Metamorphism of Mafic Rocks Metamorphism of Mafic Rocks l Mineral changes and associations along T-P gradients Plagioclase: characteristic of the three facies series l More Ca-rich plagioclases become progressively F Hydration of original mafic minerals generally required unstable as T lowered F If water unavailable, mafic igneous rocks will remain largely l General correlation between temperature and unaffected, even as associated sediments are completely re- maximum An-content of the stable plagioclase equilibrated F At low metamorphic grades only albite (An0-3) is stable F Coarse-grained intrusives are the least permeable and likely to resist metamorphic changes F In the upper-greenschist facies oligoclase becomes stable. The An-content of plagioclase thus jumps from An1-7 to F Tuffs and graywackes are the most susceptible An17- 20 (across the peristerite solvus) as grade increases F Andesine and more calcic plagioclases are stable in the upper amphibolite and granulite facies l The excess Ca and Al ® calcite, an epidote mineral, sphene, or amphibole, etc., depending on P-T-X Metamorphism of Mafic Rocks Mafic Assemblages at Low Grades l Clinopyroxene breaks down to a number of mafic l Zeolite and prehnite-pumpellyite facies minerals, depending on grade. l Do not always occur - typically require unstable l These minerals include chlorite, actinolite, protolith hornblende, epidote, a metamorphic pyroxene, etc. l Boles and Coombs (1975) showed that l The mafics that form are commonly diagnostic of the metamorphism of tuffs in NZ accompanied by grade and facies substantial chemical changes due to circulating fluids, and that these fluids played an important role in the metamorphic minerals that were stable l The classic area of burial metamorphism thus has a strong component of hydrothermal metamorphism as well Mafic Assemblages of the Medium Greenschist, Amphibolite, Granulite P/T Series: Greenschist, Facies l Zeolite and prehnite-pumpellyite facies not present in Amphibolite, and Granulite Facies the Scottish Highlands l The greenschist, amphibolite and granulite facies l Metamorphism of mafic rocks first evident in the constitute the most common facies series of regional greenschist facies, which correlates with the chlorite metamorphism and biotite zones of the associated pelitic rocks l The classical Barrovian series of pelitic zones and the F Typical minerals include chlorite, albite, actinolite, lower-pressure Buchan-Abukuma series are epidote, quartz, and possibly calcite, biotite, or variations on this trend stilpnomelane F Chlorite, actinolite, and epidote impart the green color from which the mafic rocks and facies get their name 1 Greenschist, Amphibolite, Granulite Facies Greenschist, Amphibolite, Granulite Facies l ACF diagram l Greenschist ® amphibolite facies transition l The most involves two major mineralogical changes characteristic mineral assemblage of the 1. Albite ® oligoclase (increased Ca-content greenschist facies is: with temperature across the peristerite gap) chlorite + albite + epidote + actinolite ± 2. Actinolite ® hornblende (amphibole accepts quartz increasing aluminum and alkalis at higher Ts) l Both transitions occur at approximately the Fig. 25-6. ACF diagram illustrating same grade, but have different P/T slopes representative mineral assemblages for metabasites in the greenschist facies. The composition range of common mafic rocks is shaded. Winter (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall. Greenschist, Amphibolite, Granulite Facies l ACF diagram l Typically two-phase Hbl-Plag l Amphibolites are typically black rocks with up to about 30% white plagioclase l Like diorites, but differ texturally l Garnet in more Al-Fe-rich and Ca-poor mafic rocks l Clinopyroxene in Al-poor-Ca- rich rocks Fig. 25-7. ACF diagram illustrating representative mineral assemblages for metabasites in the amphibolite Fig. 26-19. Simplified petrogenetic grid for metamorphosed mafic rocks showing the location of several determined facies. The composition range of common mafic rocks is univariant reactions in the CaO-MgO-Al2O3-SiO2-H2O-(Na2O) system ( “C(N)MASH”). Winter (2001) An shaded. Winter (2001) An Introduction to Igneous and Introduction to Igneous and Metamorphic Petrology. Prentice Hall . Metamorphic Petrology. Prentice Hall. Greenschist, Amphibolite, Granulite Greenschist, Amphibolite, Granulite Facies Facies o l Amphibolite ® granulite facies ~ 650-700 C l Mafic rocks generally melt at higher l If aqueous fluid, associated pelitic and quartzo- temperatures feldspathic rocks (including granitoids) begin to l If water is removed by the earlier melts the melt in this range at low to medium pressures ® remaining mafic rocks may become depleted migmatites and melts may become mobilized in water l As a result not all pelites and quartzo-feldspathic l Hornblende decomposes and orthopyroxene rocks reach the granulite facies + clinopyroxene appear o l This reaction occurs over a T interval > 50 C 2 Greenschist, Amphibolite, Granulite Facies l Granulite facies characterized by a largely anhydrous mineral assemblage l Critical meta-basite mineral assemblage is orthopyroxene + clinopyroxene + plagioclase + quartz F Garnet, minor hornblende and/or biotite may be Fig. 26-19. Simplified petrogenetic grid for metamorphosed mafic rocks showing the present Fig. 25-8. ACF diagram for the granulite facies. The location of several determined univariant reactions in the CaO -MgO-Al 2O 3-SiO2-H 2O-(Na2O) system (“ C(N)MASH”). Winter (2001) An Introduction to Igneous and Metamorphic composition range of common mafic rocks is shaded. Winter (2001) An Introduction to Igneous and Petrology. Prentice Hall. Metamorphic Petrology. Prentice Hall. Greenschist, Amphibolite, Granulite Greenschist, Amphibolite, Granulite Facies Facies Origin of granulite facies rocks is complex and 2) Granulites are dry controversial. There is general agreement, however, F Rocks don’t melt due to lack of available water on two points F Granulite facies terranes represent deeply buried and 1) Granulites represent unusually hot conditions dehydrated roots of the continental crust F Fluid inclusions in granulite facies rocks of S. Norway are F Temperatures > 700o C (geothermometry has CO -rich, whereas those in the amphibolite facies rocks yielded some very high temperatures, even in 2 are H2O-rich excess of 1000oC) F Average geotherm temperatures for granulite facies depths should be in the vicinity of 500oC, suggesting that granulites are the products of crustal thickening and excess heating Mafic Assemblages of the Low P/T Series: Albite-Epidote Hornfels, Hornblende Hornfels, Pyroxene Hornfels, and Sanidinite Facies l Mineralogy of low-pressure metabasites not appreciably different from the med.-P facies series l Albite-epidote hornfels facies correlates with the greenschist facies into which it grades with increasing pressure l Hornblende hornfels facies correlates with the amphibolite facies, and the pyroxene hornfels and sanidinite facies correlate with the Fig. 25-9. Typical mineral changes that take place in metabasic rocks durin g progressive metamorphism in the medium P/T facies series. The approximate location of the pelitic zones of Barrovian metamorphism are included for comparison. Winter (2001) An Introduction to Igneous and Metamorphic Petrolo gy. Prentice Hall. granulite facies 3 Mafic Assemblages of the Low P/T Series: Albite-Epidote Hornfels, Hornblende Hornfels, Pyroxene Hornfels, and Sanidinite Facies Facies of contact metamorphism are readily distinguished from those of medium-pressure regional metamorphism on the basis of: F Fig. 25-2. Metapelites (e.g. andalusite and cordierite) Temperature- pressure F Textures and field relationships diagram showing the generally F Mineral thermobarometry accepted limits of the various facies used in this text. Winter (2001) Mafic Assemblages of the Low P/T Series: Mafic Assemblages of the High P/T Albite-Epidote Hornfels, Hornblende Hornfels, Pyroxene Hornfels, and Sanidinite Facies Series: Blueschist and Eclogite Facies l Mafic rocks (not pelites) develop definitive mineral l The innermost zone of most aureoles rarely reaches assemblages under high P/T conditions the pyroxene hornfels facies l High P/T geothermal gradients characterize subduction zones F If the intrusion is hot and dry enough, a narrow l Mafic blueschists are easily recognizable by their color, and zone develops in which amphiboles break down are useful indicators of ancient subduction zones to orthopyroxene + clinopyroxene + plagioclase + l The great density of eclogites: subducted basaltic oceanic quartz (without garnet), characterizing this facies crust becomes more dense than the surrounding mantle l Sanidinite facies is not evident in basic rocks Blueschist and Eclogite Facies Blueschist and Eclogite Facies Alternative paths to the blueschist facies l The blueschist facies is characterized in metabasites by the presence of a sodic blue amphibole stable only at high pressures (notably glaucophane, but some solution of crossite or riebeckite is possible) Fig. 25-2. Temperature- l The association of glaucophane + lawsonite is pressure diagram showing the generally accepted diagnostic. Crossite is stable to lower pressures, and limits of the various facies used in this text. Winter may extend into transitional zones (2001) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall. l Albite breaks down at high pressure by reaction to jadeitic pyroxene + quartz: NaAlSi 3O8 = NaAlSi 2O6