Closure temperature: Difference between revisions
merged with '''blocking temperature''' |
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{{Short description|Temperature of a system, such as a mineral, at the time given by its radiometric date}} |
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{{About| radiometric dating| blocking temperature in a ferromagnet | Superparamagnetism}} |
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In [[radiometric dating]], '''closure temperature''' or '''blocking temperature''' refers to the temperature of a system, such as a [[mineral]], at the time given by its radiometric date. In physical terms, the closure temperature is the temperature at which a system has cooled so that there is no longer any significant diffusion of the parent or daughter [[isotopes]] out of the system and into the external environment.<ref name=Braun2006>{{cite book|last=Braun|first=Jean|title=Quantitative Thermochronology: Numerical Methods for the Interpretation of Thermochronological Data|url=https://archive.org/details/quantitativether00brau_487|url-access=limited|publisher=Cambridge University Press|location=Cambridge|isbn=978-0-521-83057-7|pages=[https://archive.org/details/quantitativether00brau_487/page/n37 24]–27|author2=Peter van der Beek |author3=Geoffrey Batt |year=2006}}<!--|accessdate=18 February 2012--></ref> The concept's initial mathematical formulation was presented in a seminal paper by [[Martin H. Dodson]], |
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| ⚫ | "Closure temperature in cooling geochronological and petrological systems" in the journal ''[[Contributions to Mineralogy and Petrology]]'', 1973, with refinements to a usable experimental formulation by other scientists in later years.<ref name=Braun2006 /> This temperature varies broadly among different minerals and also differs depending on the parent and daughter atoms being considered.<ref>''Earth: a Portrait of a Planet'' [http://www.wwnorton.com/college/geo/earth2/glossary/b.htm Glossary W.W. Norton & Company] {{webarchive|url=https://web.archive.org/web/20090108223738/http://www2.wwnorton.com/college/geo/earth2/glossary/b.htm |date=2009-01-08 }}</ref> It is specific to a particular material and isotopic system.<ref name=Rollinson>Rollinson, 1993. ''Using Geochemical Data: Evaluation, Presentation, Interpretation'' Longman Scientific & Technical. {{ISBN|978-0-582-06701-1}}</ref> |
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| ⚫ | The closure temperature of a system can be experimentally determined in the lab by [[Petrology#Branches|artificially resetting]] sample [[mineral]]s using a high-temperature furnace. As the mineral cools, the crystal structure begins to form and diffusion of [[isotope]]s slows. At a certain temperature, the crystal structure has formed sufficiently to prevent diffusion of isotopes. This temperature is what is known as blocking temperature and represents the temperature below which the mineral is a closed system to measurable diffusion of isotopes.<ref name=Rollinson/> The age that can be calculated by radiometric dating is thus the time at which the rock or mineral cooled to blocking temperature. |
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These temperatures can also be determined in the field by comparing them to the dates of other minerals with well-known closure temperatures. |
These temperatures can also be determined in the field by comparing them to the dates of other minerals with well-known closure temperatures. |
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== Table of values == |
== Table of values == |
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The following table represents the closure temperatures of some materials. These values are the approximate values of the closure temperatures of certain minerals listed by the isotopic system being used. These values are approximations; better values of the closure temperature require more precise calculations and characterizations of the diffusion characteristics of the mineral grain being studied. |
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The following are the closing temperatures of certain minerals grouped by the typical dating method with which they are used. |
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=== Potassium-argon method === |
=== [[K–Ar dating|Potassium-argon method]] === |
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| 280±40 |
| 280±40 |
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| [[Microcline]] |
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| 130±15 |
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=== [[Uranium–lead dating|Uranium-lead method]] === |
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! Mineral |
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! Closure temperature (°C)<ref>{{cite journal|doi=10.1130/G21010.1|title=Tempo of burial and exhumation within the deep roots of a magmatic arc, Fiordland, New Zealand|year=2005|author=Flowers, R.M.|journal=Geology|volume=33|pages=17|last2=Bowring|first2=S.A.|last3=Tulloch|first3=A.J.|last4=Klepeis|first4=K.A.|issue=1|bibcode = 2005Geo....33...17F }}</ref> |
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| [[Titanite]] |
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| 600-650 |
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| [[Rutile]] |
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| 400-450 |
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| [[Apatite]] |
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| 450-500 |
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| [[Zircon]] |
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| >1000 |
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| [[Monazite]] |
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| >1000 |
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=== [[Electron spin resonance dating]] === |
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! Mineral |
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! Closure temperature (°C) |
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| [[Quartz]] (of granite) |
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| ~30-90<ref>{{Cite journal |last1=Toyoda |first1=Shin |last2=Ikeya |first2=Motoji |date=1991 |title=Thermal stabilities of paramagnetic defect and impurity centers in quartz: Basis for ESR dating of thermal history. |journal=Geochemical Journal |volume=25 |issue=6 |pages=437–445 |doi=10.2343/geochemj.25.437 |bibcode=1991GeocJ..25..437T |issn=0016-7002|doi-access=free }}</ref> |
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| [[Baryte]] |
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| 190-340<ref>{{Cite journal |last1=Tsang |first1=Man-Yin |last2=Toyoda |first2=Shin |last3=Tomita |first3=Makiko |last4=Yamamoto |first4=Yuzuru |date=2022-08-01 |title=Thermal stability and closure temperature of barite for electron spin resonance dating |journal=Quaternary Geochronology |language=en |volume=71 |pages=101332 |doi=10.1016/j.quageo.2022.101332 |s2cid=248614826 |issn=1871-1014|doi-access=free |bibcode=2022QuGeo..7101332T }}</ref> |
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==References== |
==References== |
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[[Category:Radiometric dating]] |
[[Category:Radiometric dating]] |
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{{Radioactivity-stub}} |
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Latest revision as of 13:36, 28 June 2024
In radiometric dating, closure temperature or blocking temperature refers to the temperature of a system, such as a mineral, at the time given by its radiometric date. In physical terms, the closure temperature is the temperature at which a system has cooled so that there is no longer any significant diffusion of the parent or daughter isotopes out of the system and into the external environment.[1] The concept's initial mathematical formulation was presented in a seminal paper by Martin H. Dodson, "Closure temperature in cooling geochronological and petrological systems" in the journal Contributions to Mineralogy and Petrology, 1973, with refinements to a usable experimental formulation by other scientists in later years.[1] This temperature varies broadly among different minerals and also differs depending on the parent and daughter atoms being considered.[2] It is specific to a particular material and isotopic system.[3]
The closure temperature of a system can be experimentally determined in the lab by artificially resetting sample minerals using a high-temperature furnace. As the mineral cools, the crystal structure begins to form and diffusion of isotopes slows. At a certain temperature, the crystal structure has formed sufficiently to prevent diffusion of isotopes. This temperature is what is known as blocking temperature and represents the temperature below which the mineral is a closed system to measurable diffusion of isotopes.[3] The age that can be calculated by radiometric dating is thus the time at which the rock or mineral cooled to blocking temperature.
These temperatures can also be determined in the field by comparing them to the dates of other minerals with well-known closure temperatures.
Closure temperatures are used in geochronology and thermochronology to date events and determine rates of processes in the geologic past.
Table of values
[edit]The following table represents the closure temperatures of some materials. These values are the approximate values of the closure temperatures of certain minerals listed by the isotopic system being used. These values are approximations; better values of the closure temperature require more precise calculations and characterizations of the diffusion characteristics of the mineral grain being studied.
| Mineral | Closure temperature (°C) |
|---|---|
| Hornblende | 530±40 |
| Muscovite | ~350 |
| Biotite | 280±40 |
| Mineral | Closure temperature (°C)[4] |
|---|---|
| Titanite | 600-650 |
| Rutile | 400-450 |
| Apatite | 450-500 |
| Zircon | >1000 |
| Monazite | >1000 |
| Mineral | Closure temperature (°C) |
|---|---|
| Quartz (of granite) | ~30-90[5] |
| Baryte | 190-340[6] |
References
[edit]- ^ a b Braun, Jean; Peter van der Beek; Geoffrey Batt (2006). Quantitative Thermochronology: Numerical Methods for the Interpretation of Thermochronological Data. Cambridge: Cambridge University Press. pp. 24–27. ISBN 978-0-521-83057-7.
- ^ Earth: a Portrait of a Planet Glossary W.W. Norton & Company Archived 2009-01-08 at the Wayback Machine
- ^ a b Rollinson, 1993. Using Geochemical Data: Evaluation, Presentation, Interpretation Longman Scientific & Technical. ISBN 978-0-582-06701-1
- ^ Flowers, R.M.; Bowring, S.A.; Tulloch, A.J.; Klepeis, K.A. (2005). "Tempo of burial and exhumation within the deep roots of a magmatic arc, Fiordland, New Zealand". Geology. 33 (1): 17. Bibcode:2005Geo....33...17F. doi:10.1130/G21010.1.
- ^ Toyoda, Shin; Ikeya, Motoji (1991). "Thermal stabilities of paramagnetic defect and impurity centers in quartz: Basis for ESR dating of thermal history". Geochemical Journal. 25 (6): 437–445. Bibcode:1991GeocJ..25..437T. doi:10.2343/geochemj.25.437. ISSN 0016-7002.
- ^ Tsang, Man-Yin; Toyoda, Shin; Tomita, Makiko; Yamamoto, Yuzuru (2022-08-01). "Thermal stability and closure temperature of barite for electron spin resonance dating". Quaternary Geochronology. 71: 101332. Bibcode:2022QuGeo..7101332T. doi:10.1016/j.quageo.2022.101332. ISSN 1871-1014. S2CID 248614826.
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