with orogenic volcanism and plutonism. Triangles are on the overriding plate. PBS = Papuan-Bismarck-Solomon-New Hebrides arc. SAfter Wilson (1989) Igneous Petrogenesis, Allen Unwin/Kluwer.

Subduction Products • Characteristic igneous associations • Distinctive patterns of metamorphism • Orogeny and mountain belts

Structure of an Island Arc Figure 16 -2. 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)

Volcanic Rocks of Island Arcs • Complex tectonic situation and broad spectrum • High proportion of basaltic andesite – Most andesites occur in subduction zone settings

Major Elements and Magma Series • Tholeiitic (MORB, OIT) • Alkaline (OIA) • Calc-Alkaline (~ restricted to SZ)

Major Elements and Magma Series a. Alkali vs. silica b. AFM c. Fe. O*/Mg. O vs. silica diagrams for 1946 analyses from ~ 30 island continental arcs with emphasis on the more primitive volcanics Figure 16 -3. Data compiled by Terry Plank (Plank and Langmuir, 1988) Earth Planet. Sci. Lett. , 90, 349 -370.

Sub-series of Calc-Alkaline • K 2 O is an important discriminator 3 sub-series The three andesite series of Gill (1981) Orogenic Andesites and Plate Tectonics. Springer-Verlag. Contours represent the concentration of 2500 analyses of andesites stored in the large data file RKOC 76 (Carnegie Institute of Washington).

K 2 O-Si. O 2 diagram distinguishing high-K, medium-K and low-K series. Large squares = high-K, stars = med. -K, diamonds = low-K series from Table 16 -2. Smaller symbols are identified in the caption. Differentiation within a series (presumably dominated by fractional crystallization) is indicated by the arrow. Different primary magmas (to the left) are distinguished by vertical variations in K 2 O at low Si. O 2. After Gill, 1981, Orogenic Andesites and Plate Tectonics. Springer-Verlag.

AFM diagram distinguishing tholeiitic and calc-alkaline series. Arrows represent differentiation trends within a series.

Fe. O*/Mg. O vs. Si. O 2 diagram distinguishing tholeiitic and calc-alkaline series.

From Winter (2001)

Fe. O*/Mg. O vs. Si. O 2 diagram distinguishing tholeiitic and calc-alkaline series.

Fe. O*/Mg. O vs. Si. O 2 diagram distinguishing tholeiitic and calc-alkaline series.

Tholeiitic vs. Calc-alkaline From Winter (2001)

Tholeiitic vs. Calc-alkaline Tholeiitic silica in the Skaergård Intrusion No change C-A shows continually increasing Si. O 2 and lacks dramatic Fe enrichment

Calc-alkaline differentiation – Early crystallization of an Fe-Ti oxide phase Probably related to the high water content of calc-alkaline magmas in arcs, dissolves high f. O 2 – High water pressure also depresses the plagioclase liquidus and more An-rich – As hydrous magma rises, DP plagioclase liquidus moves to higher T crystallization of considerable An-rich-Si. O 2 -poor plagioclase – The crystallization of anorthitic plagioclase and low-silica, high-Fe hornblende is an alternative mechanism for the observed calc-alkaline differentiation trend

– E K 2 O-Si. O 2 diagram of nearly 700 analyses for Quaternary island arc volcanics from the Sunda-Banda arc. From Wheller et al. (1987) J. Volcan. Geotherm. Res. , 32, 137 -160.

• REEs Trace Elements – Slope within series is similar, but height varies with FX due to removal of Ol, Plag, and Pyx – (+) slope of low-K DM • Some even more depleted than MORB – Others have more normal slopes – Thus heterogeneous mantle sources – HREE flat, so no deep garnet REE diagrams for some representative Low-K (tholeiitic), Medium. K (calc-alkaline), and High-K basaltic andesites. An N -MORB is included for reference (from Sun and Mc. Donough, 1989). After Gill (1981) Orogenic Andesites and Plate Tectonics. Springer. Verlag.

• MORB-normalized Spider diagrams – Intraplate OIB has typical hump Winter (2001) Data from Sun and Mc. Donough (1989) In A. D. Saunders and M. J. Norry (eds. ), Magmatism in the Ocean Basins. Geol. Soc. London Spec. Publ. , 42. pp. 313 -345.

• MORB-normalized Spider diagrams – IA: decoupled HFS - LIL (LIL are hydrophilic) What is it about subduction zone setting that causes fluid-assisted enrichment? Figure 14 -3. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall. Data from Sun and Mc. Donough (1989) In A. D. Saunders and M. J. Norry (eds. ), Magmatism in the Ocean Basins. Geol. Soc. London Spec. Publ. , 42. pp. 313 -345. Figure 16 -11 a. MORB-normalized spider diagrams for selected island arc basalts. Using the normalization and ordering scheme of Pearce (1983) with LIL on the left and HFS on the right and compatibility increasing outward from Ba-Th. Data from BVTP. Composite OIB from Fig 14 -3 in yellow.

Petrogenesis of Island Arc Magmas • Why is subduction zone magmatism a paradox?

Of the many variables that can affect the isotherms in subduction zone systems, the main ones are: 1) the rate of subduction 2) the age of the subduction zone 3) the age of the subducting slab 4) the extent to which the subducting slab induces flow in the mantle wedge Other factors, such as: – dip of the slab – frictional heating – endothermic metamorphic reactions – metamorphic fluid flow are now thought to play only a minor role

• Typical thermal model for a subduction zone • Isotherms will be higher (i. e. the system will be hotter) if a) the convergence rate is slower b) the subducted slab is young and near the ridge (warmer) c) the arc is young (<50 -100 Ma according to Peacock, 1991) yellow curves = mantle flow Cross section of a subduction zone showing isotherms (redafter Furukawa, 1993, J. Geophys. Res. , 98, 83098319) and mantle flow lines (yellow- after Tatsumi and Eggins, 1995, Subduction Zone Magmatism. Blackwell. Oxford).

The principal source components IA magmas 1. The crustal portion of the subducted slab 1 a Altered oceanic crust (hydrated by circulating seawater, and metamorphosed in large part to greenschist facies) 1 b Subducted oceanic and forearc sediments 1 c Seawater trapped in pore spaces Cross section of a subduction zone showing isotherms (red-after Furukawa, 1993, J. Geophys. Res. , 98, 8309 -8319) and mantle flow lines (yellow- after Tatsumi and Eggins, 1995, Subduction Zone Magmatism. Blackwell. Oxford).

The principal source components IA magmas 2. 3. 4. 5. The mantle wedge between the slab and the arc crust The lithospheric mantle of the subducting plate The asthenosphere beneath the slab Cross section of a subduction zone showing isotherms (red-after Furukawa, 1993, J. Geophys. Res. , 98, 8309 -8319) and mantle flow lines (yellow- after Tatsumi and Eggins, 1995, Subduction Zone Magmatism. Blackwell. Oxford).

• Left with the subducted crust and mantle wedge • The trace element and isotopic data suggest that both contribute to arc magmatism. How, and to what extent? – Dry peridotite solidus too high for melting of anhydrous mantle to occur anywhere in thermal regime shown – LIL/HFS ratios of arc magmas water plays a significant role in arc magmatism

• The sequence of pressures and temperatures that a rock is subjected to during an interval such as burial, subduction, metamorphism, uplift, etc. is called a pressure-temperaturetime or P-T-t path

• The LIL/HFS trace element data underscore the importance of slab-derived water and a MORB-like mantle wedge source • The flat HREE pattern argues against a garnet-bearing (eclogite) source • Thus modern opinion has swung toward the non-melted slab for most cases

Mantle Wedge P-T-t Paths

• Amphibole-bearing hydrated peridotite should melt at ~ 120 km • Phlogopite-bearing hydrated peridotite should melt at ~ 200 km second arc behind first? Some calculated P-T-t paths for peridotite in the mantle wedge as it follows a path similar to the flow lines in Figure 16 -15. Included are some P-T-t path range for the subducted crust in a mature arc, and the wet and dry solidi for peridotite from Figures 10 -5 and 10 -6. The subducted crust dehydrates, and water is transferred to the wedge (arrow). After Peacock (1991), Tatsumi and Eggins (1995). Winter (2001). Crust and Mantle Wedge

Island Arc Petrogenesis A proposed model for subduction zone magmatism with particular reference to island arcs. Dehydration of slab crust causes hydration of the mantle (violet), which undergoes partial melting as amphibole (A) and phlogopite (B) dehydrate. From Tatsumi (1989), J. Geophys. Res. , 94, 4697 -4707 and Tatsumi and Eggins (1995). Subduction Zone Magmatism. Blackwell. Oxford.

Multi-stage, Multi-source Process • Dehydration of the slab provides the LIL enrichments + enriched Nd, Sr, and Pb isotopic signatures – These components, plus other dissolved silicate materials, are transferred to the wedge in a fluid phase (or melt? ) • The mantle wedge provides the HFS and other depleted and compatible element characteristics

• Phlogopite is stable in ultramafic rocks beyond the conditions at which amphibole breaks down • P-T-t paths for the wedge reach the phlogopite-2 -pyroxene dehydration reaction at about 200 km depth A proposed model for subduction zone magmatism with particular reference to island arcs. Dehydration of slab crust causes hydration of the mantle (violet), which undergoes partial melting as amphibole (A) and phlogopite (B) dehydrate. From Tatsumi (1989), J. Geophys. Res. , 94, 4697 -4707 and Tatsumi and Eggins (1995). Subduction Zone Magmatism. Blackwell. Oxford.

• The parent magma for the calc-alkaline series is a high alumina basalt, a type of basalt that is largely restricted to the subduction zone environment, and the origin of which is controversial • Some high-Mg (>8 wt% Mg. O) high alumina basalts may be primary, as may some andesites, but most surface lavas have compositions too evolved to be primary • Perhaps the more common low-Mg (< 6 wt. % Mg. O), high -Al (>17 wt% Al 2 O 3) types are the result of somewhat deeper fractionation of the primary tholeiitic magma which ponds at a density equilibrium position at the base of the arc crust in more mature arcs

Fractional crystallization occurs at various levels A proposed model for subduction zone magmatism with particular reference to island arcs. Dehydration of slab crust causes hydration of the mantle (violet), which undergoes partial melting as amphibole (A) and phlogopite (B) dehydrate. From Tatsumi (1989), J. Geophys. Res. , 94, 4697 -4707 and Tatsumi and Eggins (1995). Subduction Zone Magmatism. Blackwell. Oxford.