1Calcareous and Ultramafic RocksReading: Winter Chapter 29Calcareous Metamorphic Rocks• Calcareous rocks are predominantly carbonates, usually limestone or dolostone• Typically form in a stable continental shelf environment along a passive margin• They may be pure carbonate, or they may contain variable amounts of other precipitates (such as chert or hematite) or detrital material (sand, clays, etc.)• Result when the passive margin becomes part of an orogenic beltTypes of Calcareous Rocks• Metacarbonates– Carbonate component predominates • Marbles – Nearly pure carbonate• Calc-silicates– Carbonate is subordinate – They may contain Ca-Mg-Fe-Al silicate minerals– Diopside, grossular, Ca-amphiboles, vesuvianite, epidote, wollastonite, etc. Skarns • Calc-silicate rocks formed by metasomatism• Interaction between carbonates and silicate-rich rocks or fluids• Contact between sedimentary layers• Contact between carbonate country rocks and a hot, hydrous, silicate intrusion, such as a graniteChemographics in the CaO-MgO-SiO2-CO2-H2O system. The green shaded areas represent common compositions of limestones and dolostones. Both calcite and dolomite can coexist in carbonate rocks. The left half of the triangle represents metacarbonates. Carbonated ultramafics occupy the right half of the triangle. Winter (2001)Figure 29-2. A portion of the Alta aureole in Little Cottonwood Canyon, SE of Salt Lake City, UT, where talc, tremolite, forsterite, and periclase isograds were mapped in metacarbonates by Moore and Kerrick (1976) Amer. J. Sci., 276, 502-524.2T-XCO2phase diagram for siliceous carbonates at P = 0.1 GPa. The green area is the field in which tremolite is stable, the redish area is the field in which dolomite + diopside is stable, and the blue area is for dolomite + talc. Winter (2001).The sequence of CaO-MgO-SiO2-H2O-CO2compatibility diagrams for metamorphosed siliceous carbonates (shaded half) up metamorphic grade. The dashed isograd requires that tremolite is more abundant than either calcite or quartz. After Spear (1993)Metamorphic zones developed in regionally metamorphosed dolomitic rocks of the Lepontine Alps, along the Swiss-Italian border. After Trommsdorff (1966). Winter (2001).T-XCO2phase diagram for siliceous carbonates at P = 0.5 Gpa. The light-shaded area is the field in which tremolite is stable, the darker shaded areas are the fields in which talc or diopside are stable. Winter (2001).T-XH2Odiagram illustrating the shapes and relative locations of the reactions for theisograds mapped in the Whetstone Lake area. After Carmichael (1970) J. Petrol., 11:147-181.Isograds mapped in the field. Note that isograd (5) crosses the others. This behavior is attributed to infiltration of H2O from the syn-metamorphic pluton in the area, creating a gradient in XH2Oacross the area at a high angle to the regional temperature gradient, equivalent to the T-X diagram. After Carmichael (1970) J. Petrol., 11, 147-181.3Schematic T-XCO2diagram illustrating the characteristic shape of typical dehydration reactions, such as those that generate orthopyroxene from hornblende or biotite. Notice that the amphibolite facies to granulite facies can be accomplished by either an increase in temperature or infiltration of CO2at a constant temperature. Winter (2001) Map of isograds in the pelitic Waterville and calcareous Vassalboroformations of south-central Maine. After Ferry (1983) J. Petrol., 24, 343-376. Petrogenetic grid for water-saturated ultramafic rocks in the system CaO-MgO-SiO2-H2O. The green arrow represents a typical medium P/T metamorphic field gradient. The dark blue area represents the stability range of anthophyllite in “normal” ultramafic compositions. The lighter blue area represents the overall stability range of anthophyllite, including more siliceous ultramafic rocks. After Spear (1993).Ultramafic Metamorphic Rocks• Alpine peridotites– Uppermost mantle = base of slivers of oceanic lithosphere that become incorporated into the continental crust along subduction zones• Dismembered portions of ophiolites– Pieces of oceanic crust and mantle that either separate from the subducting slab and become incorporated into the accretionary wedge of the subduction zone,– Or (more commonly) get trapped between two terranesduring an accretion eventAssociations• Strings of ultramafic bodies in orogens follow major fault zones separating contrasting rock bodies. Interpreted as remnants of oceanic crust + mantle that once separated collisional terranes, and thus mark the suture zone• Association of blueschist facies rocks with the ultramafics further supports a subduction-related originUltramafic Bodies in VermontChain indicating a suture zone of the Ordovician Taconic Orogeny. The ultramafics mark a closed oceanic basin between North American rocks and an accreted island arc terrane. From Chidester, (1968) in Zen et al., Studies in Appalachian Geology, Northern and Maritime. Wiley Interscience.4Chemographics of ultramafic rocks in the CMS-H system (projected from H2O) showing the stable mineral assemblages (in the presence of excess H2O) and changes in topology due to reactions along a medium P/T metamorphic field gradient. The star represents the composition of a typical mantle lherzolite. After Spear (1993).T-XCO2phase diagram for the system CaO-MgO-SiO2-H2O-CO2at 0.5 Gpa. Focuses on ultramafic-carbonate rocks. Shaded fields represent the stability ranges of serpentine-antigorite (purple), anthophyllite in low-SiO2ultramafics (blue), and tremolite in low-SiO2ultramafics (green). Winter