View source for OpenMath

[[File:2000 Year Temperature Comparison.png|thumb|right|300px]]

In the study of past climates, known as [[paleoclimatology]],<ref>[http://serc.carleton.edu/microbelife/topics/proxies/paleoclimate.html Bruckner, Monica. "Paleoclimatology: How Can We Infer Past Climates?"]</ref> '''climate proxies''' are preserved physical characteristics of the past that stand in for direct measurements (as [[Proxy (statistics)|statistical proxies]]), to enable scientists to reconstruct the [[Climate|climatic conditions]] that prevailed during much of the Earth's history. As reliable modern records of climate only began in the 1880s, proxies provide a means for scientists to determine climatic patterns before record-keeping began. Examples of proxies include [[ice core]]s, [[tree rings]], [[palynology|sub-fossil pollen]], [[borehole]]s, [[coral]]s, and [[Sediment|lake and ocean sediments]]. The character of deposition or rate of  growth of the proxies' material has been influenced by the climatic conditions of the time in which they were laid down or grew. Chemical traces produced by climatic changes, such as quantities of particular [[isotopes]], can be recovered from proxies. Some proxies, such as gas bubbles trapped in ice, enable traces of the ancient atmosphere to be recovered and measured directly to provide a history of fluctuations in the composition of the Earth's atmosphere.<ref>{{cite book|last=Strom|first=Robert G.|title=Hot house: global climate change and the human condition|page=253|publisher=Copernicus Books|isbn=978-0-387-34179-8|year=2007}}</ref> To produce the most precise results, systematic cross-verification between proxy indicators is necessary for accuracy in readings and record-keeping.<ref>[http://www.grida.no/publications/other/ipcc_tar/?src=/climate/ipcc_tar/wg1/068.htm "Climate Change 2001: 2.3.2.1 Palaeoclimate proxy indicators."]</ref> 

Proxies can be combined to produce temperature reconstructions longer than the [[instrumental temperature record]] and can inform discussions of [[global warming]]. The distribution of proxy records, just like the instrumental record, is strongly non-uniform, with more records in the northern hemisphere.<ref name="unisci.com">[http://unisci.com/stories/20011/0227012.htm "Borehole Temperatures Confirm Global Warming Pattern."]</ref>

==Ice cores==
===Drilling===

[[Image:Icecore 4x.jpg|thumb|Ice core|Ice Core sample taken from drill. Photo by [[Lonnie Thompson]], [[Byrd Polar Research Center]].]] [[Ice cores]] are [[Core sample|cylindrical samples]] from within [[ice sheets]] in the [[Greenland]], [[Antarctic]], and [[North American]] regions.<ref name="Strom, Robert p. 255">Strom, Robert. ''Hot House.'' p. 255</ref><ref name="Core Location Maps.">[http://nicl.usgs.gov/coresite.htm "Core Location Maps."]</ref> First attempts of extraction occurred in 1956 as part of the [[International Geophysical Year]]. As original means of extraction, the [[Cold Regions Research and Engineering Laboratory|U.S. Army’s Cold Regions Research and Engineering Laboratory]] used an {{convert|80|ft|m|adj=on}}-long modified electrodrill in 1968 at [[Camp Century]], [[Greenland]], and [[Byrd Station]], [[Antarctica]]. Their machinery could drill through 15–20 feet of [[ice sheet|ice]] in 40–50 minutes. From 1300 to {{convert|3000|ft|m}} in depth, [[core sample]]s were 4 ¼ inches in [[diameter]] and 10 to {{convert|20|ft|m}} long. Deeper [[core sample|samples]] of 15 to {{convert|20|ft|m}} long were not uncommon. Every subsequent [[drilling]] team improves their method with each new effort.<ref>Vardiman, Larry, Ph.D. ''Ice Cores and the Age of the Earth.'' p. 9-13</ref>

===Proxy===

[[File:Vostok deltaD deltaO18.jpg|thumb|left|xcenter|tt300px|&delta;18O<sub>air</sub> and &delta;D<sub>ice</sub> for Vostok, Antarctica ice core.]]

Presence of [[Properties of water#Heavy water and isotopologues|water molecule isotopic compositions]] of <sup>16</sup>O and <sup>18</sup>O in an [[ice core]] help determine [[Paleoclimatology|past temperatures]] and [[Precipitation (meteorology)#Measurement|snow accumulations]].<ref name="Strom, Robert p. 255"/> The heavier [[isotope]] (<sup>18</sup>O) condenses more readily as [[temperatures]] decrease and falls as [[Precipitation (meteorology)|precipitation]], while the lighter [[isotope]] (<sup>16</sup>O) can fall in even colder conditions. The farther [[north]] elevated levels of an <sup>18</sup>O isotope are detected signals a warming over time.<ref>[http://earthobservatory.nasa.gov/Features/Paleoclimatology_OxygenBalance/oxygen_balance.php "Paleoclimatology: the Oxygen Balance."]</ref> 

In addition to oxygen isotopes, water contains hydrogen isotopes - <sup>1</sup>H and <sup>2</sup>H, usually referred to as H and D (for [[deuterium]]) - that are also used for temperature proxies. Normally, ice cores from Greenland are analyzed for δ<sup>18</sup>O and those from Antarctica for δ-deuterium.{{Why?|date=November 2011}} Those cores that analyze for both show a lack of agreement. (In the figure, δ<sup>18</sup>O is for the trapped air, not the ice. δD is for the ice.)

[[Air bubble]]s in the ice, which contain trapped [[greenhouse gases]] such as [[carbon dioxide]] and [[methane]], are also helpful in determining [[Paleoclimatology|past climate]] changes.<ref name="Strom, Robert p. 255"/>

From 1989-1992, the European Greenland Ice Core Drilling Project drilled in central [[Greenland]] at coordinates 72° 35' N, 37° 38' W.  In their project, ice at a depth of 770 m were 3840 years old; 2521 m were 40,000 years old; and 3029 m at [[bedrock]] were 200,000 years old or more.<ref>[http://www.ncdc.noaa.gov/paleo/icecore/greenland/summit/document/ "The GRIP Coring Effort."]</ref> However, [[ice cores]] can reveal the climate records for the past 650,000 years.<ref name="Strom, Robert p. 255"/>

Location [[maps]] and a complete list of [[U.S.]] [[ice core]] drilling sites can be found on the website for the [[National Ice Core Laboratory]]: http://nicl.usgs.gov/coresite.htm<ref>[http://nicl.usgs.gov/coresite.htm "Core Location Maps."]</ref>

==Tree rings==
[[Image:Tree rings.jpg|thumb|left|Tree rings seen in a cross section of a trunk of a tree|Tree rings seen in a cross section of a trunk of a tree.]]
{{main|Dendroclimatology}}

Dendroclimatology is the science of determining past climates from trees (primarily properties of the annual tree rings). Tree rings are wider when conditions favor growth, narrower when times are difficult. Other properties of the annual rings, such as maximum latewood density (MXD) have been shown to be better proxies than simple ring width. Using tree rings, scientists have estimated many local climates for hundreds to thousands of years previous. By combining multiple tree-ring studies (sometimes with other climate proxy records), scientists have estimated past regional and global climates (see [[Temperature record of the past 1000 years]]).

==Boreholes==

[[Borehole]] temperatures are used as temperature proxies. Since heat transfer through the ground is slow, temperature measurements at a series of different depths down the borehole, adjusted for the effect of rising heat from inside the Earth, can be "[[Invertible matrix|inverted]]" (a mathematical formula to solve matrix equations) to produce a non-unique series of surface temperature values. The solution is "non-unique" because there are multiple possible surface temperature reconstructions that can produce the same borehole temperature profile. In addition,  due to physical limitations, the reconstructions are inevitably "smeared", and become more smeared further back in time. When reconstructing temperatures around 1,500 AD, boreholes have a temporal resolution of a few centuries. At the start of the 20th Century, their resolution is a few decades; hence they do not provide a useful check on the [[instrumental temperature record]].<ref name="Boreholes_in_Glacial_Ice_p80">http://www.nap.edu/openbook.php?record_id=11676&page=80</ref><ref>Huang, S. P., Pollack, H. N., Shen, P. Y. [http://www.ldeo.columbia.edu/~peter/Resources/Seminar/readings/Huang_boreholeTemp_Nature%2700.pdf ''Temperature trends ever the past five centuries reconstructed from borehole temperatures''] ''Nature'', 403, 6771, pp 756-758, 2000. {{doi|10.1038/35001556}}.</ref> However, they are broadly comparable.<ref name="unisci.com"/> These confirmations have given paleoclimatologists the confidence that they can measure the temperature of 500 years ago. This is concluded by a depth scale of about 492 feet (150 meters) to measure the temperatures from 100 years ago and 1,640 feet (500 meters) to measure the temperatures from 1,000 years ago.<ref name="archives.cnn.com">[http://archives.cnn.com/2000/NATURE/02/17/boreholes.enn/ Environmental News Network staff. "Borehole temperatures confirm global warming."]</ref> 

Boreholes have a great advantage over many other proxies in that no calibration is required: they are actual temperatures. However, they record surface temperature not the near-surface temperature (1.5 meter) used for most "surface" weather observations. These can differ substantially under extreme conditions or when there is surface snow. In practice the effect on borehole temperature is believed to be generally small. A second source of error is contamination of the well by groundwater may affect the temperatures, since the water "carries" more modern temperatures with it. This effect is believed to be generally small, and more applicable at very humid sites.<ref name="Boreholes_in_Glacial_Ice_p80" /> It does not apply in ice cores where the site remains frozen all year.

More than 600 boreholes, on all continents, have been used as proxies for reconstructing surface temperatures.<ref>[http://www.nature.com/nature/journal/v403/n6771/abs/403756a0.html Huang, Shaopeng, et al. "Temperature trends over the past five centuries reconstructed from borehole temperatures."]</ref> The highest concentration of boreholes exist in [[North America]] and [[Europe]]. Their depths of drilling typically range from 200 to greater than 1,000 meters into the [[Crust (geology)|crust]] of the Earth or ice sheet.<ref name="archives.cnn.com"/>

A small number of boreholes have been drilled in the ice sheets; the purity of the ice there permits longer reconstructions. Central Greenland borehole temperatures show "a warming over the last 150 years of approximately 1°C ± 0.2°C preceded by a few centuries of cool conditions. Preceding this was a warm period centered around A.D. 1000, which was warmer than the late 20th century by approximately 1°C." A borehole in the Antarctica icecap shows that the "temperature at A.D. 1 [was] approximately 1°C warmer than the late 20th century".<ref name="Boreholes_in_Glacial_Ice_p81">[http://www.nap.edu/openbook.php?record_id=11676&page=81 BOREHOLES IN GLACIAL ICE] Surface Temperature Reconstructions for the Last 2,000 Years (2006), pp 81,82 Board on Atmospheric Sciences and Climate (BASC), National Academy of Science, ISBN 978-0-309-10225-4</ref>

Borehole temperatures in Greenland were responsible for an important revision to the isotopic temperature reconstruction, revealing that the former assumption that "spatial slope equals temporal slope" was incorrect.

==Corals==

[[Ocean]] [[coral]] [[skeletal]] rings, or bands, also share paleoclimatological information, similarly to [[tree rings]]. In 2002, a report was published on the findings of Drs. Lisa Greer and Peter Swart, associates of [[University of Miami]] at the time, in regard to [[Isotopes of oxygen|stable oxygen isotopes]] in the [[calcium carbonate]] of coral. Cooler temperatures tend to cause coral to use heavier isotopes in its structure, while warmer temperatures result in more normal [[oxygen isotopes]] being built into the coral structure. Denser water [[salinity]] also tends to contain the heavier isotope. Greer’s coral sample from the [[Atlantic Ocean]] was taken in 1994 and dated back to 1935. Greer recalls her conclusions, "When we look at the averaged annual data from 1935 to about 1994, we see it has the shape of a [[sine wave]]. It is periodic and has a significant pattern of [[oxygen isotope]] composition that has a peak at about every twelve to fifteen years." [[Sea surface temperature|Surface water temperatures]] have coincided by also peaking every twelve and a half years. However, since recording this temperature has only been practiced for the last fifty years, correlation between recorded water temperature and coral structure can only be drawn so far back.<ref>[http://earthobservatory.nasa.gov/Newsroom/view.php?id=22843 "Coral Layers Good Proxy for Atlantic Climate Cycles."]</ref>

==Pollen grains==
Pollen can be found in sediments. Plants produce [[pollen]] in large quantities and it is extremely resistant to decay. It is possible to identify a plant species from its pollen grain. The identified plant community of the area at the relative time from that sediment layer, will provide information about the climatic condition. The abundance of pollen of a given [[vegetation]] period or year depends partly on the weather conditions of the previous months, hence pollen density provides information on short-term climatic conditions.<ref>Bradley, R. S. and Jones, P. D. (eds) 1992: Climate since AD 1500. London: Routledge.</ref> The study of prehistoric pollen is [[palynology]].

==Lake and ocean sediments==

Similar to their study on other proxies, [[paleoclimatologists]] examine [[oxygen isotopes]] in the contents of ocean [[sediments]]. Likewise, they measure the layers of [[varve]] (deposited fine and coarse silt or clay)<ref>[http://www.merriam-webster.com/dictionary/varve "Varve."]</ref> laminating lake sediments. Lake varves are primarily influenced by:

* Summer temperature, which shows the energy available to melt seasonal snow and ice
* Winter snowfall, which determines the level of disturbance to sediments when melting occurs
* Rainfall<ref>[http://www.grida.no/publications/other/ipcc_tar/?src=/climate/ipcc_tar/wg1/068.htm "Climate Change 2001: 2.3.2.1 Palaeoclimate proxy indicators"]</ref>

== Water isotopes and temperature reconstruction ==

Ocean water is mostly <math>{H_2}^{16}O</math>, with small amounts of <math>HD^{16}O</math> and <math>{H_2}^{18}O</math>, where D denotes [[Deuterium]], i.e. Hydrogen with an extra neutron.  In [[Vienna Standard Mean Ocean Water]] (VSMOW) the ratio of D to H is <math>155.76\times 10^{-6}</math> and O-18 to O-16 is <math>2005.2\times 10^{-6}</math>.  Fractionation occurs during changes between condensed and vapour phases: the vapour pressure of heavier isotopes is lower, so vapour contains relatively more of the lighter isotopes and when the vapour condenses the precipitation preferentially contains heavier isotopes.  The difference from VSMOW is expressed as δ<sup>18</sup>O = 1000‰ <math>\times \left( \frac{([{}^{18}O]/[{}^{16}O])}{([{}^{18}O]/[{}^{16}O])_{\mathrm{VSMOW}}} - 1\right)</math>; and a similar formula for δD. δ values for precipitation are always negative.<ref>http://books.nap.edu/openbook.php?record_id=11676&page=66</ref>  The major influence on δ is the difference between ocean temperatures where the moisture evaporated and the place where the final precipitation occurred; since ocean temperatures are relatively stable the δ value mostly reflects the temperature where precipitation occurs. Taking into account that the precipitation forms above the [[inversion (meteorology)|inversion]] layer, we are left with a linear relation:

: &delta; <sup>18</sup>O = aT + b

which is empirically calibrated from measurements of temperature and δ as a = 0.67 ‰/<sup>o</sup>C for [[Greenland]] and 0.76 ‰/<sup>o</sup>C for East [[Antarctica]].  The calibration was initially done on the basis of ''spatial'' variations in temperature and it was assumed that this corresponded to ''temporal'' variations (Jouzel and Merlivat, 1984). More recently, [[#Boreholes|borehole thermometry]] has shown that for glacial-interglacial variations, a = 0.33 ‰/<sup>o</sup>C (Cuffey et al., 1995), implying that glacial-interglacial temperature changes were twice as large as previously believed.

== Pseudoproxies ==

The skill of algorithms used to combine proxy records into an overall hemispheric temperature reconstruction may be tested using a technique known as "[[pseudoproxy|pseudoproxies]]". In this method, output from a [[climate model]] is sampled at locations corresponding to the known proxy network, and the temperature record produced is compared to the (known) overall temperature of the model. Some methods of combining the records, in particular [[least squares]], perform poorly.{{cn|date=October 2012}}

== See also ==

* [[Paleothermometer]]
* [[Ice core]]
* [[Dendrochronology]]
* [[Historical climatology]], the study of climate over human history (as opposed to [[Geologic temperature record|earth]]'s)
* [[Palynology]]
* [[Speleothem#As climate proxies|Speleothem]]

==Notes==
{{reflist}}

==References==

* "Borehole Temperatures Confirm Global Warming Pattern." UniSci. 27 Feb. 2001. 7 Oct. 2009. [http://unisci.com/stories/20011/0227012.htm]
* Bruckner, Monica. "Paleoclimatology: How Can We Infer Past Climates?" Microbial Life. 29 Sept. 2008. 23 Nov. 2009. [http://serc.carleton.edu/microbelife/topics/proxies/paleoclimate.html]
* "Climate Change 2001: 2.3.2.1 Palaeoclimate proxy indicators." IPCC. 2003. Sept. 23, 2009.  [http://www.grida.no/publications/other/ipcc_tar/?src=/climate/ipcc_tar/wg1/068.htm]
* "Coral Layers Good Proxy for Atlantic Climate Cycles." Earth Observatory. Webmaster: Paul Przyborski. 7 Dec. 2002. 2 Nov. 2009. [http://earthobservatory.nasa.gov/Newsroom/view.php?id=22843]
* "Core Location Maps." National Ice Core Laboratory. 9 Apr. 2009. 23 Nov. 2009. [http://nicl.usgs.gov/coresite.htm]
* "Dendrochronology." Merriam-Webster Online Dictionary. Merriam-Webster Online. 2009. 2 Oct. 2009. [http://www.merriam-webster.com/dictionary/Dendrochronology]
* Environmental News Network staff. "Borehole temperatures confirm global warming." CNN.com. 17 Feb. 2000. 7 Oct. 2009. [http://archives.cnn.com/2000/NATURE/02/17/boreholes.enn/]
* "The GRIP Coring Effort." NCDC. 26 Sept. 2009. [http://www.ncdc.noaa.gov/paleo/icecore/greenland/summit/document/]
* "Growth ring." Encyclopædia Britannica. Encyclopædia Britannica Online. 2009. 23 Oct. 2009. [http://www.britannica.com/EBchecked/topic/247295/growth-ring]
* Huang, Shaopeng, et al. "Temperature trends over the past five centuries reconstructed from borehole temperatures." Nature. 2009. 6 Oct. 2009. [http://www.nature.com/nature/journal/v403/n6771/abs/403756a0.html]
* "Objectives - Kola Superdeep Borehole (KSDB) - IGCP 408: ‘Rocks and Minerals at Great Depths and on the Surface.’" International Continental Scientific Drilling Program. 18 July 2006. 6 Oct. 2009. [http://www.icdp-online.org/contenido/icdp/front_content.php?client=29&lang=28&idcat=1089&idart=1554]
* "Paleoclimatology: the Oxygen Balance." Earth Observatory. Webmaster: Paul Przyborski. 24 Nov. 2009. 24 Nov. 2009. [http://earthobservatory.nasa.gov/Features/Paleoclimatology_OxygenBalance/oxygen_balance.php]
* Schweingruber, Fritz Hans. ''Tree Rings: Basics and Application of Dendrochronology.'' Dordrecht: 1988. 2, 47-8, 54, 256-7.
* Strom, Robert. ''Hot House.'' New York: Praxis, 2007. 255.
* "Varve." Merriam-Webster Online Dictionary. Merriam-Webster Online. 2009. 2 Nov. 2009. [http://www.merriam-webster.com/dictionary/varve]
* Wolff, E. W. (2000) ''History of the atmosphere from ice cores''; ERCA vol 4 pp 147–177

==External links==
*[http://www.rsc.org/chemistryworld/2013/01/climate-proxies Chemical climate proxies] at [[Royal Society of Chemistry]], January 23, 2013

{{DEFAULTSORT:Proxy (Climate)}}
[[Category:Paleoclimatology]]