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

Igneous Minerals Quartz, Feldspars (plagioclase and alkaline), Olivines, Pyroxenes, Amphiboles Accessory Minerals – mostly in small quantities or in ‘special’ rocks Magnetite (Fe3O4) Ilmenite (FeTiO3) Apatite (Ca5(PO4)3(OH,F,Cl) Zircon (ZrSiO4) Titanite (CaTiSiO5) Pyrite (FeS2) Fluorite (CaF2)

Mg2+ Na+ Ca2+ Fe2+ Liquid hot rock MAGMA cooling O2- Si4+ Mg2+ Fe2+ Minerals which form are thus a function of melt composition and how fast it cools (re-equilibration?)  governed by the stability of those minerals and how quickly they may or may not react with the melt during crystallization General Compositions  Silicic (Si-rich), Sialic (Si and Al rich), Intermediate, Mafic (Mg and Fe-rich), Ultramafic Also ID’d based on alkalic (K and Na) or alkaline (Ca-rich) Liquid hot MAGMA Ca2+ Na+ Mg2+ Fe2+ Si4+ O2- rock Mg2+ Fe2+ cooling Mg2+

Composition From Magma we saw how a crystal’s composition can change on crystallization  different elemental composition from melt on partial crystallization

Silica and Aluminum Content Oversaturated if it contains Quartz Undersaturated if it has silica-deficient minerals (like the feldspathoids, ex: nepheline) Aluminum Peraluminous if it has a great excess of aluminum  after feldspars form, more Al left over for Al-rich phases like corumndum, garnet, kyanite, etc. Peralkaline – So little Al left after feldspars form, only Al-deficient minerals like aegerine (type of pyroxene) and riebekite (sodic amphibole)

Classification of Igneous Rocks Figure 2-4. A chemical classification of volcanics based on total alkalis vs. silica. After Le Bas et al. (1986) J. Petrol., 27, 745-750. Oxford University Press.

Igneous Rocks Textures  aphanitic, phaneritic, porphyritic, pegmatitic, vesicular, glass, and pyroclastic Compositions  Silicic, Intermediate, Mafic, Ultramafic

Igneous Textures Figure 3-1. Idealized rates of crystal nucleation and growth as a function of temperature below the melting point. Slow cooling results in only minor undercooling (Ta), so that rapid growth and slow nucleation produce fewer coarse-grained crystals. Rapid cooling permits more undercooling (Tb), so that slower growth and rapid nucleation produce many fine-grained crystals. Very rapid cooling involves little if any nucleation or growth (Tc) producing a glass.

Figure 3-17. “Ostwald ripening” in a monomineralic material Figure 3-17. “Ostwald ripening” in a monomineralic material. Grain boundaries with significant negative curvature (concave inward) migrate toward their center of curvature, thus eliminating smaller grains and establishing a uniformly coarse-grained equilibrium texture with 120o grain intersections (polygonal mosaic). © John Winter and Prentice Hall

Textures I Aphanitic - fine grain size (< 1 mm); result of quick cooling Rhyolite, Basalt, Rhyolite, Andesite Phaneritic - coarse grain size; visible grains (1-10 mm); result of slow cooling Granite, Diorite, Gabbro Pegmatitic - very large crystals (many over 2 cm) Granite pegmatite or pegmatitic granite

Porphyritic- Mixture of grain sizes caused by mixed cooling history; slow cooling first, followed by a period of somewhat faster cooling. Terms for the textural components: Phenocrysts - the large crystals Groundmass or matrix - the finer crystals surrounding the large crystals. The groundmass may be either aphanitic or phaneritic. Types of porphyritic textures: Porphyritic-aphanitic Porphyritic-phaneritic Origin: mixed grain sizes and hence cooling rates, imply upward movement of magma from a deeper (hotter) location of extremely slow cooling, to either: a much shallower (cooler) location with fast cooling (porphyritic- aphanitic), or a somewhat shallower (slightly cooler) location with continued fairly slow cooling (porphyritic-phaneritic).

Typically Volcanic Textures Glassy - instantaneous cooling Obsidian = volcanic glass Vesicular - contains tiny holes called vesicles which formed due to gas bubbles in the lava or magma. Very porous. May resemble a sponge. Commonly low density; may float on water. Vesicular Basalt, Pumice, Scoria Pyroclastic or Fragmental - pieces of rock and ash come out of a volcano and get welded together by heat. May resemble rhyolite or andesite, but close examination shows pieces of fine-grained rock fragments in it. May also resemble a sedimentary conglomerate or breccia, except that rock fragments are all fine-grained igneous or vesicular. Tuff - made of volcanic ash Volcanic breccia - contains fragments of fine-grained igneous rocks that are larger than ash.

Classification based on Field Relations Extrusive or volcanic rocks: typically aphanitic or glassy. Many varieties are porphyritic and some have fragmental (volcaniclastic) fabric. High-T disordered fsp is common (e.g. sanadine). Also see leucite, tridymite, and cristobalite. Intrusive or plutonic rocks: typically phaneritic. Monomineralic rocks of plagioclase, olivine, or pyroxene are well known but rare. Amphiboles and biotites are commonly altered to chlorite. Muscovite found in some granites, but rarely in volcanic rocks. Perthitic fsp, reflecting slow cooling and exsolution is widespread.

Names of Igneous Rocks Texture + Composition = name Set up diagrams (many ternary ones again, you remember how these work?) to represent composition changes for rocks of a certain texture Composition can be related to specific minerals, or even physical characteristics of mineral grains Modal Composition - % of minerals comprising a rock

Visual Estimation of Modal Abundance

Classification based on Modal Mineralogy Felsic rocks: mnemonic based on feldspar and silica. Also applies to rocks containing abundant feldspathoids, such as nepheline. GRANITE Mafic rocks: mnemonic based on magnesium and ferrous/ferric. Synonymous with ferromagnesian, which refers to biotite, amphibole, pyroxene, olivine, and Fe-Ti oxides. BASALT Ultramafic rocks: very rich in Mg and Fe. Generally have little feldspar. PERIDOTITE Silicic rocks: dominated by quartz and alkali fsp. Sometimes refered to as sialic (Si + Al).

Classification of Igneous Rocks

granite granodiorite

Classification of Phaneritic Igneous Rocks Q Quartzolite 90 90 Quartz-rich Granitoid 60 60 The rock must contain a total of at least 10% of the minerals below. Renormalize to 100% Granite Grano- Tonalite Alkali Feldspar Granite diorite Q=quartz A=Alkali fledspars (An0-An5) P=Plagioclase feldspars (An5-An100) F=Feldspathoid Alkali Fs. 20 20 Qtz. Diorite/ Quartz Syenite Quartz Quartz Quartz Qtz. Gabbro Alkali Fs. Syenite Monzonite Monzodiorite Syenite 5 5 Diorite/Gabbro/ Syenite Monzonite Monzodiorite A 10 35 65 90 Anorthosite (Foid)-bearing (Foid)-bearing (Foid)-bearing P Syenite Monzonite Monzodiorite (Foid)-bearing 10 10 Diorite/Gabbro (Foid)-bearing Alkali Fs. Syenite (Foid) Syenite (Foid) (Foid) Monzosyenite Monzodiorite (Foid) Gabbro Figure 2-2. A classification of the phaneritic igneous rocks. a. Phaneritic rocks with more than 10% (quartz + feldspar + feldspathoids). After IUGS. 60 60 (Foid)olites F

Aphanitic rocks basalt rhyolite

Classification of Igneous Rocks Figure 2-3. A classification and nomenclature of volcanic rocks. After IUGS.

Classification of Igneous Rocks Figure 2-5. Classification of the pyroclastic rocks. a. Based on type of material. After Pettijohn (1975) Sedimentary Rocks, Harper & Row, and Schmid (1981) Geology, 9, 40-43. b. Based on the size of the material. After Fisher (1966) Earth Sci. Rev., 1, 287-298.

Classification of Igneous Rocks Plagioclase Feldspar Anorthosite Figure 2-2. A classification of the phaneritic igneous rocks. b. Gabbroic rocks. c. Ultramafic rocks. After IUGS. Olivine Clinopyroxene Orthopyroxene Lherzolite Harzburgite Wehrlite Websterite Orthopyroxenite Clinopyroxenite Olivine Websterite Peridotites Pyroxenites 90 40 10 Dunite Pyroxene Olivine (c)

Igneous Textures Figure 3-2. Backscattered electron image of quenched “blue glassy pahoehoe,” 1996 Kalapana flow, Hawaii. Black minerals are felsic plagioclase and gray ones are mafics. a. Large embayed olivine phenocryst with smaller plagioclase laths and clusters of feathery augite nucleating on plagioclase. Magnification ca. 400X. b. ca. 2000X magnification of feathery quenched augite crystals nucleating on plagioclase (black) and growing in a dendritic form outward. Augite nucleates on plagioclase rather than pre-existing augite phenocrysts, perhaps due to local enrichment in mafic components as plagioclase depletes the adjacent liquid in Ca, Al, and Si. © John Winter and Prentice Hall.

Igneous Textures Figure 3-4. a. Skeletal olivine phenocryst with rapid growth at edges enveloping melt at ends. Taupo, N.Z. b. “Swallow-tail” plagioclase in trachyte, Remarkable Dike, N.Z. Length of both fields ca. 0.2 mm. From Shelley (1993). Igneous and Metamorphic Rocks Under the Microscope. © Chapman and Hall. London.

Igneous Textures Figure 3-5. a. Compositionally zoned hornblende phenocryst with pronounced color variation visible in plane-polarized light. Field width 1 mm. b. Zoned plagioclase twinned on the carlsbad law. Andesite, Crater Lake, OR. Field width 0.3 mm. © John Winter and Prentice Hall.

Figure 3-6. Examples of plagioclase zoning profiles determined by microprobe point traverses. a. Repeated sharp reversals attributed to magma mixing, followed by normal cooling increments. b. Smaller and irregular oscillations caused by local disequilibrium crystallization. c. Complex oscillations due to combinations of magma mixing and local disequilibrium. From Shelley (1993). Igneous and Metamorphic Rocks Under the Microscope. © Chapman and Hall. London.

Figure 3-7. Euhedral early pyroxene with late interstitial plagioclase (horizontal twins). Stillwater complex, Montana. Field width 5 mm. © John Winter and Prentice Hall.

Figure 3-8. Ophitic texture Figure 3-8. Ophitic texture. A single pyroxene envelops several well-developed plagioclase laths. Width 1 mm. Skaergård intrusion, E. Greenland. © John Winter and Prentice Hall.

Figure 3-9. a. Granophyric quartz-alkali feldspar intergrowth at the margin of a 1-cm dike. Golden Horn granite, WA. Width 1mm. b. Graphic texture: a single crystal of cuneiform quartz (darker) intergrown with alkali feldspar (lighter). Laramie Range, WY. © John Winter and Prentice Hall.

Figure 3-10. Olivine mantled by orthopyroxene in (a) plane-polarized light and (b) crossed nicols, in which olivine is extinct and the pyroxenes stand out clearly. Basaltic andesite, Mt. McLaughlin, Oregon. Width ~ 5 mm. © John Winter and Prentice Hall.

Figure 3-11. a. Sieve texture in a cumulophyric cluster of plagioclase phenocrysts. Note the later non-sieve rim on the cluster. Andesite, Mt. McLoughlin, OR. Width 1 mm. © John Winter and Prentice Hall.

Figure 3-11. b. Resorbed and embayed olivine phenocryst. Width 0. 3 mm Figure 3-11. b. Resorbed and embayed olivine phenocryst. Width 0.3 mm. © John Winter and Prentice Hall.

Figure 3-11. c. Hornblende phenocryst dehydrating to Fe-oxides plus pyroxene due to pressure release upon eruption, andesite. Crater Lake, OR. Width 1 mm. © John Winter and Prentice Hall.

Figure 3-12. a. Trachytic texture in which microphenocrysts of plagioclase are aligned due to flow. Note flow around phenocryst (P). Trachyte, Germany. Width 1 mm. From MacKenzie et al. (1982). © John Winter and Prentice Hall. Figure 3-12. b. Felty or pilotaxitic texture in which the microphenocrysts are randomly oriented. Basaltic andesite, Mt. McLaughlin, OR. Width 7 mm. © John Winter and Prentice Hall.

Figure 3-13. Flow banding in andesite. Mt. Rainier, WA Figure 3-13. Flow banding in andesite. Mt. Rainier, WA. © John Winter and Prentice Hall. Figure 3-15. Intergranular texture in basalt. Columbia River Basalt Group, Washington. Width 1 mm. © John Winter and Prentice Hall.

Figure 3-14. Development of cumulate textures. a Figure 3-14. Development of cumulate textures. a. Crystals accumulate by crystal settling or simply form in place near the margins of the magma chamber. In this case plagioclase crystals (white) accumulate in mutual contact, and an intercumulus liquid (pink) fills the interstices. b. Orthocumulate: intercumulus liquid crystallizes to form additional plagioclase rims plus other phases in the interstitial volume (colored). There is little or no exchange between the intercumulus liquid and the main chamber. After Wager and Brown (1967), Layered Igneous Rocks. © Freeman. San Francisco.

Figure 3-14. Development of cumulate textures. c Figure 3-14. Development of cumulate textures. c. Adcumulates: open-system exchange between the intercumulus liquid and the main chamber (plus compaction of the cumulate pile) allows components that would otherwise create additional intercumulus minerals to escape, and plagioclase fills most of the available space. d. Heteradcumulate: intercumulus liquid crystallizes to additional plagioclase rims, plus other large minerals (hatched and shaded) that nucleate poorly and poikilitically envelop the plagioclases. . After Wager and Brown (1967), Layered Igneous Rocks. © Freeman. San Francisco.

Figure 3-16. a. The interstitial liquid (red) between bubbles in pumice (left) become 3-pointed-star-shaped glass shards in ash containing pulverized pumice. If they are sufficiently warm (when pulverized or after accumulation of the ash) the shards may deform and fold to contorted shapes, as seen on the right and b. in the photomicrograph of the Rattlesnake ignimbrite, SE Oregon. Width 1 mm. © John Winter.

Figure 3-18. a. Carlsbad twin in orthoclase Figure 3-18. a. Carlsbad twin in orthoclase. Wispy perthitic exsolution is also evident. Granite, St. Cloud MN. Field widths ~1 mm. © John Winter and Prentice Hall. Figure 3-18. b. Very straight multiple albite twins in plagioclase, set in felsitic groundmass. Rhyolite, Chaffee, CO. Field widths ~1 mm. © John Winter and Prentice Hall.

Figure 3-18. (c-d) Tartan twins in microcline. Field widths ~1 mm Figure 3-18. (c-d) Tartan twins in microcline. Field widths ~1 mm. © John Winter and Prentice Hall.

Figure 3-19. Polysynthetic deformation twins in plagioclase Figure 3-19. Polysynthetic deformation twins in plagioclase. Note how they concentrate in areas of deformation, such as at the maximum curvature of the bent cleavages, and taper away toward undeformed areas. Gabbro, Wollaston, Ontario. Width 1 mm. © John Winter and Prentice Hall.

Pyx Hbl Figure 3-20. a. Pyroxene largely replaced by hornblende. Some pyroxene remains as light areas (Pyx) in the hornblende core. Width 1 mm. b. Chlorite (green) replaces biotite (dark brown) at the rim and along cleavages. Tonalite. San Diego, CA. Width 0.3 mm. © John Winter and Prentice Hall. Bt Chl

Figure 3-21. Myrmekite formed in plagioclase at the boundary with K-feldspar. Photographs courtesy © L. Collins. http://www.csun.edu/~vcgeo005