Worked Example Of Batch Melting: Rb And Sr
Worked Example of Batch Melting: Rb and SrBasalt with the mode:Table 9.2. Conversion from mode toweight percentMineral Mode Density Wt prop Wt%ol153.654 0.18cpx333.4 112.2 0.37plag512.7 137.7 0.45Sum303.9 1.001. Convert to weight % minerals (Wol Wcpx etc.)
Worked Example of Batch Melting: Rb and SrBasalt with the mode:Table 9.2. Conversion from mode toweight percentMineral Mode Density Wt prop Wt%ol153.654 0.18cpx333.4 112.2 0.37plag512.7 137.7 0.45Sum303.9 1.001. Convert to weight % minerals (Wol Wcpx etc.)2. Use equation eq. 9.4:Di Σ WA Diand the table of D values for Rb and Sr in each mineralto calculate the bulk distribution coefficients: DRb 0.045 and DSr 0.848
3. Use the batch melting equation(9.5)1CL C O Di (1 F) Fto calculate CL/CO for various values of FTable 9.3 . Batch Fractionation Model forRb and SrF0.050.10.150.20.30.40.50.60.70.80.9C L/C O 1/(D(1-F) F)D RbD rom Winter (2010) An Introduction to Igneous and Metamorphic Petrology. Prentice Hall.
4. Plot CL/CO vs. F for each elementFigure 9.3. Change in the concentrationof Rb and Sr in the melt derived byprogressive batch melting of a basalticrock consisting of plagioclase, augite,and olivine. From Winter (2001) AnIntroduction to Igneous andMetamorphic Petrology. Prentice Hall.
Incremental Batch Melting Calculate batch melting for successivebatches (same equation)Must recalculate Di as solids change asminerals are selectively melted (computer)
Fractional Crystallization1. Crystals remain in equilibrium with eachmelt increment1CL C O Di (1 F) F
Rayleigh fractionationThe other extreme: separation of eachcrystal as it formed perfectly continuousfractional crystallization in a magmachamber
Rayleigh fractionationThe other extreme: separation of eachcrystal as it formed perfectly continuousfractional crystallization in a magmachamber Concentration of some element in the residualliquid, CL is modeled by the Rayleigh equation:eq. 9.8 CL/CO F (D-1) Rayleigh Fractionation
4. Plot CL/CO vs. F for each elementFigure 9.3. Change in the concentrationof Rb and Sr in the melt derived byprogressive batch melting of a basalticrock consisting of plagioclase, augite,and olivine. From Winter (2001) AnIntroduction to Igneous andMetamorphic Petrology. Prentice Hall.
Other models are used to analyze Mixing of magmas Wall-rock assimilation Zone refining Combinations of processes
The Rare Earth Elements (REE)
Contrasts and similarities in the D values:All are incompatibleTable 9-1. Partition Coefficients (CS/CL) for Some Commonly Used TraceElements in Basaltic and Andesitic RocksHREE are lessincompatibleEspecially ingarnetEu can 2 which conc.in plagioclaseRbSrBaNiCrLaCeNdSmEuDyErYbLuRare Earth ElementsAlso 00.030.020.030.050.050.150.230.340.42Data from Rollinson 20.4740.2430.5823.170.5836.560.542 11.50.506 11.9PlagAmph .40.0191.563* Eu3 /Eu2 Italics are estimated
REE DiagramsPlots of concentration as the ordinate (y-axis)against increasing atomic numberDegree of compatibility increases from left to rightacross the diagram (“lanthanide contraction”)Concentration La Ce Nd Sm Eu Tb Er Dy Yb Lu
Log (Abundance in CI Chondritic Meteorite)11HHe1098C7654321LiONe MgSiFeNS ArCa NiNaTiAlPKClFVBScSnBaPt Pb0Be-1Th-2U-30102030405060708090Atomic Number (Z) Eliminate Oddo-Harkins effect and make y-scalemore functional by normalizing to a standard estimates of primordial mantle REE chondrite meteorite concentrations100
What would an REE diagram looklike for an analysis of a .002.000.0056 La58CeL60Nd 62Sm 64Eu66Tb68Er 70 Yb 72Lu
Divide each element in analysis by theconcentration in a chondrite 6 La58CeL60Nd 62Sm 64Eu66Tb68Er 70 Yb 72Lu
REE diagrams using batch melting model ofa garnet lherzolite for various values of F:Figure 9.4. Rare Earthconcentrations (normalized tochondrite) for melts produced atvarious values of F via melting of ahypothetical garnet lherzolite usingthe batch melting model (equation9.5). From Winter (2001) AnIntroduction to Igneous andMetamorphic Petrology. PrenticeHall.
Europium anomaly when plagioclase isa fractionating phenocrystor a residual solid in source Figure 9.5. REE diagram for 10%batch melting of a hypotheticallherzolite with 20% plagioclase,resulting in a pronounced negativeEuropium anomaly. From Winter(2001) An Introduction to Igneousand Metamorphic Petrology.Prentice Hall.
Normalized Multielement (Spider) DiagramsAn extension of the normalized REEtechnique to a broader spectrum of elementsChondrite-normalized spiderdiagrams are commonlyorganized by (the author’sestimate) of increasingincompatibility L RDifferent estimates different ordering (poorstandardization)Fig. 9.6. Spider diagram for an alkaline basalt from Gough Island, southern Atlantic.After Sun and MacDonough (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 SpiderSeparates LIL and HFSFigure 9.7. Ocean island basaltplotted on a mid-ocean ridgebasalt (MORB) normalizedspider diagram of the type usedby Pearce (1983). Data fromSun and McDonough (1989).From Winter (2001) AnIntroduction to Igneous andMetamorphic Petrology.Prentice Hall.
Application of Trace Elements toIgneous Systems1. Use like major elements on variation diagrams todocument FX, assimilation, etc. in a suite of rocks More sensitive larger variations as processcontinuesFigure 9.1a. Ni Harker Diagram forCrater Lake. From data compiled byRick Conrey. From Winter (2001) AnIntroduction to Igneous andMetamorphic Petrology. Prentice Hall.
Contrasts and similarities in the D values:All are incompatibleTable 9-1. Partition Coefficients (CS/CL) for Some Commonly Used TraceElements in Basaltic and Andesitic RocksHREE are lessincompatibleEspecially ingarnetEu can 2 which conc.in plagioclaseRbSrBaNiCrLaCeNdSmEuDyErYbLuRare Earth ElementsAlso 00.030.020.030.050.050.150.230.340.42Data from Rollinson 20.4740.2430.5823.170.5836.560.542 11.50.506 11.9PlagAmph .40.0191.563* Eu3 /Eu2 Italics are estimated
2. Identification of the source rock or a particularmineral involved in either partial melting orfractional crystallization processes
Garnet concentrates the HREE and fractionates among themThus if garnet is in equilibrium with the partial melt (a residualphase in the source left behind) expect a steep (-) slope in REE andHREEShallow ( 40km) partialmelting of themantle will haveplagioclase inthe resuduumand a Euanomaly willresultRbSrBaNiCrLaCeNdSmEuDyErYbLuRare Earth ElementsTable 9-1. Partition Coefficients (CS/CL) for Some Commonly Used TraceElements in Basaltic and Andesitic 00.030.020.030.050.050.150.230.340.42Data from Rollinson 20.4740.2430.5823.170.5836.560.542 11.50.506 11.9PlagAmph .40.0191.563* Eu3 /Eu2 Italics are estimated
10.0067% Olsample/chondrite8.0017% Opx17% CpxGarnet and Plagioclaseeffect on HREE6.004.002.000.005658 Ce 60 Nd 62Sm Eu64LaTb6668Er70 Lu 72Yb10.0010.0060% Ol 15% Opx 15% Cpx 10%Plag57% Ol8.0014% Opx14% Cpx 14% 04.002.002.000.000.00La Ce Nd Sm EuTbErYb Lu5658La64Ce60 Nd 62Sm EuTb6668Er70 LuYb72
Figure 9.3. Change in the concentrationof Rb and Sr in the melt derived byprogressive batch melting of a basalticrock consisting of plagioclase, augite,and olivine. From Winter (2001) AnIntroduction to Igneous andMetamorphic Petrology. Prentice Hall.
Table 9.6 A Brief Summary of Some Particularly Useful Trace Elements in Igneous PetrologyElementUse as a Petrogenetic IndicatorNi, Co, CrHighly compatible elements. Ni and Co are concentrated in olivine, and Cr in spinel and clinopyroxene. High concentrationsindicate a mantle source, limited fractionation, or crystal accumulation.Zr, HfVery incompatible elements that do not substitute into major silicate phases (although they may replace Ti in titanite orrutile). High concentrations imply an enriched source or extensive liquid evolution.Nb, TaHigh field-strength elements that partition into Ti-rich phases (titanite, Ti-amphibole, Fe-Ti oxides. Typically lowconcentrations in subduction-related melts.Ru, Rh, Pd,Platinum group elements (PGEs) are siderophile and used mostly to study melting and crystallization in mafic-ultramaficRe, Os, Ir,systems in which PGEs are typically hosted by sulfides. The Re/Os isotopic system is controlled by initial PGEPddifferentiation and is applied to mantle evolution and mafic melt processes.ScConcentrates in pyroxenes and may be used as an indicator of pyroxene fractionation.SrSubstitutes for Ca in plagioclase (but not in pyroxene), and, to a lesser extent, for K in K-feldspar. Behaves as a compatibleelement at low pressure where plagioclase forms early, but as an incompatible element at higher pressure whereplagioclase is no longer stable.REEMyriad uses in modeling source characteristics and liquid evolution. Garnet accommodates the HREE more than the LREE,and orthopyroxene and hornblende do so to a lesser degree. Titanite and plagioclase accommodates more LREE. Eu2 isstrongly partitioned into plagioclase.YCommonly incompatible. Strongly partitioned into garnet and amphibole. Titanite and apatite also concentrate Y, so thepresence of these as accessories could have a significant effect.
Trace elements as a tool to determinepaleotectonic environment Useful for rocks in mobile belts that are nolonger recognizably in their original settingCan trace elements be discriminators ofigneous environment?Approach is empirical on modern occurrencesConcentrate on elements that are immobileduring low/medium grade metamorphism
Figure 9.8 Examples of discrimination diagrams used to infer tectonic setting of ancient (meta)volcanics. (a) after Pearce and Cann (1973), (b)after Pearce (1982), Coish et al. (1986). Reprinted by permission of the American Journal of Science, (c) after Mullen (1983) Copyright withpermission from Elsevier Science, (d) and (e) after Vermeesch (2005) AGU with permission.
Worked Example of Batch Melting: Rb and Sr Table 9.2.Conversion from mode to weight percent Mineral Mode Density Wt prop Wt% ol 15 3.6 54 0.18 cpx 33 3.4 112.2 0.37
3.1.1 Determining the melting point in the capillary tube 16 3.1.2 Immediate melting point 16 3.2 Principles of melting point determination 18 3.2.1 Melting point determination according to the pharmacopoeia 19 3.2.2 Thermodynamic determination of melting points 20 3.3 Melting point determination yesterday and today - an overview 21
WITEPSOL E 85 melting point 42–44 C HV 5–15 WITEPSOL S 51 melting point 30–32 C HV 55–70 WITEPSOL S 55 melting point 33.5–35.5 C HV 50–65 WITEPSOL S 58 melting point 31.5–33.5 C HV 60–70 WITEPSOL W 32 melting point 32–33.5 C HV 40-50 WITEPSOL W 25 melting point 33.5–35.5 C HV 20-30
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