Geothermobarometry

Last updated March 06, 2024

Geothermobarometry is the methodology for estimating the pressure and temperature history of rocks (metamorphic, igneous or sedimentary). Geothermobarometry is a combination of geobarometry, where the pressure attained (and retained) by a mineral assemblage is estimated, and geothermometry where the temperature attained (and retained) by a mineral assemblage is estimated.

Methodology

Geothermobarometry relies upon understanding the temperature and pressure of the formation of minerals within rocks.^[1] There are several methods of measuring the temperature or pressure of mineral formation or re-equilibration relying for example on chemical equilibrium between minerals^[1]^[2]^[3] or by measuring the chemical composition^[4] and/or the crystal-chemical state of order^[5] of individual minerals or by measuring the residual stresses on solid inclusions^[6] or densities in fluid inclusions.^[7]

"Classic" (thermodynamic) thermobarometry^[8] relies upon the attainment of thermodynamic equilibrium between mineral pairs/assemblages that vary their compositions as a function of temperature and pressure. The distribution of component elements between the mineral assemblages is then analysed using a variety of analytical techniques as for example electron microprobe (EM), scanning electron microscope (SEM), Mass Spectrometry (MS). There are numerous extra factors to consider such as oxygen fugacity and water activity (roughly, the same as concentration) that must be accounted for using the appropriate methodological and analytical approach (e.g. Mössbauer spectroscopy, micro-raman spectroscopy, infrared spectroscopy etc...) Geobarometers are typically net-transfer reactions, which are sensitive to pressure but have little change with temperature, such as garnet-plagioclase-muscovite-biotite reaction that involves a significant volume reduction upon high pressure:^[1]

{\mathsf {\underbrace {{\ce {Fe3Al2Si3O12}}} _{\text{Fe-Al garnet}}+\underbrace {{\ce {Ca3Al2Si3O12}}} _{\text{Ca-Al garnet}}+\underbrace {{\ce {KAl3Si3O10(OH)2}}} _{\text{muscovite}}\ {\ce {<=>}}\ \underbrace {{\ce {3CaAl2Si2O8}}} _{\text{plagioclase}}+\underbrace {{\ce {KFe3AlSi3O10(OH)2}}} _{\text{biotite}}}}

Since mineral assemblages at equilibrium are dependent on pressures and temperatures, by measuring the composition of the coexisting minerals, together with using suitable activity models, the P-T conditions experienced by the rock can be determined.^[1]

After one equilibrium constant is found, a line would be plotted on the P-T diagram.^{[ citation needed ]} As different equilibrium constants of mineral assemblages would occur as lines with different slopes in the P-T diagram, therefore, by finding the intersection of at least two lines in the P-T diagram, the P-T condition of the specimen can be obtained.^[1]

Despite the usefulness of geothermobarometry, special attention should be paid to whether the mineral assemblages represent an equilibrium, any occurrence of retrograde equilibrium in the rock, and appropriateness of calibration of the results.^[1]

Elastic thermobarometry is a method of determining the equilibrium pressure and temperature attained by the host mineral and its inclusion on the rock history from the excess pressures exhibited by mineral inclusions trapped inside host minerals. Upon exhumation and cooling, contrasting compressibilities and thermal expansivities induce differential strains (volume mismatches) between a host crystal and its inclusions. These strains can be quantified in situ using Raman spectroscopy or X-ray diffraction. Knowing equations of state and elastic properties of minerals, elastic thermobarometry inverts measured strains to calculate the pressure-temperature conditions under which the stress state was uniform in the host and inclusion.^[6] These are commonly interpreted to represent the conditions of inclusion entrapment or the last elastic equilibration of the pair.

Data on the geothermometers and geobarometers is derived from both laboratory studies on synthetic (artificial) mineral assemblages and from natural systems for which other constraints are available.

For example, one of the best known and most widely applicable geothermometers is the garnet-biotite relationship where the relative proportions of Fe and Mg in garnet and biotite change with increasing temperature, so measurement of the compositions of these minerals to give the Fe-Mg distribution between them allows the temperature of crystallization to be calculated, given some assumptions.

Assumptions in thermodynamic thermobarometry

In natural systems, the chemical reactions occur in open systems with unknown geological and chemical histories, and application of geothermobarometers relies on several assumptions that must hold in order for the laboratory data and natural compositions to relate in a valid fashion:

That the full mineralogical assemblage required for the thermobarometer is present. If not all of the minerals of the reaction are present, or did not equilibrate with each other simultaneously, then any pressures and temperatures calculated for the ideal reaction will deviate from those actually experienced by the rock.
That chemical equilibrium was achieved to a satisfactory degree. This could be impossible to demonstrate definitively, if the minerals of the thermobarometer assemblage are not all observed in contact with each other.
That any minerals in a two-mineral barometer or thermometer grew in equilibrium, which is assumed when the minerals are seen to be in contact.
That the mineral assemblage has not been altered by retrograde metamorphism, which can be assessed using an optical microscope in most cases.
That certain mineralogical assemblages are present. Without these, the accuracy of a reading may be altered from an ideal, and there may be more error inherent in the measurement.
That minerals present in thin section are in the same solid solution state as in the model. Many minerals such as feldspars and augite have a range of solid solution variations. Each variation can effect the model and the way a rock is metamorphosed over time.

Assumptions in elastic thermobarometry

In natural systems elastic behaviour of minerals can be easily perturbed by high temperature re-equilibration, plastic or brittle deformation, leading to an irreversible change beyond the elastic regime that will prevent reconstructing the "elastic history" of the pair.

The major assumption behind elastic geobarometry is that the host and the inclusion have experience initially the same pressure and that deformation of the host-inclusion system is elastic, hence reversible, and can therefore be inverted to obtain the entrapment pressure of the inclusion.^[9]
The shape of the inclusion is assumed to be spherical but calculations for non-spherical shapes are available^[10]
For several host-inclusion pairs the elastic properties for the host and the inclusion are assumed to be isotropic. For some pairs anisotropic solutions are available (e.g. quartz in garnet, zircon in garnet)^[11]^[12]
Simple calculation methods assume linear elasticity

Techniques

Some techniques include:

Geothermometers

Ti saturation content of biotite mica.^[13]
Fe-Mg exchange between garnet-biotite and garnet-amphibole.
Mg-Fe systematics in pigeonites and augites ^[14]
Zr content of rutile, effective for higher temperatures than the Ti-in-biotite thermometer. Requires quartz, rutile, and zircon to be equilibrated.^[15]
Ti-in-zircon crystallization thermometer

Note that the Fe-Mg exchange thermometers are empirical (laboratory tested and calibrated) as well as calculated based on a theoretical thermodynamic understanding of the components and phases involved. The Ti-in-biotite thermometer is solely empirical and not well understood thermodynamically.

Geobarometers

GASP; an acronym for the assemblage garnet-(Al₂SiO₅)-silica(quartz)-plagioclase
GPMB; an acronym for the assemblage garnet-plagioclase-muscovite-biotite
Garnet-plagioclase-hornblende-quartz.^[16]^[17]
Hornblende ^[18]^[19]^[20]

Various mineral assemblages rely more upon pressure than temperature; for example reactions which involve a large volume change. At high pressure, specific minerals assume lower volumes (therefore density increases, as the mass does not change) - it is these minerals which are good indicators of paleo-pressure.

Software

Software for "classic" thermobarometry includes:

THERMO-CALC softwarewas founded in 1997, but it all started much before that, as early as the mid-1970s, in fact. The place was the department for physical metallurgy at the Royal Institute of Technology (KTH) in Stockholm, Sweden, where Mats Hillert was a professor. Three of his graduate students at this time were, Bo Sundman, Bo Jansso and John Ågren. Thermo-calc is a software used by materials scientists and engineers to generate material properties data, gain insights about materials, understand a specific observation, and answer direct questions related to a specific material and/or its processing. Used in conjunction with suitable databases, Thermo-Calc can be used for a wide variety of applications.

THERMOCALC^[21]^[22] developed by Tim Holland and Roger Powell calculates model phase equilibria involving the HPx-eos and/or individual end-members from the Holland & Powell dataset.
Perple_X,^[23]^[24]^[25]^[26]^[27] originally developed by James A.D. Connolly is a collection of fortran programs for calculating and displaying petrologic phase equilibria
XMapTools ^[28] orioginally developed by Pierre Lanari is an advanced analysis software for quantitative chemical analysis of solids in 1D, 2D and 3D. It provides numerical tools and packages implemented in a guided and versatile environment that allows you to explore and visualise data in your own way. For example, XMapTools includes a wide range of data processing options including routines for classification, segmentation, calibration and visualisation via single and multi-channel maps or via binary, ternary and spider diagrams. Now it includes Bingo Antidote.
Bingo-Antidote is a petrological software originally developed by Pierre Lanari and Erik Duesterhoeft that offers an alternative modelling strategy based on iterative thermodynamic models integrated with quantitative compositional mapping. The latter is distributed as an XMapTools add-on and comes with a redesigned graphical user interface and improved features.

Software for elastic thermobarometry includes:

EntraPT ^[29] originally developed by Mattia L. Mazzucchelli, Ross J. Angel and Matteo Alvaro is a web application for elastic geobarometry. It is designed to make elastic thermobarometry easier. You can graphically analyze the residual strains of your inclusions and estimate their entrapment conditions, all in one place. It makes also easy to export, reuse, share and compare your data.
Strainman ^[30] originally developed by Ross J. Angel, Mara Murri, Boriana Mihailova and Matteo Alvaro is computer program for Windows for calculating strains from changes in Raman (or other phonon) mode wavenumbers, and vice-versa.
EosFit ^[31] is a software suite for calculations involving both thermal expansion and equations of state which now includes five major components to perform EoS calculations both with (EosFit7GUI)^[32] and without (EosFit7c)^[31] graphic user interface and perform host-inclusion calculations (Eosfit7-Pinc^[33]) with non-linear elasticity. Eosfit uses cfml_eos a validated set of Fortran modules that can be ‘used’ (in the Fortran sense) to easily write programs that can read, manipulate and fit EoS data, and perform related calculations for EoS.

Clinopyroxene thermobarometry

The mineral clinopyroxene is used for temperature and pressure calculations of the magma that produced igneous rock containing this mineral.

Related Research Articles

Biotite is a common group of phyllosilicate minerals within the mica group, with the approximate chemical formula K(Mg,Fe)₃AlSi₃O₁₀(F,OH)₂. It is primarily a solid-solution series between the iron-endmember annite, and the magnesium-endmember phlogopite; more aluminous end-members include siderophyllite and eastonite. Biotite was regarded as a mineral species by the International Mineralogical Association until 1998, when its status was changed to a mineral group. The term biotite is still used to describe unanalysed dark micas in the field. Biotite was named by J.F.L. Hausmann in 1847 in honor of the French physicist Jean-Baptiste Biot, who performed early research into the many optical properties of mica.

Metamorphism is the transformation of existing rock to rock with a different mineral composition or texture. Metamorphism takes place at temperatures in excess of 150 °C (300 °F), and often also at elevated pressure or in the presence of chemically active fluids, but the rock remains mostly solid during the transformation. Metamorphism is distinct from weathering or diagenesis, which are changes that take place at or just beneath Earth's surface.

Amphibolite is a metamorphic rock that contains amphibole, especially hornblende and actinolite, as well as plagioclase feldspar, but with little or no quartz. It is typically dark-colored and dense, with a weakly foliated or schistose (flaky) structure. The small flakes of black and white in the rock often give it a salt-and-pepper appearance.

Granulites are a class of high-grade metamorphic rocks of the granulite facies that have experienced high-temperature and moderate-pressure metamorphism. They are medium to coarse–grained and mainly composed of feldspars sometimes associated with quartz and anhydrous ferromagnesian minerals, with granoblastic texture and gneissose to massive structure. They are of particular interest to geologists because many granulites represent samples of the deep continental crust. Some granulites experienced decompression from deep in the Earth to shallower crustal levels at high temperature; others cooled while remaining at depth in the Earth.

<span class="mw-page-title-main">Hornfels</span>

Hornfels is the group name for a set of contact metamorphic rocks that have been baked and hardened by the heat of intrusive igneous masses and have been rendered massive, hard, splintery, and in some cases exceedingly tough and durable. These properties are caused by fine grained non-aligned crystals with platy or prismatic habits, characteristic of metamorphism at high temperature but without accompanying deformation. The term is derived from the German word Hornfels, meaning "hornstone", because of its exceptional toughness and texture both reminiscent of animal horns. These rocks were referred to by miners in northern England as whetstones.

<span class="mw-page-title-main">Chlorite group</span> Type of mineral

The chlorites are the group of phyllosilicate minerals common in low-grade metamorphic rocks and in altered igneous rocks. Greenschist, formed by metamorphism of basalt or other low-silica volcanic rock, typically contains significant amounts of chlorite.

Greenschists are metamorphic rocks that formed under the lowest temperatures and pressures usually produced by regional metamorphism, typically 300–450 °C (570–840 °F) and 2–10 kilobars (29,000–145,000 psi). Greenschists commonly have an abundance of green minerals such as chlorite, serpentine, and epidote, and platy minerals such as muscovite and platy serpentine. The platiness gives the rock schistosity. Other common minerals include quartz, orthoclase, talc, carbonate minerals and amphibole (actinolite).

Omphacite is a member of the clinopyroxene group of silicate minerals with formula: (Ca, Na)(Mg, Fe²⁺, Al)Si₂O₆. It is a variably deep to pale green or nearly colorless variety of clinopyroxene. It normally appears in eclogite, which is the high-pressure metamorphic rock of basalt. Omphacite is the solid solution of Fe-bearing diopside and jadeite. It crystallizes in the monoclinic system with prismatic, typically twinned forms, though usually anhedral. Its space group can be P2/n or C2/c depending on the thermal history. It exhibits the typical near 90° pyroxene cleavage. It is brittle with specific gravity of 3.29 to 3.39 and a Mohs hardness of 5 to 6.

Restite is the residual material left at the site of melting during the in place production of magma.

An index mineral is used in geology to determine the degree of metamorphism a rock has experienced. Depending on the original composition of and the pressure and temperature experienced by the protolith, chemical reactions between minerals in the solid state produce new minerals. When an index mineral is found in a metamorphosed rock, it indicates the minimum pressure and temperature the protolith must have achieved in order for that mineral to form. The higher the pressure and temperature in which the rock formed, the higher the grade of the rock.

A metamorphic facies is a set of mineral assemblages in metamorphic rocks formed under similar pressures and temperatures. The assemblage is typical of what is formed in conditions corresponding to an area on the two dimensional graph of temperature vs. pressure. Rocks which contain certain minerals can therefore be linked to certain tectonic settings, times and places in the geological history of the area. The boundaries between facies are wide because they are gradational and approximate. The area on the graph corresponding to rock formation at the lowest values of temperature and pressure is the range of formation of sedimentary rocks, as opposed to metamorphic rocks, in a process called diagenesis.

In geology ultrahigh-temperature metamorphism (UHT) is extreme crustal metamorphism with metamorphic temperatures exceeding 900 °C. Granulite-facies rocks metamorphosed at very high temperatures were identified in the early 1980s, although it took another decade for the geoscience community to recognize UHT metamorphism as a common regional phenomenon. Petrological evidence based on characteristic mineral assemblages backed by experimental and thermodynamic relations demonstrated that Earth's crust can attain and withstand very high temperatures (900–1000 °C) with or without partial melting.

Clinopyroxene thermobarometry is a scientific method that uses the mineral clinopyroxene to determine the temperature and pressure of the magma when the mineral crystalized. Clinopyroxene is found in many igneous rocks, so the method can be used to determine information about the entire rock. Many different minerals can be used for geothermobarometry, but clinopyroxene is especially useful because it's a common phenocryst in igneous rocks and easy to identify, and the crystallization of jadeite, a type of clinopyroxene, implies a growth in molar volume, making it a good indicator of pressure.

Timothy John Barrington Holland is a petrologist and Emeritus Professor in the Department of Earth Sciences at the University of Cambridge.

Roger Powell FRS, is a British-born Australian based educator and academic. He is Emeritus professor in the School of Geography, Earth and Atmospheric Sciences at the University of Melbourne.

The Pressure-Temperature-time path is a record of the pressure and temperature (P-T) conditions that a rock experienced in a metamorphic cycle from burial and heating to uplift and exhumation to the surface. Metamorphism is a dynamic process which involves the changes in minerals and textures of the pre-existing rocks (protoliths) under different P-T conditions in solid state. The changes in pressures and temperatures with time experienced by the metamorphic rocks are often investigated by petrological methods, radiometric dating techniques and thermodynamic modeling.

A petrogenetic grid is a geological phase diagram that connects the stability ranges or metastability ranges of metamorphic minerals or mineral assemblages to the conditions of metamorphism. Experimentally determined mineral or mineral-assemblage stability ranges are plotted as metamorphic reaction boundaries in a pressure–temperature cartesian coordinate system to produce a petrogenetic grid for a particular rock composition. The regions of overlap of the stability fields of minerals form equilibrium mineral assemblages used to determine the pressure–temperature conditions of metamorphism. This is particularly useful in geothermobarometry.

Garnet-Biotite Geothermometry is a method used to evaluate the peak temperature at which metamorphic rocks have formed. Geothermometry makes up one component of geothermobarometry, which also includes the evaluation of pressure (geobarometry). There are many geothermometers, but garnet-biotite is particularly useful because of the frequent occurrence of biotite and garnet together in medium grade metamorphic rocks. The garnet biotite thermometer correlates temperature with the partitioning of Fe and Mg in coinciding garnet and biotite. The garnet-biotite thermometer has been "calibrated" many times since the 70's by both experimental and empirical methods, however Ferry and Spear's 1978 experimental calibration study is reported thoroughly and commonly cited. Given a rock containing both garnet and biotite, an equilibrium constant (K_D) can be found simply by using microprobe analysis. Then, by comparing the found K_D value to the calculated garnet-biotite geothermometer, the peak temperature of rock formation can be determined.

Gore Mountain Garnet, found in the Adirondack Mountains in New York, contains the world's largest garnets. The rock that holds these garnets, garnet amphibolite, is sometimes referred to as 'black ore' or 'dark ore.' This rock formation formed during metamorphism during the Ottawan phase of the Grenvillian orogeny, and extremely high temperatures combined with introduction of fluids is what most likely contributed to the unusual size of the megacrystic garnets.

In metamorphic geology, a compatibility diagram shows how the mineral assemblage of a metamorphic rock in thermodynamic equilibrium varies with composition at a fixed temperature and pressure. Compatibility diagrams provide an excellent way to analyze how variations in the rock's composition affect the mineral paragenesis that develops in a rock at particular pressure and temperature conditions. Because of the difficulty of depicting more than three components, usually only the three most important components are plotted, though occasionally a compatibility diagram for four components is plotted as a projected tetrahedron.

References

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↑ Goncalves, Philippe; Marquer, Didier; Oliot, Emilien; Durand, Cyril (2013), "Thermodynamic Modeling and Thermobarometry of Metasomatized Rocks", Metasomatism and the Chemical Transformation of Rock, Berlin, Heidelberg: Springer Berlin Heidelberg, pp. 53–91, doi:10.1007/978-3-642-28394-9_3, ISBN 978-3-642-28393-2 , retrieved 2023-07-31
↑ Wood, B.J.; Holland, T.J.B.; Newton, R.C.; Kleppa, O.J. (September 1980). "Thermochemistry of jadeite—diopside pyroxenes". Geochimica et Cosmochimica Acta. 44 (9): 1363–1371. Bibcode:1980GeCoA..44.1363W. doi:10.1016/0016-7037(80)90095-2.
↑ Holland, Heinrich D.; Turekian, Karl K. (2004). Treatise on geochemistry (1st ed.). Amsterdam Boston: Elsevier/Pergamon. ISBN 978-0-08-043751-4.
↑ Ghose, S.; Ganguly, J. (1982), Saxena, Surendra K. (ed.), "Mg-Fe Order-Disorder in Ferromagnesian Silicates", Advances in Physical Geochemistry, New York, NY: Springer New York, vol. 2, pp. 3–99, doi:10.1007/978-1-4612-5683-0_1, ISBN 978-1-4612-5685-4 , retrieved 2023-07-31
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↑ Levresse, Gilles; Cervantes-de la Cruz, Karina Elizabeth; Aranda-Gómez, José Jorge; Dávalos-Elizondo, María Guadalupe; Jiménez-Sandoval, Sergio; Rodríguez-Melgarejo, Francisco; Alba-Aldave, Leticia Araceli (January 2016). "CO2 fluid inclusion barometry in mantle xenoliths from central Mexico: A detailed record of magma ascent". Journal of Volcanology and Geothermal Research. 310: 72–88. doi:10.1016/j.jvolgeores.2015.11.012.
↑ Powell, Roger; Holland, Tim (1994). "Optimal geothermometry and geobarometry". American Mineralogist. 79: 120–133.
↑ Moulas, Evangelos; Kostopoulos, Dimitrios; Podladchikov, Yury; Chatzitheodoridis, Elias; Schenker, Filippo L.; Zingerman, Konstantin M.; Pomonis, Panagiotis; Tajčmanová, Lucie (2020-12-15). "Calculating pressure with elastic geobarometry: A comparison of different elastic solutions with application to a calc-silicate gneiss from the Rhodope Metamorphic Province". Lithos. 378–379: 105803. Bibcode:2020Litho.37805803M. doi:10.1016/j.lithos.2020.105803. ISSN 0024-4937. S2CID 224846463.
↑ Mazzucchelli, M.L.; Burnley, P.; Angel, R.J.; Morganti, S.; Domeneghetti, M.C.; Nestola, F.; Alvaro, M. (2018). "Elastic geothermobarometry: Corrections for the geometry of the host-inclusion system". Geology. 46 (3): 231–234. Bibcode:2018Geo....46..231M. doi: 10.1130/g39807.1 . Retrieved 2023-08-01.
↑ Mazzucchelli, M. L.; Reali, A.; Morganti, S.; Angel, R. J.; Alvaro, M. (2019-12-15). "Elastic geobarometry for anisotropic inclusions in cubic hosts". Lithos. 350–351: 105218. Bibcode:2019Litho.35005218M. doi: 10.1016/j.lithos.2019.105218 . ISSN 0024-4937.
↑ Murri, Mara; Mazzucchelli, Mattia L.; Campomenosi, Nicola; Korsakov, Andrey V.; Prencipe, Mauro; Mihailova, Boriana D.; Scambelluri, Marco; Angel, Ross J.; Alvaro, Matteo (2018-11-01). "Raman elastic geobarometry for anisotropic mineral inclusions". American Mineralogist. 103 (11): 1869–1872. doi:10.2138/am-2018-6625CCBY. hdl: 11567/919890 . ISSN 1945-3027.
↑ http://www.geol.lsu.edu/henry/Research/biotite/TiInBiotiteGeothermometer.htm Archived 2018-04-04 at the Wayback Machine Ti-in biotite geothermometer, Henry et al. 2005
↑ Lindsley & Andersen 1983 - A Two-pyroxene Thermometer; Journal of Geophysical Research, vol. 88
↑ http://www.rpi.edu/~watsoe/research/Watson_etal_CMP06.pdf Crystallization thermometers for zircon and rutile, Watson et al. 2006; Contributions to mineralogy and petrology v. 151
↑ Kohn, M.J. and Spear, F.S. (1989): Am. Min. 74:77-84. (Pargasite component)
↑ Kohn, M.J. and Spear, F.S. (1990): Am. Min. 75:89-96. (Tschermakite component)
↑ Hammerstrom, J.M. and Zen, E.-an. (1986): Am. Min. 71:1297-1313.
↑ Hollister, L.S., Grissom, G.C., Peters, E.K., Stowell, H.H. and Sisson, V.B.(1987): Am. Mineral. 72:231-239.
↑ Johnson, and Rutherford (1989): Geology 17: 837-841.
↑ Holland, T. J. B.; Powell, R. (2004-10-08). "An internally consistent thermodynamic data set for phases of petrological interest: AN INTERNALLY CONSISTENT THERMODYNAMIC DATA SET". Journal of Metamorphic Geology. 16 (3): 309–343. doi:10.1111/j.1525-1314.1998.00140.x.
↑ Powell, R; Holland, T.; Worley, B. (June 1998). "Calculating phase diagrams involving solid solutions via non-linear equations, with examples using THERMOCALC". Journal of Metamorphic Geology. 16 (4): 577–588. Bibcode:1998JMetG..16..577P. doi:10.1111/j.1525-1314.1998.00157.x. ISSN 0263-4929. S2CID 129301254.
↑ Connolly, J. a. D. (1990-06-01). "Multivariable phase diagrams; an algorithm based on generalized thermodynamics". American Journal of Science. 290 (6): 666–718. Bibcode:1990AmJS..290..666C. doi:10.2475/ajs.290.6.666.
↑ Connolly, J.A.D. (July 2005). "Computation of phase equilibria by linear programming: A tool for geodynamic modeling and its application to subduction zone decarbonation". Earth and Planetary Science Letters. 236 (1–2): 524–541. Bibcode:2005E&PSL.236..524C. doi:10.1016/j.epsl.2005.04.033.
↑ Connolly, James A. D.; Galvez, Matthieu E. (2018-11-01). "Electrolytic fluid speciation by Gibbs energy minimization and implications for subduction zone mass transfer". Earth and Planetary Science Letters. 501: 90–102. Bibcode:2018E&PSL.501...90C. doi:10.1016/j.epsl.2018.08.024. ISSN 0012-821X. S2CID 134999977.
↑ Connolly, J. A. D.; Petrini, K. (September 2002). "An automated strategy for calculation of phase diagram sections and retrieval of rock properties as a function of physical conditions". Journal of Metamorphic Geology. 20 (7): 697–708. Bibcode:2002JMetG..20..697C. doi:10.1046/j.1525-1314.2002.00398.x. ISSN 0263-4929. S2CID 73603565.
↑ Connolly, J. A. D.; Kerrick, D. M. (1987-01-01). "An algorithm and computer program for calculating composition phase diagrams". Calphad. 11 (1): 1–55. doi:10.1016/0364-5916(87)90018-6. ISSN 0364-5916.
↑ Lanari, Pierre; Vidal, Olivier; De Andrade, Vincent; Dubacq, Benoît; Lewin, Eric; Grosch, Eugene G.; Schwartz, Stéphane (2014-01-01). "XMapTools: A MATLAB©-based program for electron microprobe X-ray image processing and geothermobarometry". Computers & Geosciences. 62: 227–240. doi:10.1016/j.cageo.2013.08.010. ISSN 0098-3004.
↑ Mazzucchelli, Mattia Luca; Angel, Ross John; Alvaro, Matteo (2021). "EntraPT: An online platform for elastic geothermobarometry". American Mineralogist. 106 (5): 830–837. Bibcode:2021AmMin.106..830M. doi: 10.2138/am-2021-7693ccbyncnd . Retrieved 2023-08-01.
↑ Angel, Ross J.; Murri, Mara; Mihailova, Boriana; Alvaro, Matteo (2019-02-01). "Stress, strain and Raman shifts". Zeitschrift für Kristallographie - Crystalline Materials. 234 (2): 129–140. doi:10.1515/zkri-2018-2112. ISSN 2196-7105. S2CID 105926659.
1 2 Angel, Ross J.; Alvaro, Matteo; Gonzalez-Platas, Javier (2014-05-01). "EosFit7c and a Fortran module (library) for equation of state calculations". Zeitschrift für Kristallographie - Crystalline Materials (in German). 229 (5): 405–419. doi:10.1515/zkri-2013-1711. ISSN 2196-7105. S2CID 56434995.
↑ Gonzalez-Platas, J.; Alvaro, M.; Nestola, F.; Angel, R. (2016-08-01). "EosFit7-GUI: a new graphical user interface for equation of state calculations, analyses and teaching". Journal of Applied Crystallography. 49 (4): 1377–1382. doi:10.1107/S1600576716008050. ISSN 1600-5767.
↑ Angel, Ross J.; Mazzucchelli, Mattia L.; Alvaro, Matteo; Nestola, Fabrizio (2017-09-01). "EosFit-Pinc: A simple GUI for host-inclusion elastic thermobarometry". American Mineralogist. 102 (9): 1957–1960. Bibcode:2017AmMin.102.1957A. doi:10.2138/am-2017-6190. ISSN 1945-3027.

Winter, D.John.Thermodynamics of metamorphic reactions: Geothermobarometry, 543-556
Henry, D. J., Guidotti, C. V. and Thomson, J. A. (2005) The Ti-saturation surface for low-to-medium pressure metapelitic biotite: Implications for Geothermometry and Ti-substitution Mechanisms. American Mineralogist, 90, 316-328.
Guidotti, C. V., Cheney, J. T. and Henry, D. J. (1988) Compositional variation of biotite as a function of metamorphic reactions and mineral assemblage in the pelitic schists of western Maine: American Journal of Science-Wones Memorial Volume, v. 288A, 270-292.

External links

Thermo-Calc Software - this can be purchased online with a range of databases however there is also a free Educational Package on their website https://thermocalc.com/academia/free-educational-package/
THERMOCALC (Holland & Powell) - currently free to download online for everyone with a range of databases available. See the download guide at: https://hpxeosandthermocalc.org/the-thermocalc-software/thermocalc-get-started/thermocalc-download-guide/

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[:0-1] 1 2 3 4 5 6 Powell, R.; Holland, T. J. B. (February 2008). "On thermobarometry". Journal of Metamorphic Geology. 26 (2): 155–179. Bibcode:2008JMetG..26..155P. doi:10.1111/j.1525-1314.2007.00756.x. ISSN 0263-4929.

[2] Goncalves, Philippe; Marquer, Didier; Oliot, Emilien; Durand, Cyril (2013), "Thermodynamic Modeling and Thermobarometry of Metasomatized Rocks", Metasomatism and the Chemical Transformation of Rock, Berlin, Heidelberg: Springer Berlin Heidelberg, pp. 53–91, doi:10.1007/978-3-642-28394-9_3, ISBN 978-3-642-28393-2 , retrieved 2023-07-31

[3] Wood, B.J.; Holland, T.J.B.; Newton, R.C.; Kleppa, O.J. (September 1980). "Thermochemistry of jadeite—diopside pyroxenes". Geochimica et Cosmochimica Acta. 44 (9): 1363–1371. Bibcode:1980GeCoA..44.1363W. doi:10.1016/0016-7037(80)90095-2.

[4] Holland, Heinrich D.; Turekian, Karl K. (2004). Treatise on geochemistry (1st ed.). Amsterdam Boston: Elsevier/Pergamon. ISBN 978-0-08-043751-4.

[5] Ghose, S.; Ganguly, J. (1982), Saxena, Surendra K. (ed.), "Mg-Fe Order-Disorder in Ferromagnesian Silicates", Advances in Physical Geochemistry, New York, NY: Springer New York, vol. 2, pp. 3–99, doi:10.1007/978-1-4612-5683-0_1, ISBN 978-1-4612-5685-4 , retrieved 2023-07-31

[:1-6] 1 2 Kohn, Matthew J.; Mazzucchelli, Mattia L.; Alvaro, Matteo (2023-05-30). "Elastic Thermobarometry". Annual Review of Earth and Planetary Sciences. 51 (1): 331–366. Bibcode:2023AREPS..51..331K. doi:10.1146/annurev-earth-031621-112720. ISSN 0084-6597. S2CID 256443282.

[7] Levresse, Gilles; Cervantes-de la Cruz, Karina Elizabeth; Aranda-Gómez, José Jorge; Dávalos-Elizondo, María Guadalupe; Jiménez-Sandoval, Sergio; Rodríguez-Melgarejo, Francisco; Alba-Aldave, Leticia Araceli (January 2016). "CO2 fluid inclusion barometry in mantle xenoliths from central Mexico: A detailed record of magma ascent". Journal of Volcanology and Geothermal Research. 310: 72–88. doi:10.1016/j.jvolgeores.2015.11.012.

[8] Powell, Roger; Holland, Tim (1994). "Optimal geothermometry and geobarometry". American Mineralogist. 79: 120–133.

[9] Moulas, Evangelos; Kostopoulos, Dimitrios; Podladchikov, Yury; Chatzitheodoridis, Elias; Schenker, Filippo L.; Zingerman, Konstantin M.; Pomonis, Panagiotis; Tajčmanová, Lucie (2020-12-15). "Calculating pressure with elastic geobarometry: A comparison of different elastic solutions with application to a calc-silicate gneiss from the Rhodope Metamorphic Province". Lithos. 378–379: 105803. Bibcode:2020Litho.37805803M. doi:10.1016/j.lithos.2020.105803. ISSN 0024-4937. S2CID 224846463.

[10] Mazzucchelli, M.L.; Burnley, P.; Angel, R.J.; Morganti, S.; Domeneghetti, M.C.; Nestola, F.; Alvaro, M. (2018). "Elastic geothermobarometry: Corrections for the geometry of the host-inclusion system". Geology. 46 (3): 231–234. Bibcode:2018Geo....46..231M. doi: 10.1130/g39807.1 . Retrieved 2023-08-01.

[11] Mazzucchelli, M. L.; Reali, A.; Morganti, S.; Angel, R. J.; Alvaro, M. (2019-12-15). "Elastic geobarometry for anisotropic inclusions in cubic hosts". Lithos. 350–351: 105218. Bibcode:2019Litho.35005218M. doi: 10.1016/j.lithos.2019.105218 . ISSN 0024-4937.

[12] Murri, Mara; Mazzucchelli, Mattia L.; Campomenosi, Nicola; Korsakov, Andrey V.; Prencipe, Mauro; Mihailova, Boriana D.; Scambelluri, Marco; Angel, Ross J.; Alvaro, Matteo (2018-11-01). "Raman elastic geobarometry for anisotropic mineral inclusions". American Mineralogist. 103 (11): 1869–1872. doi:10.2138/am-2018-6625CCBY. hdl: 11567/919890 . ISSN 1945-3027.

[13] ttp://www.geol.lsu.edu/henry/Research/biotite/TiInBiotiteGeothermometer.htm Archived 2018-04-04 at the Wayback Machine Ti-in biotite geothermometer, Henry et al. 2005

[14] Lindsley & Andersen 1983 - A Two-pyroxene Thermometer; Journal of Geophysical Research, vol. 88

[15] ttp://www.rpi.edu/~watsoe/research/Watson_etal_CMP06.pdf Crystallization thermometers for zircon and rutile, Watson et al. 2006; Contributions to mineralogy and petrology v. 151

[16] Kohn, M.J. and Spear, F.S. (1989): Am. Min. 74:77-84. (Pargasite component)

[17] Kohn, M.J. and Spear, F.S. (1990): Am. Min. 75:89-96. (Tschermakite component)

[18] Hammerstrom, J.M. and Zen, E.-an. (1986): Am. Min. 71:1297-1313.

[19] Hollister, L.S., Grissom, G.C., Peters, E.K., Stowell, H.H. and Sisson, V.B.(1987): Am. Mineral. 72:231-239.

[20] Johnson, and Rutherford (1989): Geology 17: 837-841.

[21] Holland, T. J. B.; Powell, R. (2004-10-08). "An internally consistent thermodynamic data set for phases of petrological interest: AN INTERNALLY CONSISTENT THERMODYNAMIC DATA SET". Journal of Metamorphic Geology. 16 (3): 309–343. doi:10.1111/j.1525-1314.1998.00140.x.

[22] Powell, R; Holland, T.; Worley, B. (June 1998). "Calculating phase diagrams involving solid solutions via non-linear equations, with examples using THERMOCALC". Journal of Metamorphic Geology. 16 (4): 577–588. Bibcode:1998JMetG..16..577P. doi:10.1111/j.1525-1314.1998.00157.x. ISSN 0263-4929. S2CID 129301254.

[23] Connolly, J. a. D. (1990-06-01). "Multivariable phase diagrams; an algorithm based on generalized thermodynamics". American Journal of Science. 290 (6): 666–718. Bibcode:1990AmJS..290..666C. doi:10.2475/ajs.290.6.666.

[24] Connolly, J.A.D. (July 2005). "Computation of phase equilibria by linear programming: A tool for geodynamic modeling and its application to subduction zone decarbonation". Earth and Planetary Science Letters. 236 (1–2): 524–541. Bibcode:2005E&PSL.236..524C. doi:10.1016/j.epsl.2005.04.033.

[25] Connolly, James A. D.; Galvez, Matthieu E. (2018-11-01). "Electrolytic fluid speciation by Gibbs energy minimization and implications for subduction zone mass transfer". Earth and Planetary Science Letters. 501: 90–102. Bibcode:2018E&PSL.501...90C. doi:10.1016/j.epsl.2018.08.024. ISSN 0012-821X. S2CID 134999977.

[26] Connolly, J. A. D.; Petrini, K. (September 2002). "An automated strategy for calculation of phase diagram sections and retrieval of rock properties as a function of physical conditions". Journal of Metamorphic Geology. 20 (7): 697–708. Bibcode:2002JMetG..20..697C. doi:10.1046/j.1525-1314.2002.00398.x. ISSN 0263-4929. S2CID 73603565.

[27] Connolly, J. A. D.; Kerrick, D. M. (1987-01-01). "An algorithm and computer program for calculating composition phase diagrams". Calphad. 11 (1): 1–55. doi:10.1016/0364-5916(87)90018-6. ISSN 0364-5916.

[28] Lanari, Pierre; Vidal, Olivier; De Andrade, Vincent; Dubacq, Benoît; Lewin, Eric; Grosch, Eugene G.; Schwartz, Stéphane (2014-01-01). "XMapTools: A MATLAB©-based program for electron microprobe X-ray image processing and geothermobarometry". Computers & Geosciences. 62: 227–240. doi:10.1016/j.cageo.2013.08.010. ISSN 0098-3004.

[29] Mazzucchelli, Mattia Luca; Angel, Ross John; Alvaro, Matteo (2021). "EntraPT: An online platform for elastic geothermobarometry". American Mineralogist. 106 (5): 830–837. Bibcode:2021AmMin.106..830M. doi: 10.2138/am-2021-7693ccbyncnd . Retrieved 2023-08-01.

[30] Angel, Ross J.; Murri, Mara; Mihailova, Boriana; Alvaro, Matteo (2019-02-01). "Stress, strain and Raman shifts". Zeitschrift für Kristallographie - Crystalline Materials. 234 (2): 129–140. doi:10.1515/zkri-2018-2112. ISSN 2196-7105. S2CID 105926659.

[:2-31] 1 2 Angel, Ross J.; Alvaro, Matteo; Gonzalez-Platas, Javier (2014-05-01). "EosFit7c and a Fortran module (library) for equation of state calculations". Zeitschrift für Kristallographie - Crystalline Materials (in German). 229 (5): 405–419. doi:10.1515/zkri-2013-1711. ISSN 2196-7105. S2CID 56434995.

[32] Gonzalez-Platas, J.; Alvaro, M.; Nestola, F.; Angel, R. (2016-08-01). "EosFit7-GUI: a new graphical user interface for equation of state calculations, analyses and teaching". Journal of Applied Crystallography. 49 (4): 1377–1382. doi:10.1107/S1600576716008050. ISSN 1600-5767.

[33] Angel, Ross J.; Mazzucchelli, Mattia L.; Alvaro, Matteo; Nestola, Fabrizio (2017-09-01). "EosFit-Pinc: A simple GUI for host-inclusion elastic thermobarometry". American Mineralogist. 102 (9): 1957–1960. Bibcode:2017AmMin.102.1957A. doi:10.2138/am-2017-6190. ISSN 1945-3027.

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