View source for TEX86

{{DISPLAYTITLE:TEX<sub>86</sub>}}
[[File:Molecular structures and HPLC detection of GDGTs.jpg|thumb|Molecular structures and [[High-performance liquid chromatography|HPLC detection]] of GDGTs. Retrieved from Tierney and Tingley (2015).<ref>{{Cite journal |last=Tierney |first=Jessica E. |last2=Tingley |first2=Martin P. |date=2015-06-23 |title=A TEX86 surface sediment database and extended Bayesian calibration |url=https://www.nature.com/articles/sdata201529 |journal=Scientific Data |language=en |volume=2 |issue=1 |pages=150029 |doi=10.1038/sdata.2015.29 |issn=2052-4463|pmc=4477698 }}</ref>|433x433px]]

'''TEX<sub>86</sub>''' is an organic [[paleothermometer]] based upon the membrane lipids of [[mesophilic]] marine [[Nitrososphaerota]] (formerly "Thaumarchaeota", "Marine Group 1 [[TACK|Crenarchaeota]]").<ref>{{cite journal | last1 = Schouten | first1 = S. | last2 = Hopmans | first2 = E.C. | last3 = Schefuß | first3 = E. | last4 = Sinninghe Damste | first4 = J.S. | date = 2002 | title = Distributional variation in marine crenarchaeotal membrane lipids: a new tool for reconstructing ancient sea water temperatures? | journal = Earth and Planetary Science Letters | volume = 204 | issue = 1–2 | pages = 265–274 | doi = 10.1016/S0012-821X(02)00979-2| bibcode = 2002E&PSL.204..265S | s2cid = 54198843 }}</ref><ref>{{cite journal | last1 = Kim | first1 = J.-H. | first2 = S. | last2 = Schouten | first3 = E.C. | last3 = Hopmans | first4 = B. | last4 = Donner | first5 = J.S. | last5 = Sinninghe Damsté | date = 2008 | title = Global sediment core-top calibration of the TEX86 paleothermometer in the ocean | journal = Geochimica et Cosmochimica Acta | volume = 72 | issue = 4 | pages = 1154–1173 | doi = 10.1016/j.gca.2007.12.010| bibcode = 2008GeCoA..72.1154K }}</ref>

==Basics==
The membrane lipids of [[Nitrososphaerota]] are composed of [[glycerol dialkyl glycerol tetraethers]] (GDGTs) which contain 0-3 [[cyclopentane]] moieties (commonly annotated as GDGT-''n'' where ''n'' = numbers of cyclopentane moieties). Nitrososphaerota also synthesise crenarchaeol (cren) which contains four cyclopentane moieties and a single [[cyclohexane]] moiety and a regio-isomer (cren'). The cyclohexane and cyclopentane rings, formed by internal cyclisation of one of the [[biphytane]] chains,<ref>{{cite journal | last1 = Schouten | first1 = S. | last2 = Hopmans | first2 = E.C. | last3 = Sinninghe Damsté | first3 = J.S. | date = 2013 | title = The organic geochemistry of glycerol dialkyl glycerol tetraether lipids: A review | journal = Organic Geochemistry | volume = 54 | pages = 19–61 | doi = 10.1016/j.orggeochem.2012.09.006}}</ref> have a pronounced effect on the thermal transition points of the Nitrososphaerota cell membrane. Mesocosm studies demonstrate that the degree of cyclisation is generally governed by growth temperature.<ref>{{cite journal | last1 = Wuchter | first1 = C. | last2 = Schouten | first2 = S. | last3 = Coolen | first3 = M.J.L. | last4 = Sinninghe Damsté | first4 = J.S. | date = 2004 | title = Temperature-dependent variation in the distribution of tetraether membrane lipids of marine Crenarchaeota: Implications for TEX<sub>86</sub> paleothermometry | journal = Paleoceanography and Paleoclimatology | volume = 19 | number = 4 | page = PA4028 | doi = 10.1029/2004PA001041| bibcode = 2004PalOc..19.4028W | doi-access = free }}</ref>

==Calibrations==
Based upon the relative distribution of isoprenoidal GDGTs, Schouten et al. (2002)<ref>{{Cite journal |last=Schouten |first=Stefan |last2=Hopmans |first2=Ellen C. |last3=Schefuß |first3=Enno |last4=Sinninghe Damsté |first4=Jaap S. |date=2002-11-30 |title=Distributional variations in marine crenarchaeotal membrane lipids: a new tool for reconstructing ancient sea water temperatures? |url=https://www.sciencedirect.com/science/article/pii/S0012821X02009792 |journal=Earth and Planetary Science Letters |language=en |volume=204 |issue=1 |pages=265–274 |doi=10.1016/S0012-821X(02)00979-2 |issn=0012-821X}}</ref> proposed the tetraether index of 86 carbon atoms (TEX<sub>86</sub>) as a proxy for [[sea surface temperature]] (SST). GDGT-0 is excluded from the calibration as it can have multiple sources <ref>Koga, Y., Nishihara, M., Morii, H., and Akagawa-Matsushita, M., 1993, Ether polar lipids of methanogenic bacteria: structures, comparative aspects, and biosyntheses: Microbiological Reviews, v. 57, no. 1, p. 164-182</ref> while cren is omitted as it exhibits no correlation with SST and is often an order of magnitude more abundant than its isomer and the other GDGTs. The most recent TEX<sub>86</sub> calibration invokes two separate indices and calibrations:<ref>Kim, J.-H., van der Meer, J., Schouten, S., Helmke, P., Willmott, V., Sangiorgi, F., Koç, N., Hopmans, E. C., and Damsté, J. S. S., 2010, New indices and calibrations derived from the distribution of crenarchaeal isoprenoid tetraether lipids: Implications for past sea surface temperature reconstructions: Geochimica et Cosmochimica Acta, v. 74, no. 16, p. 4639-4654.</ref> TEX<sub>86</sub><sup>H</sup> uses the same combination of GDGTs as in the original TEX<sub>86</sub> relationship:

:<math>\text{GDGT ratio-2}=\tfrac{[\text{GDGT-2}]+[\text{GDGT-3}]+[\text{cren}']}{[\text{GDGT-1}]+[\text{GDGT-2}]+[\text{GDGT-3}]+[\text{cren}']}</math>

GDGT ratio-2 is correlated to SST using the calibration equation: 
:TEX<sub>86</sub><sup>H</sup> = 68.4&times;log(GDGT ratio-2) + 38.6. 
TEX<sub>86</sub><sup>H</sup> has a calibration error of ±2.5&nbsp;°C and is based upon 255 core-top sediments.

TEX<sub>86</sub><sup>L</sup> employs a combination of GDGTs that is different from TEX<sub>86</sub><sup>H</sup>, removing GDGT-3 from the numerator and excluding cren' entirely:

:<math>\text{GDGT ratio-1}=\tfrac{[\text{GDGT-2}]}{[\text{GDGT-1}]+[\text{GDGT-2}]+[\text{GDGT-3}]}</math>

GDGT ratio-1 is correlated to SST using the calibration equation:
:TEX<sub>86</sub><sup>L</sup> = 67.5&times;log(GDGT ratio-1) + 46.9. 
TEX<sub>86</sub><sup>L</sup>has a calibration error of ±4&nbsp;°C and is based upon 396 core-top sediment samples.

Other calibrations exist (including 1/TEX<sub>86</sub>,<ref>Liu, Z., Pagani, M., Zinniker, D., DeConto, R., Huber, M., Brinkhuis, H., Shah, S. R., Leckie, R. M., and Pearson, A., 2009, Global Cooling During the Eocene-Oligocene Climate Transition: Science, v. 323, no. 5918, p. 1187-1190</ref> TEX<sub>86</sub>'<ref>Sluijs, A., Schouten, S., Pagani, M., Woltering, M., Brinkhuis, H., Damsté, J. S. S., Dickens, G. R., Huber, M., Reichart, G.-J., Stein, R., Matthiessen, J., Lourens, L. J., Pedentchouk, N., Backman, J., Moran, K., and the Expedition, S., 2006, Subtropical Arctic Ocean temperatures during the Palaeocene/Eocene thermal maximum: Nature, v. 441, no. 7093, p. 610-613.</ref> and pTEX<sub>86</sub> <ref>Hollis, C. J., Taylor, K. W. R., Handley, L., Pancost, R. D., Huber, M., Creech, J. B., Hines, B. R., Crouch, E. M., Morgans, H. E. G., Crampton, J. S., Gibbs, S., Pearson, P. N., and Zachos, J. C., 2012, Early Paleogene temperature history of the Southwest Pacific Ocean: Reconciling proxies and models: Earth and Planetary Science Letters, v. 349–350, no. 0, p. 53-66.</ref>) and should be considered when reconstructing temperature.

==Caveats==
There are several caveats to this proxy and this list is by no means exhaustive. For more information, consult Schouten ''et al.''  2013.<ref name="Schouten13.rev">{{Cite journal|date=2013-01-01|title=The organic geochemistry of glycerol dialkyl glycerol tetraether lipids: A review|url=https://www.sciencedirect.com/science/article/abs/pii/S0146638012001982|journal=Organic Geochemistry|language=en|volume=54|pages=19–61|doi=10.1016/j.orggeochem.2012.09.006|issn=0146-6380|last1=Schouten|first1=Stefan|last2=Hopmans|first2=Ellen C.|last3=Sinninghe Damsté|first3=Jaap S.}}</ref>

===Terrestrial input===
The branched vs isoprenoidal tetratether (BIT) index can used to measure the relative fluvial input of terrestrial organic matter (TOM) into the marine realm.<ref>{{Cite journal |last=Hopmans |first=Ellen C |last2=Weijers |first2=Johan W. H |last3=Schefuß |first3=Enno |last4=Herfort |first4=Lydie |last5=Sinninghe Damsté |first5=Jaap S |last6=Schouten |first6=Stefan |date=2004-07-30 |title=A novel proxy for terrestrial organic matter in sediments based on branched and isoprenoid tetraether lipids |url=https://www.sciencedirect.com/science/article/pii/S0012821X04003176 |journal=Earth and Planetary Science Letters |language=en |volume=224 |issue=1 |pages=107–116 |doi=10.1016/j.epsl.2004.05.012 |issn=0012-821X}}</ref> The BIT index is based upon the premise that crenarchaeol is derived from marine-dwelling Nitrososphaerota and branched GDGTs are derived from terrestrial soil bacteria. When BIT values exceed 0.4, a deviation of >2&nbsp;°C is incorporated into TEX<sub>86</sub>-based SST estimates. However, isoprenoidal GDGTs can be synthesised on land (by terrestrial archaea) and can render BIT values unreliable; isoGDGT becomes more abundant with higher soil pH.<ref name="Schouten13.rev"/>{{rp|at=§7.1.2}} A strong co-variation between GDGT-4 and branched GDGTs in modern marine and freshwater environments also suggests a common or mixed source for isoprenoidal and branched GDGTs (Fietz et al., 2012).{{full citation needed|date=December 2023}}

===Anaerobic oxidation of methane (AOM)===
The Methane Index (MI) was proposed to help distinguish the relative input of methanotrophic [[Euryarchaeota]] in settings characterised by diffuse methane flux and anaerobic oxidation of methane (AOM).<ref>{{Cite journal|title = Methane Index: A tetraether archaeal lipid biomarker indicator for detecting the instability of marine gas hydrates |date = 2011|journal = Earth and Planetary Science Letters |volume=307 |issue = 3–4 |pages=525–534|doi = 10.1016/j.epsl.2011.05.031|bibcode = 2011E&PSL.307..525Z |last1 = Zhang |first1 = Yi Ge |last2 = Zhang |first2 = Chuanlun L. |last3 = Liu |first3 = Xiao-Lei |last4 = Li |first4 = Li |last5 = Hinrichs |first5 = Kai-Uwe |last6 = Noakes |first6 = John E. }}</ref> These sites are characterised by a distinct GDGT distribution, namely the predominance of GDGT-1. -2 and -3. High MI values (>0.5) reflect high rates of gas-hydrate-related AOM.

===Degradation===
Thermal maturity is only thought to affect GDGTs when temperature exceed 240&nbsp;°C. This can be tested using a ratio of specific [[hopane]] [[isomers]]. [[Oxic]] degradation, which is a selective process and degrades compounds at different rates, has been shown to affect TEX<sub>86</sub> values and can bias SST values by up to 6&nbsp;°C.

==Application==
The oldest TEX<sub>86</sub> record is from the middle [[Jurassic]] (~160Ma) and indicates relatively warm sea surface temperatures.<ref>Jenkyns, H., Schouten-Huibers, L., Schouten S. and Sinninghe-Damste, J.S., 2012, Warm Middle Jurassic-early Cretaceous high-latitude sea surface temperature from the Southern Ocean. Climate of the Past, v. 8, p.215-226</ref> TEX<sub>86</sub> has been used to reconstruct temperature throughout the [[Cenozoic]] era (65–0 Ma)<ref>Sluijs, A., Schouten, S., Donders, T. H., Schoon, P. L., Rohl, U., Reichart, G.-J., Sangiorgi, F., Kim, J.-H., Sinninghe Damste, J. S., and Brinkhuis, H., 2009, Warm and wet conditions in the Arctic region during Eocene Thermal Maximum 2: Nature Geosci, v. 2, no. 11, p. 777-780.</ref><ref>Zachos, J. C., Schouten, S., Bohaty, S., Quattlebaum, T., Sluijs, A., Brinkhuis, H., Gibbs, S. J., and Bralower, T. J., 2006, Extreme warming of mid-latitude coastal ocean during the Paleocene-Eocene Thermal Maximum: Inferences from TEX86 and isotope data: Geology, v. 34, no. 9, p. 737-740.</ref> and is useful when other SST proxies are diagenetically altered (e.g. planktonic [[foraminifera]]<ref>Pearson, P. N., van Dongen, B. E., Nicholas, C. J., Pancost, R. D., Schouten, S., Singano, J. M., and Wade, B. S., 2007, Stable warm tropical climate through the Eocene Epoch: Geology, v. 35, no. 3, p. 211-214.</ref>) or absent (e.g. [[alkenones]]<ref>Bijl, P. K., Schouten, S., Sluijs, A., Reichart, G.-J., Zachos, J. C., and Brinkhuis, H., 2009, Early Palaeogene temperature evolution of the southwest Pacific Ocean: Nature, v. 461, no. 7265, p. 776-779.</ref>).

===Eocene===
TEX<sub>86</sub> has been extensively used to reconstruct [[Eocene]] (55-34Ma) SST. During the early Eocene, TEX<sub>86</sub> values indicate warm high southern hemisphere latitude SSTs (20-25&nbsp;°C) in agreement  with other, independently derived proxies (e.g. [[alkenones]], [[Paleothermometer#CLAMP (Climate leaf analysis multivariate program)|CLAMP]], [[Mg/Ca]]). During the middle and late Eocene, high southern latitude sites cooled while the tropics remained stable and warm. Possible reasons for this cooling include long-term changes in [[carbon dioxide]] and/or changes in gateway reorganisation (e.g. [[Tasman Gateway]], [[Drake Passage]]).

==References==
<references/>

== Further reading ==
{{Wikibooks|Historical Geology|TEX86}}

[[Category:Lipid methods]]
[[Category:Paleoclimatology]]