View source for Earth:Ice core

{{Short description|Cylindrical sample drilled from an ice sheet}}
[[File:Icecore 4.jpg|thumb|Ice core sample taken from drill|alt=An ice core being slid out of a drill barrel sideways]]
An '''ice core''' is a [[Earth:Core sample|core sample]] that is typically removed from an [[Earth:Ice sheet|ice sheet]] or a high mountain [[Earth:Glacier|glacier]].  Since the ice forms from the incremental buildup of annual layers of snow, lower layers are older than upper ones, and an ice core contains ice formed over a range of years.  Cores are [[Earth:Ice drilling|drilled]] with hand [[Engineering:Auger (drill)|augers]] (for shallow holes) or powered drills; they can reach depths of over two miles (3.2&nbsp;km), and contain ice up to 800,000 years old.

The physical properties of the ice and of material trapped in it can be used to reconstruct the climate over the age range of the core.  The proportions of different oxygen and hydrogen [[Physics:Isotope|isotope]]s provide information about [[Earth:Paleothermometer|ancient temperatures]], and the [[Earth:Atmosphere of Earth|air]] trapped in tiny bubbles can be analysed to determine the level of atmospheric gases such as [[Chemistry:Carbon dioxide|carbon dioxide]].  Since [[Physics:Heat transfer|heat flow]] in a large ice sheet is very slow, the borehole temperature is another indicator of temperature in the past.  These data can be combined to find the [[Earth:Climate model|climate model]] that best fits all the available data.

Impurities in ice cores may depend on location.  Coastal areas are more likely to include material of marine origin, such as sea salt [[Physics:Ion|ion]]s.  [[Place:Greenland|Greenland]] ice cores contain layers of [[Earth:Loess|wind-blown dust]] that correlate with cold, dry periods in the past, when cold deserts were scoured by wind.  Radioactive elements, either of natural origin or created by nuclear testing, can be used to date the layers of ice.  Some volcanic events that were sufficiently powerful to send material around the globe have left a signature in many different cores that can be used to synchronise their time scales.

Ice cores have been studied since the early 20th century, and several cores were drilled as a result of the [[Earth:International Geophysical Year|International Geophysical Year]] (1957–1958).  Depths of over 400 m were reached, a record which was extended in the 1960s to 2164 m at Byrd Station in Antarctica.  [[Place:Soviet Union|Soviet]] ice drilling projects in Antarctica include decades of work at Vostok Station, with the deepest core reaching 3769 m.  Numerous other deep cores in the Antarctic have been completed over the years, including the West Antarctic Ice Sheet project, and cores managed by the British Antarctic Survey and the International Trans-Antarctic Scientific Expedition.  In Greenland, a sequence of collaborative projects began in the 1970s with the [[Earth:Greenland Ice Sheet Project|Greenland Ice Sheet Project]]; there have been multiple follow-up projects, with the most recent, the [[Earth:East Greenland Ice-Core Project|East Greenland Ice-Core Project]], originally expected to complete a deep core in east Greenland in 2020 but since postponed.<ref name="corona">{{Cite web|url=https://insideclimatenews.org/news/26032020/coronavirus-climate-science-research-impact|title=Coronavirus Already Hindering Climate Science, But the Worst Disruptions Are Likely Yet to Come|date=27 March 2020|first=Bob|last=Berwyn|access-date=5 April 2020}}</ref>

== Structure of ice sheets and cores ==
[[File:Taku glacier firn ice sampling.png|thumb|Sampling the surface of Taku Glacier in Alaska.  There is increasingly dense firn between surface snow and blue glacier ice.|alt=A scientist in a pit of snow]]

An ice core is a vertical column through a glacier, sampling the layers that formed through an annual cycle of snowfall and melt.<ref name=":23" /> As snow accumulates, each layer presses on lower layers, making them denser until they turn into [[Earth:Firn|firn]]. Firn is not dense enough to prevent air from escaping; but at a density of about 830&nbsp;kg/m<sup>3</sup> it turns to ice, and the air within is sealed into bubbles that capture the composition of the atmosphere at the time the ice formed.<ref name=":0" /> The depth at which this occurs varies with location, but in Greenland and the Antarctic it ranges from 64&nbsp;m to 115&nbsp;m.<ref name=":6">{{harvnb|Talalay|2016}}, p. 263.</ref> Because the rate of snowfall varies from site to site, the age of the firn when it turns to ice varies a great deal. At Summit Camp in Greenland, the depth is 77 m and the ice is 230 years old; at [[Place:Dome C|Dome C]] in Antarctica the depth is 95 m and the age 2500 years.<ref>{{Cite book|title=Paleoclimatology: Reconstructing Climates of the Quaternary|last=Bradley|first=Raymond S.|publisher=Academic Press|year=2015|isbn=978-0-12-386913-5|location=Amsterdam|page=138}}</ref> As further layers build up, the pressure increases, and at about 1500&nbsp;m the [[Chemistry:Crystal structure|crystal structure]] of the ice changes from hexagonal to cubic, allowing air molecules to move into the cubic crystals and form a clathrate. The bubbles disappear and the ice becomes more transparent.<ref name=":0">{{harvnb|Alley|2000}}, pp. 48–50.</ref>

Two or three feet of snow may turn into less than a foot of ice.<ref name=":0" /> The weight above makes deeper layers of ice thin and flow outwards. Ice is lost at the edges of the glacier to icebergs, or to summer melting, and the overall shape of the glacier does not change much with time.<ref>{{harvnb|Alley|2000}}, pp. 35–36.</ref> The outward flow can distort the layers, so it is desirable to drill deep ice cores at places where there is very little flow. These can be located using maps of the flow lines.<ref>{{Cite book|title=Glaciers|last=Knight|first=Peter G.|publisher=Stanley Thornes|year=1999|isbn=978-0-7487-4000-0|location=Cheltenham, UK|page=[https://archive.org/details/glaciers0000knig/page/206 206]|url=https://archive.org/details/glaciers0000knig/page/206}}</ref>

Impurities in the ice provide information on the environment from when they were deposited. These include soot, ash, and other types of particle from [[Biology:Wildfire|forest fires]] and [[Earth:Volcano|volcano]]es; isotopes such as [[Physics:Beryllium-10|beryllium-10]] created by [[Astronomy:Cosmic ray|cosmic ray]]s;
[[Chemistry:Micrometeorite|micrometeorite]]s; and [[Biology:Pollen|pollen]].<ref name=":23">{{harvnb|Alley|2000}}, pp. 71–73.</ref> The lowest layer of a glacier, called basal ice, is frequently formed of subglacial meltwater that has refrozen. It can be up to about 20 m thick, and though it has scientific value (for example, it may contain subglacial microbial populations),<ref>{{Cite report|url=https://websites.pmc.ucsc.edu/~tulaczyk/Report_I_V.pdf|title=FASTDRILL: Interdisciplinary Polar Research Based on Fast Ice-Sheet Drilling|last1=Tulaczyk|first1=S. |last2=Elliot|first2=D. |last3=Vogel|first3=S.W. |last4=Powell|first4=R.D. |last5=Priscu|first5=J.C. |last6=Clow|first6=G.D. |year=2002|publisher=2002 FASTDRILL Workshop|page=9}}</ref> it often does not retain stratigraphic information.<ref>{{Cite book|title=Environmental Contaminants: Using Natural Archives to Track Sources and Long-Term Trends of Pollution|last1=Gabrielli|first1=Paolo|last2=Vallelonga|first2=Paul|publisher=Springer|year=2015|isbn=978-94-017-9540-1|editor-last=Blais|editor-first=Jules M.|location=Dordrecht, Netherlands|page=395|chapter=Contaminant Records in Ice Cores|display-editors=et al.}}</ref>

Cores are often drilled in areas such as Antarctica and central Greenland where the temperature is almost never warm enough to cause melting, but the summer sun can still alter the snow. In polar areas, the sun is visible day and night during the local summer and invisible all winter. It can make some snow [[Sublimation (phase transition)|sublimate]], leaving the top inch or so less dense. When the sun approaches its lowest point in the sky, the temperature drops and hoar frost forms on the top layer. Buried under the snow of following years, the coarse-grained hoar frost compresses into lighter layers than the winter snow. As a result, alternating bands of lighter and darker ice can be seen in an ice core.<ref>{{harvnb|Alley|2000}}, pp. 43–46.</ref>

== Coring ==
[[File:Brooks ice auger patent drawings 1932-retouched.png|alt=Drawing of a cylinder with two helical flanges around it and cutting teeth at the bottom|left|thumb|Ice auger patented in 1932; the design is very similar to modern augers used for shallow drilling.<ref name=":1">{{harvnb|Talalay|2016}}, pp. 34–35.</ref>]]
Ice cores are collected by cutting around a cylinder of ice in a way that enables it to be brought to the surface.  Early cores were often collected with hand [[Engineering:Auger (drill)|augers]] and they are still used for short holes. A design for ice core augers was patented in 1932 and they have changed little since.  An auger is essentially a cylinder with [[Helix|helical]] metal ribs (known as flights) wrapped around the outside, at the lower end of which are cutting blades.  Hand augers can be rotated by a T handle or a [[Engineering:Brace (tool)|brace handle]], and some can be attached to handheld [[Engineering:Electric drill|electric drill]]s to power the rotation.  With the aid of a [[Engineering:Tripod|tripod]] for lowering and raising the auger, cores up to 50&nbsp;m deep can be retrieved, but the practical limit is about 30&nbsp;m for engine-powered augers, and less for hand augers.  Below this depth, electromechanical or thermal drills are used.<ref name=":1" />

The cutting apparatus of a drill is on the bottom end of a drill barrel, the tube that surrounds the core as the drill cuts downward.  The [[Earth:Drill cuttings|cuttings]] (chips of ice cut away by the drill) must be drawn up the hole and disposed of or they will reduce the cutting efficiency of the drill.<ref name=":2">{{harvnb|Talalay|2016}}, p. 59.</ref> They can be removed by compacting them into the walls of the hole or into the core, by air circulation (dry drilling),<ref name=":2" /><ref name="Talalay 2016">{{harvnb|Talalay|2016}}, p. 7.</ref> or by the use of a [[Engineering:Drilling fluid|drilling fluid]] (wet drilling).<ref name=":3">{{harvnb|Talalay|2016}}, p. 77.</ref> Dry drilling is limited to about 400&nbsp;m depth, since below that point a hole would close up as the ice deforms from the weight of the ice above.<ref>{{Cite web|url=http://www.iceandclimate.nbi.ku.dk/research/drill_analysing/drilling_techniques/deep_drilling/|title=Deep drilling with the Hans Tausen drill|date=2 October 2008|publisher=Niels Bohr Institute Centre for Ice and Climate|language=en|access-date=3 June 2017|archive-date=3 September 2017|archive-url=https://web.archive.org/web/20170903025631/http://www.iceandclimate.nbi.ku.dk/research/drill_analysing/drilling_techniques/deep_drilling/|url-status=dead}}</ref>

Drilling fluids are chosen to balance the pressure so that the hole remains stable.<ref name="Talalay 2016"/> The fluid must have a low kinematic [[Physics:Viscosity|viscosity]] to reduce [[Engineering:Tripping (pipe)|tripping]] time (the time taken to pull the drilling equipment out of the hole and return it to the bottom of the hole).  Since retrieval of each segment of core requires tripping, a slower speed of travel through the drilling fluid could add significant time to a project—a year or more for a deep hole.  The fluid must contaminate the ice as little as possible; it must have low [[Medicine:Toxicity|toxicity]], for safety and to minimize the effect on the environment; it must be available at a reasonable cost; and it must be relatively easy to transport.<ref>{{cite journal|last1=Sheldon|first1=Simon G.|last2=Popp|first2=Trevor J.|last3=Hansen|first3=Steffen B.|last4=Steffensen|first4=Jørgen P.|title=Promising new borehole liquids for ice-core drilling on the East Antarctic high plateau|journal=Annals of Glaciology|date=26 July 2017|volume=55|issue=68|pages=260–270|doi=10.3189/2014AoG68A043|doi-access=free}}</ref> Historically, there have been three main types of ice drilling fluids: two-component fluids based on [[Chemistry:Kerosene|kerosene]]-like products mixed with [[Chemistry:Fluorocarbon|fluorocarbon]]s to increase density; alcohol compounds, including aqueous [[Chemistry:Ethylene glycol|ethylene glycol]] and [[Chemistry:Ethanol|ethanol]] solutions; and [[Chemistry:Ester|ester]]s, including n-butyl acetate.  Newer fluids have been proposed, including new ester-based fluids, low-molecular weight dimethyl siloxane oils, [[Chemistry:Fatty acid ester|fatty-acid esters]], and kerosene-based fluids mixed with foam-expansion agents.<ref>{{harvnb|Talalay|2016}}, pp. 259–263.</ref>

Rotary drilling is the main method of drilling for minerals and it has also been used for ice drilling. It uses a string of drill pipe rotated from the top, and drilling fluid is pumped down through the pipe and back up around it.  The cuttings are removed from the fluid at the top of the hole and the fluid is then pumped back down.<ref name=":3" /> This approach requires long trip times, since the entire drill string must be hoisted out of the hole, and each length of pipe must be separately disconnected, and then reconnected when the drill string is reinserted.<ref name=":2" /><ref name=":4">{{harvnb|Talalay|2016}}, p. 101.</ref> Along with the logistical difficulties associated with bringing heavy equipment to ice sheets, this makes traditional rotary drills unattractive.<ref name=":2" /> In contrast, [[Engineering:Wireline (cabling)|wireline]] drills allow the removal of the core barrel from the drill assembly while it is still at the bottom of the borehole.  The core barrel is hoisted to the surface, and the core removed; the barrel is lowered again and reconnected to the drill assembly.<ref>{{harvnb|Talalay|2016}}, p. 79.</ref> Another alternative is flexible drill-stem rigs, in which the drill string is flexible enough to be coiled when at the surface.  This eliminates the need to disconnect and reconnect the pipes during a trip.<ref name=":4" />[[File:Drilling mechanical-drill-head.jpg|thumb|Mechanical drill head, showing cutting teeth|alt=The bottom of an ice drill]] The need for a string of drillpipe that extends from the surface to the bottom of the borehole can be eliminated by suspending the entire downhole assembly on an armoured cable that conveys power to the downhole motor.  These cable-suspended drills can be used for both shallow and deep holes; they require an anti-torque device, such as [[Physics:Leaf spring|leaf-springs]] that press against the borehole, to prevent the drill assembly rotating around the drillhead as it cuts the core.<ref>{{harvnb|Talalay|2016}}, pp. 109–111.</ref> The drilling fluid is usually circulated down around the outside of the drill and back up between the core and core barrel; the cuttings are stored in the downhole assembly, in a chamber above the core.  When the core is retrieved, the cuttings chamber is emptied for the next run.  Some drills have been designed to retrieve a second annular core outside the central core, and in these drills the space between the two cores can be used for circulation.  Cable-suspended drills have proved to be the most reliable design for deep ice drilling.<ref>{{harvnb|Talalay|2016}}, pp. 173–175.</ref><ref>{{harvnb|Talalay|2016}}, pp. 252–254.</ref>

Thermal drills, which cut ice by electrically heating the drill head, can also be used, but they have some disadvantages.  Some have been designed for working in cold ice; they have high power consumption and the heat they produce can degrade the quality of the retrieved ice core.  Early thermal drills, designed for use without drilling fluid, were limited in depth as a result; later versions were modified to work in fluid-filled holes but this slowed down trip times, and these drills retained the problems of the earlier models.  In addition, thermal drills are typically bulky and can be impractical to use in areas where there are logistical difficulties.  More recent modifications include the use of [[Chemistry:Antifreeze|antifreeze]], which eliminates the need for heating the drill assembly and hence reduces the power needs of the drill.<ref>{{cite journal|last1=Zagorodnov|first1=V.|last2=Thompson|first2=L.G.|title=Thermal electric ice-core drills: history and new design options for intermediate-depth drilling|journal=Annals of Glaciology|date=26 July 2017|volume=55|issue=68|pages=322–330|doi=10.3189/2014AoG68A012|doi-access=free}}</ref> Hot-water drills use jets of hot water at the drill head to melt the water around the core. The drawbacks are that it is difficult to accurately control the dimensions of the borehole, the core cannot easily be kept sterile, and the heat may cause [[Physics:Thermal shock|thermal shock]] to the core.<ref>{{Cite book|title=Exploration of Antarctic Subglacial Aquatic Environments: Environmental and Scientific Stewardship|last=National Research Council of the National Academies|publisher=National Academies Press|year=2007|isbn=978-0-309-10635-1|location=Washington DC|pages=82–84}}</ref>

When drilling in temperate ice, thermal drills have an advantage over electromechanical (EM) drills: ice melted by pressure can refreeze on EM drill bits, reducing cutting efficiency, and can clog other parts of the mechanism.  EM drills are also more likely to fracture ice cores where the ice is under high stress.<ref>{{cite journal|last1=Schwikowski|first1=Margit|last2=Jenk|first2=Theo M.|last3=Stampfli|first3=Dieter|last4=Stampfli|first4=Felix|title=A new thermal drilling system for high-altitude or temperate glaciers|journal=Annals of Glaciology|date=26 July 2017|volume=55|issue=68|pages=131–136|doi=10.3189/2014AoG68A024|doi-access=free}}</ref>

When drilling deep holes, which require drilling fluid, the hole must be [[Engineering:Casing (borehole)|cased]] (fitted with a cylindrical lining), since otherwise the drilling fluid will be absorbed by the snow and firn.  The casing has to reach down to the impermeable ice layers.  To install casing a shallow auger can be used to create a pilot hole, which is then reamed (expanded) until it is wide enough to accept the casing; a large diameter auger can also be used, avoiding the need for reaming.  An alternative to casing is to use water in the borehole to saturate the porous snow and firn; the water eventually turns to ice.<ref name=":6" />

Ice cores from different depths are not all equally in demand by scientific investigators, which can lead to a shortage of ice cores at certain depths.  To address this, work has been done on technology to drill replicate cores: additional cores, retrieved by drilling into the sidewall of the borehole, at depths of particular interest.  Replicate cores were successfully retrieved at WAIS divide in the 2012–2013 drilling season, at four different depths.<ref>Anonymous (30 June 2017), Ice Drilling Design and Operations: Long Range Technology Plan, p. 24.</ref>

=== Large coring projects ===
The logistics of any coring project are complex because the locations are usually difficult to reach, and may be at high altitude.  The largest projects require years of planning and years to execute, and are usually run as international consortiums.  The [[Earth:East Greenland Ice-Core Project|EastGRIP]] project, for example, which as of 2017 is drilling in eastern Greenland, is run by the Centre for Ice and Climate ([[Organization:Niels Bohr Institute|Niels Bohr Institute]], [[Organization:University of Copenhagen|University of Copenhagen]]) in {{wipe|Denmark}},<ref>{{Cite web|url=http://eastgrip.org/|title=EastGrip – The East Greenland Ice-core Project|last=Petersen|first=Sandra|date=23 February 2016|website=East Greenland Ice Core Project|language=en|access-date=17 June 2017}}</ref> and includes representatives from 12 countries on its steering committee.<ref>{{Cite web|url=http://eastgrip.org/partners/|title=Partners|last=Madsen|first=Martin Vindbæk|date=14 April 2016|website=East Greenland Ice Core Project|language=en|access-date=17 June 2017|archive-url=https://web.archive.org/web/20170628113003/http://eastgrip.org/partners/|archive-date=28 June 2017|url-status=dead}}</ref> Over the course of a drilling season, scores of people work at the camp,<ref>{{harvnb|Dahl-Jensen|Kirk|Larsen|Sheldon|Steffensen|2016}}, pp. 17–19.</ref> and logistics support includes airlift capabilities provided by the US Air National Guard, using [[Engineering:Lockheed C-130 Hercules|Hercules transport planes]] owned by the [[Organization:National Science Foundation|National Science Foundation]].<ref>{{Cite web|url=http://eastgrip.org/about/|title=About EastGRIP|last=Petersen|first=Sandra|date=23 February 2016|website=East Greenland Ice Core Project|language=en|access-date=17 June 2017|archive-url=https://web.archive.org/web/20170628113110/http://eastgrip.org/about/|archive-date=28 June 2017|url-status=dead}}</ref> In 2015 the EastGRIP team moved the camp facilities from NEEM, a previous Greenland ice core drilling site, to the EastGRIP site.<ref>{{harvnb|Dahl-Jensen|Kirk|Larsen|Sheldon|Steffensen|2016}}, pp. 8–9.</ref> Drilling is expected to continue until at least 2020.<ref>{{Cite magazine|url=http://www.newyorker.com/magazine/2016/10/24/greenland-is-melting|title=When a Country Melts|last=Kolbert|first=Elizabeth|date=24 October 2016|magazine=The New Yorker|access-date=17 June 2017}}</ref>

== Core processing ==
[[File:Gripsaw.jpg|thumb|Sawing the [[Earth:Greenland ice core project|GRIP]] core|alt=Scientist standing at a bench, sawing an ice core]]

With some variation between projects, the following steps must occur between drilling and final storage of the ice core.<ref name=":7">{{Cite web|url=http://icecores.org/icecores/drilling.shtml|title=About Ice Cores :: Drilling Ice Cores|last=UNH|first=Joe Souney|publisher=National Ice Core Laboratory|language=en|access-date=21 May 2017|url-status=dead|archive-url=https://web.archive.org/web/20170504192232/http://icecores.org/icecores/drilling.shtml|archive-date=4 May 2017}}</ref>

The drill removes an annulus of ice around the core but does not cut under it. A spring-loaded lever arm called a core dog can break off the core and hold it in place while it is brought to the surface.  The core is then extracted from the drill barrel, usually by laying it out flat so that the core can slide out onto a prepared surface.<ref name=":7" /> The core must be cleaned of drilling fluid as it is slid out; for the [[Place:WAIS Divide|WAIS Divide]] coring project, a vacuuming system was set up to facilitate this.  The surface that receives the core should be aligned as accurately as possible with the drill barrel to minimise mechanical stress on the core, which can easily break.  The ambient temperature is kept well below freezing to avoid thermal shock.<ref name=":8">{{harvnb|Souney et al.|2014}}, pp. 16–19.</ref>

A log is kept with information about the core, including its length and the depth it was retrieved from, and the core may be marked to show its orientation.  It is usually cut into shorter sections, the standard length in the US being one metre.   The cores are then stored on site, usually in a space below snow level to simplify temperature maintenance, though additional refrigeration can be used.  If more drilling fluid must be removed, air may be blown over the cores.  Any samples needed for preliminary analysis are taken.  The core is then bagged, often in polythene, and stored for shipment.  Additional packing, including padding material, is added.  When the cores are flown from the drilling site, the aircraft's flight deck is unheated to help maintain a low temperature; when they are transported by ship they must be kept in a refrigeration unit.<ref name=":8" />

There are several locations around the world that store ice cores, such as the [[Organization:National Ice Core Laboratory|National Ice Core Laboratory]] in the US. These locations make samples available for testing.  A substantial fraction of each core is archived for future analyses.<ref name=":8" /><ref>{{Cite journal|last=Hinkley|first=Todd|date=9 December 2003|title=International ice core community meets to discuss best practices for ice core curation|journal=Eos Trans AGU|volume=84|issue=49|page=549|doi=10.1029/2003EO490006|bibcode=2003EOSTr..84..549H|doi-access=free}}.</ref>

=== Brittle ice ===
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 | image1    = CSIRO ScienceImage 518 Air Bubbles Trapped in Ice.jpg
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Over a depth range known as the brittle ice zone, bubbles of air are trapped in the ice under great pressure.  When the core is brought to the surface, the bubbles can exert a stress that exceeds the tensile strength of the ice, resulting in cracks and [[Chemistry:Spall|spall]].<ref name=":9" /> At greater depths, the air disappears into clathrates and the ice becomes stable again.<ref name=":9" /><ref>{{Cite journal|last1=Uchida|first1=Tsutomu|last2=Duval|first2=P.|last3=Lipenkov|first3=V.Ya.|last4=Hondoh|first4=T.|last5=Mae|first5=S.|last6=Shoji|first6=H.|year=1994|title=Brittle zone and air-hydrate formation in polar ice sheets|url=http://id.nii.ac.jp/1291/00002234/|journal=Memoirs of National Institute of Polar Research|volume=49 |issue=49|page=302}}.</ref> At the WAIS Divide site, the brittle ice zone was from 520&nbsp;m to 1340&nbsp;m depth.<ref name=":9">{{harvnb|Souney et al.|2014}}, pp. 20–21.</ref>

The brittle ice zone typically returns poorer quality samples than for the rest of the core.  Some steps can be taken to alleviate the problem.  Liners can be placed inside the drill barrel to enclose the core before it is brought to the surface, but this makes it difficult to clean off the drilling fluid.  In mineral drilling, special machinery can bring core samples to the surface at bottom-hole pressure, but this is too expensive for the inaccessible locations of most drilling sites.  Keeping the processing facilities at very low temperatures limits thermal shocks.  Cores are most brittle at the surface, so another approach is to break them into 1&nbsp;m lengths in the hole.  Extruding the core from the drill barrel into a net helps keep it together if it shatters. Brittle cores are also often allowed to rest in storage at the drill site for some time, up to a full year between drilling seasons, to let the ice gradually relax.<ref name=":9" /><ref>{{harvnb|Talalay|2016}}, pp. 265–266.</ref>

== Ice core data ==

=== Dating ===

Many different kinds of analysis are performed on ice cores, including visual layer counting, tests for [[Physics:Electrical resistivity and conductivity|electrical conductivity]] and physical properties, and assays for inclusion of gases, particles, [[Physics:Radionuclide|radionuclide]]s, and various molecular [[Chemistry:Chemical species|species]].  For the results of these tests to be useful in the reconstruction of palaeoenvironments, there has to be a way to determine the relationship between depth and age of the ice.  The simplest approach is to count layers of ice that correspond to the original annual layers of snow, but this is not always possible.  An alternative is to model the ice accumulation and flow to predict how long it takes a given snowfall to reach a particular depth.  Another method is to correlate radionuclides or trace atmospheric gases with other timescales such as periodicities in the earth's orbital parameters.<ref>{{cite book|url=http://ww2.valdosta.edu/~dmthieme/Geomorph/Walker_2005_QuaternaryDatingMethods.pdf|title=Quaternary Dating Methods|last=Walker|first=Mike|publisher=John Wiley & Sons|year=2005|isbn=978-0-470-86927-7|location=Chichester|page=150|url-status=dead|archive-url=https://web.archive.org/web/20140714195126/http://ww2.valdosta.edu/~dmthieme/Geomorph/Walker_2005_QuaternaryDatingMethods.pdf|archive-date=14 July 2014}}</ref>

A difficulty in ice core dating is that gases can [[Physics:Diffusion|diffuse]] through firn, so the ice at a given depth may be substantially older than the gases trapped in it.  As a result, there are two chronologies for a given ice core: one for the ice, and one for the trapped gases.  To determine the relationship between the two, models have been developed for the depth at which gases are trapped for a given location, but their predictions have not always proved reliable.<ref>{{cite journal|last1=Bazin|first1=L.|last2=Landais|first2=A.|last3=Lemieux-Dudon|first3=B.|last4=Toyé Mahamadou Kele|first4=H.|last5=Veres|first5=D.|last6=Parrenin|first6=F.|last7=Martinerie|first7=P.|last8=Ritz|first8=C.|last9=Capron|first9=E.|last10=Lipenkov|first10=V.|last11=Loutre|first11=M.-F.|last12=Raynaud|first12=D.|last13=Vinther|first13=B.|last14=Svensson|first14=A.|last15=Rasmussen|first15=S. O.|last16=Severi|first16=M.|last17=Blunier|first17=T.|last18=Leuenberger|first18=M.|last19=Fischer|first19=H.|last20=Masson-Delmotte|first20=V.|last21=Chappellaz|first21=J.|last22=Wolff|first22=E.|title=An optimized multi-proxy, multi-site Antarctic ice and gas orbital chronology (AICC2012): 120–800 ka|journal=Climate of the Past|date=1 August 2013|volume=9|issue=4|pages=1715–1731|doi=10.5194/cp-9-1715-2013|bibcode=2013CliPa...9.1715B|doi-access=free|hdl=2158/969431|hdl-access=free}}</ref><ref>{{harvnb|Jouzel|2013}}, pp. 2530–2531.</ref> At locations with very low snowfall, such as Vostok, the uncertainty in the difference between ages of ice and gas can be over 1,000 years.<ref>{{harvnb|Jouzel|2013}}, p. 2535.</ref>

The density and size of the bubbles trapped in ice provide an indication of crystal size at the time they formed.  The size of a crystal is related to its growth rate, which in turn depends on the temperature, so the properties of the bubbles can be combined with information on accumulation rates and firn density to calculate the temperature when the firn formed.<ref name=":21">{{harvnb|Alley|2010}}, p. 1098.</ref>

[[Physics:Radiocarbon dating|Radiocarbon dating]] can be used on the carbon in trapped {{chem|C|O|2}}.  In the polar ice sheets there is about 15–20&nbsp;µg of carbon in the form of {{chem|C|O|2}} in each kilogram of ice, and there may also be [[Chemistry:Carbonate|carbonate]] particles from wind-blown dust ([[Earth:Loess|loess]]).  The {{chem|C|O|2}} can be isolated by subliming the ice in a vacuum, keeping the temperature low enough to avoid the loess giving up any carbon.  The results have to be corrected for the presence of [[Physics:Carbon-14|{{Chem|14|C}}]] produced directly in the ice by cosmic rays, and the amount of correction depends strongly on the location of the ice core.  Corrections for {{Chem|14|C}} produced by nuclear testing have much less impact on the results.<ref>{{Cite journal|last1=Wilson|first1=A.T.|last2=Donahue|first2=D.J.|year=1992|title=AMS radiocarbon dating of ice: validity of the technique and the problem of cosmogenic ''in-situ'' production in polar ice cores|url=https://journals.uair.arizona.edu/index.php/radiocarbon/article/viewFile/1487/1491|journal=Radiocarbon|volume=34|issue=3|pages=431–435|doi=10.1017/S0033822200063657|bibcode=1992Radcb..34..431W |doi-access=free}}</ref> Carbon in [[Earth:Particulates|particulates]] can also be dated by separating and testing the water-insoluble [[Chemistry:Organic chemistry|organic]] components of dust. The very small quantities typically found require at least 300 g of ice to be used, limiting the ability of the technique to precisely assign an age to core depths.<ref>{{cite journal|last1=Uglietti|first1=Chiara|last2=Zapf|first2=Alexander|last3=Jenk|first3=Theo Manuel|last4=Sigl|first4=Michael|last5=Szidat|first5=Sönke|last6=Salazar|first6=Gary|last7=Schwikowski|first7=Margit|title=Radiocarbon dating of glacier ice: overview, optimisation, validation and potential|journal=The Cryosphere|date=21 December 2016|volume=10|issue=6|pages=3091–3105|doi=10.5194/tc-10-3091-2016|bibcode=2016TCry...10.3091U|doi-access=free}}</ref>

Timescales for ice cores from the same hemisphere can usually be synchronised using layers that include material from volcanic events.  It is more difficult to connect the timescales in different hemispheres.  The [[Earth:Laschamp event|Laschamp event]], a [[Earth:Geomagnetic reversal|geomagnetic reversal]] about 40,000 years ago, can be identified in cores;<ref>{{Cite news|url=https://phys.org/news/2012-10-extremely-reversal-geomagnetic-field-climate.html|title=An extremely brief reversal of the geomagnetic field, climate variability and a super volcano |work=Phys.org |date= 16 October 2012 |publisher=ScienceX network |access-date=29 May 2017}}</ref><ref>{{harvnb|Blunier et al.|2007}}, p. 325.</ref> away from that point, measurements of gases such as {{chem|C|H|4}} ([[Chemistry:Methane|methane]]) can be used to connect the chronology of a Greenland core (for example) with an Antarctic core.<ref>{{harvnb|Landais|Dreyfus|Capron|Pol|2012}}, pp. 191–192.</ref><ref>{{harvnb|Blunier et al.|2007}}, pp. 325–327.</ref> In cases where volcanic tephra is interspersed with ice, it can be dated using [[Physics:Argon–argon dating|argon/argon dating]] and hence provide fixed points for dating the ice.<ref name=":14">{{harvnb|Landais|Dreyfus|Capron|Pol|2012}}, p. 192.</ref><ref>{{Cite encyclopedia|encyclopedia=Encyclopedia of Quaternary Science|publisher=Elsevier|year=2013|editor-last=Elias|editor-first=Scott|location=Amsterdam|title=Volcanic Tephra Layers|editor-last2=Mock|editor-first2=Cary|isbn=9780444536426}}</ref> Uranium decay has also been used to date ice cores.<ref name=":14" /><ref>{{Cite journal|last=Aciego|first=S.|display-authors=et al.|date=15 April 2010|title=Toward a radiometric ice clock: U-series of the Dome C ice core|url=http://www.earth-prints.org/bitstream/2122/7786/1/mmc1.pdf|journal=TALDICE-EPICA Science Meeting|pages=1–2}}</ref> Another approach is to use [[Bayesian probability]] techniques to find the optimal combination of multiple independent records.  This approach was developed in 2010 and has since been turned into a software tool, DatIce.<ref>{{harvnb|Lowe |Walker|2014}}, p. 315.</ref><ref>{{cite conference|last1=Toyé Mahamadou Kele|first1=H.|display-authors=et al.|date=22 April 2012|title=Toward unified ice core chronologies with the DatIce tool|url=http://datice.gforge.inria.fr/pdf/EGU2012_BLAYO_LEMIEUX_TOYE.pdf|conference=EGU General Assembly 2012|location=Vienna, Austria|access-date=5 September 2017|archive-date=5 September 2017|archive-url=https://web.archive.org/web/20170905233004/http://datice.gforge.inria.fr/pdf/EGU2012_BLAYO_LEMIEUX_TOYE.pdf|url-status=dead}}</ref>

The boundary between the [[Earth:Quaternary extinction event|Pleistocene]] and the [[Earth:Holocene|Holocene]], about 11,700 years ago, is now formally defined with reference to data on Greenland ice cores.  Formal definitions of stratigraphic boundaries allow scientists in different locations to correlate their findings. These often involve fossil records, which are not present in ice cores, but cores have extremely precise [[Earth:Paleoclimatology|palaeoclimatic]] information that can be correlated with other climate proxies.<ref>{{cite journal|last1=Walker|first1=Mike|last2=Johnsen|first2=Sigfus|last3=Rasmussen|first3=Sune Olander|last4=Popp|first4=Trevor|last5=Steffensen|first5=Jørgen-Peder|last6=Gibbard|first6=Phil|last7=Hoek|first7=Wim|last8=Lowe|first8=John|last9=Andrews|first9=John|last10=Björck|first10=Svante|last11=Cwynar|first11=Les C.|last12=Hughen|first12=Konrad|last13=Kershaw|first13=Peter|last14=Kromer|first14=Bernd|last15=Litt|first15=Thomas|last16=Lowe|first16=David J.|last17=Nakagawa|first17=Takeshi|last18=Newnham|first18=Rewi|last19=Schwander|first19=Jakob|title=Formal definition and dating of the GSSP (Global Stratotype Section and Point) for the base of the Holocene using the Greenland NGRIP ice core, and selected auxiliary records|journal=Journal of Quaternary Science|date=January 2009|volume=24|issue=1|pages=3–17|doi=10.1002/jqs.1227|bibcode=2009JQS....24....3W|s2cid=40380068|doi-access=free}}</ref>

The dating of ice sheets has proved to be a key element in providing dates for palaeoclimatic records.  According to [[Biography:Richard Alley|Richard Alley]], "In many ways, ice cores are the 'rosetta stones' that allow development of a global network of accurately dated paleoclimatic records using the best ages determined anywhere on the planet".<ref name=":21" />

=== Visual analysis ===
[[File:GISP2 1855m ice core layers.png|thumb|19 cm long section of GISP 2 ice core from 1855&nbsp;m showing annual layer structure illuminated from below by a fibre optic source. Section contains 11 annual layers with summer layers (arrowed) sandwiched between darker winter layers.<ref>{{Cite web|url=http://www.ncdc.noaa.gov/paleo/slides/slideset/15/15_281_slide.html|title=Summer and winter core layers|last=Gow|first=Anthony|date=12 October 2001|publisher=NOAA|archive-url=https://web.archive.org/web/20100213035305/http://www.ncdc.noaa.gov/paleo/slides/slideset/15/15_281_slide.html|archive-date=13 February 2010}}</ref>|left|alt=A series of dark and light bands, with arrows identifying the lighter bands]]

Cores show visible layers, which correspond to annual snowfall at the core site.  If a pair of pits is dug in fresh snow with a thin wall between them and one of the pits is roofed over, an observer in the roofed pit will see the layers revealed by sunlight shining through.  A six-foot pit may show anything from less than a year of snow to several years of snow, depending on the location.  Poles left in the snow from year to year show the amount of accumulated snow each year, and this can be used to verify that the visible layer in a snow pit corresponds to a single year's snowfall.<ref>{{harvnb|Alley|2000}}, pp. 44–48.</ref>

In central Greenland a typical year might produce two or three feet of winter snow, plus a few inches of summer snow.  When this turns to ice, the two layers will make up no more than a foot of ice.  The layers corresponding to the summer snow will contain bigger bubbles than the winter layers, so the alternating layers remain visible, which makes it possible to count down a core and determine the age of each layer.<ref>{{harvnb|Alley|2000}}, p. 49.</ref> As the depth increases to the point where the ice structure changes to a clathrate, the bubbles are no longer visible, and the layers can no longer be seen.  Dust layers may now become visible.  Ice from Greenland cores contains dust carried by wind; the dust appears most strongly in late winter, and appears as cloudy grey layers.  These layers are stronger and easier to see at times in the past when the earth's climate was cold, dry, and windy.<ref>{{harvnb|Alley|2000}}, pp. 50–51.</ref>

Any method of counting layers eventually runs into difficulties as the flow of the ice causes the layers to become thinner and harder to see with increasing depth.<ref>{{harvnb|Alley|2000}}, p. 56.</ref> The problem is more acute at locations where accumulation is high; low accumulation sites, such as central Antarctica, must be dated by other methods.<ref name=":13" /> For example, at Vostok, layer counting is only possible down to an age of 55,000 years.<ref name=Ruddiman>{{Cite journal|last1=Ruddiman|first1=William F.|year=2003|title=A methane-based time scale for Vostok ice|url=http://moraymo.us/wp-content/uploads/2014/04/2003_ruddimanraymo.pdf|journal=Quaternary Science Reviews|volume=22|issue=2|pages=141–155|last2=Raymo|first2=Maureen E.|doi=10.1016/S0277-3791(02)00082-3|bibcode=2003QSRv...22..141R}}</ref>

When there is summer melting, the melted snow refreezes lower in the snow and firn, and the resulting layer of ice has very few bubbles so is easy to recognise in a visual examination of a core.  Identification of these layers, both visually and by measuring density of the core against depth, allows the calculation of a melt-feature percentage (MF): an MF of 100% would mean that every year's deposit of snow showed evidence of melting.  MF calculations are averaged over multiple sites or long time periods in order to smooth the data.  Plots of MF data over time reveal variations in the climate, and have shown that since the late 20th century melting rates have been increasing.<ref>{{harvnb|Jouzel|2013}}, p. 2533.</ref><ref>{{Cite journal|last=Fisher|first=David|year=2011|title=Recent melt rates of Canadian arctic ice caps are the highest in four millennia|url=http://arctic.eas.ualberta.ca/downloads/Fisheretal2011onlineGPC.pdf|journal=Global and Planetary Climate Change|volume=84–85|pages=1–4|doi=10.1016/j.gloplacha.2011.06.005}}</ref>

In addition to manual inspection and logging of features identified in a visual inspection, cores can be optically scanned so that a digital visual record is available.  This requires the core to be cut lengthwise, so that a flat surface is created.<ref>{{harvnb|Souney et al.|2014}}, p. 25.</ref>

===  Isotopic analysis ===
The isotopic composition of the oxygen in a core can be used to model the temperature history of the ice sheet.  Oxygen has three stable isotopes, {{chem|link=oxygen-16|16|O}}, {{chem|link=oxygen-17|17|O}} and {{chem|link=oxygen-18|18|O}}.<ref>{{Cite web|url=https://environmentalchemistry.com/yogi/periodic/O-pg2.html|last=Barbalace |first=Kenneth L.|title=Periodic Table of Elements: O – Oxygen |publisher=EnvironmentalChemistry.com|language=en-US|access-date=20 May 2017}}</ref> The ratio between {{chem|18|O}} and {{chem|16|O}} indicates the temperature when the snow fell.<ref name=":5">{{harvnb|Lowe |Walker|2014}}, pp. 165–170.</ref> Because {{chem|16|O}} is lighter than {{chem|18|O}}, water containing {{chem|16|O}} is slightly more likely to turn into vapour, and water containing {{chem|18|O}} is slightly more likely to condense from vapour into rain or snow crystals.  At lower temperatures, the difference is more pronounced.  The standard method of recording the {{chem|18|O}}/{{chem|16|O}} ratio is to subtract the ratio in a standard known as standard mean ocean water (SMOW):<ref name=":5" />

<math>\mathrm{\delta ^{18}O} = \Biggl( \mathrm{\frac{\bigl( \frac{^{18}O}{^{16}O} \bigr)_{sample}}{\bigl( \frac{^{18}O}{^{16}O} \bigr)_{SMOW}}} -1 \Biggr) \times 1000\ ^{o}\!/\!_{oo},</math>

where the ‰ sign indicates [[Parts per thousand|parts per thousand]].<ref name=":5" /> A sample with the same {{chem|18|O}}/{{chem|16|O}} ratio as SMOW has a {{delta|18|O}} of 0‰; a sample that is depleted in {{chem|18|O}} has a negative {{delta|18|O}}.<ref name=":5" /> Combining the {{delta|18|O}} measurements of an ice core sample with the borehole temperature at the depth it came from provides additional information, in some cases leading to significant corrections to the temperatures deduced from the {{delta|18|O}} data.<ref>{{harvnb|Alley|2000}}, pp. 65–70.</ref><ref name=":15" /> Not all boreholes can be used in these analyses. If the site has experienced significant melting in the past, the borehole will no longer preserve an accurate temperature record.<ref>{{harvnb|Alley|2010}}, p. 1097.</ref>

Hydrogen ratios can also be used to calculate a temperature history. [[Physics:Deuterium|Deuterium]] ({{chem|2|H}}, or D) is heavier than hydrogen ({{chem|1|H}}) and makes water more likely to condense and less likely to evaporate.  A {{delta|D}} ratio can be defined in the same way as {{delta|18|O}}.<ref>{{Cite web|url=http://www.iceandclimate.nbi.ku.dk/research/past_atmos/past_temperature_moisture/isotopes_delta_notation/|title=Isotopes and the delta notation|date=8 September 2009|publisher=Centre for Ice and Climate|language=en|access-date=25 May 2017|archive-date=10 July 2017|archive-url=https://web.archive.org/web/20170710163804/http://www.iceandclimate.nbi.ku.dk/research/past_atmos/past_temperature_moisture/isotopes_delta_notation|url-status=dead}}</ref><ref>{{Cite news|url=https://www.scientificamerican.com/article/how-are-past-temperatures/|first=Robert |last=Mulvaney|title=How are past temperatures determined from an ice core?|date=20 September 2004|publisher=Scientific American|access-date=25 May 2017|language=en}}</ref> There is a linear relationship between {{delta|18|O}} and {{delta|D}}:<ref name=":16">{{harvnb|Jouzel|2013}}, pp. 2533–2534.</ref>

<math>\mathrm{\delta D} = 8 \times \mathrm{\delta ^{18} O} + \mathrm{d},</math>

where d is the deuterium excess. It was once thought that this meant it was unnecessary to measure both ratios in a given core, but in 1979 Merlivat and Jouzel showed that the deuterium excess reflects the temperature, relative humidity, and wind speed of the ocean where the moisture originated. Since then it has been customary to measure both.<ref name=":16" />

Water isotope records, analyzed in cores from Camp Century and [[Earth:Dye 3|Dye 3]] in Greenland, were instrumental in the discovery of [[Earth:Dansgaard–Oeschger event|Dansgaard-Oeschger events]]—rapid warming at the onset of an [[Earth:Interglacial|interglacial]], followed by slower cooling.<ref>{{harvnb|Jouzel|2013}}, p. 2531.</ref> Other isotopic ratios have been studied, for example, the ratio between {{chem|13|C}} and {{chem|12|C}} can provide information about past changes in the [[Earth:Carbon cycle|carbon cycle]].  Combining this information with records of carbon dioxide levels, also obtained from ice cores, provides information about the mechanisms behind changes in {{chem|C|O|2}} over time.<ref>{{cite journal|last1=Bauska|first1=Thomas K.|last2=Baggenstos|first2=Daniel|last3=Brook|first3=Edward J.|last4=Mix|first4=Alan C.|last5=Marcott|first5=Shaun A.|last6=Petrenko|first6=Vasilii V.|last7=Schaefer|first7=Hinrich|last8=Severinghaus|first8=Jeffrey P.|last9=Lee|first9=James E.|title=Carbon isotopes characterize rapid changes in atmospheric carbon dioxide during the last deglaciation|journal=Proceedings of the National Academy of Sciences of the United States of America|date=29 March 2016|volume=113|issue=13|pages=3465–3470|doi=10.1073/pnas.1513868113|pmid=26976561|pmc=4822573|bibcode=2016PNAS..113.3465B|doi-access=free}}</ref>

=== Palaeoatmospheric sampling ===
[[File:Vostok Petit data.svg|thumb|Graph of CO<sub>2</sub> (green), reconstructed temperature (blue) and dust (red) from the Vostok ice core for the past 420,000 years|alt=Three graphs laid out one above the other; the CO<sub>2</sub> and temperature can be visually seen to be correlated; the dust graph is inversely correlated with the other two|300x300px]]
[[File:Greenland firn CFCs.png|thumb|Ozone-depleting gases in Greenland firn.<ref>{{Cite web|url=http://www.cpc.ncep.noaa.gov/products/assessments/assess_99/fig76.html|title=Climate Prediction Center – Expert Assessments|publisher=National Weather Service Climate Prediction Center|access-date=3 June 2017}}</ref>|alt=Graph showing the relationship between depth below surface, and fraction of surface concentration at the surface, for multiple gases|300x300px]]

It was understood in the 1960s that analyzing the air trapped in ice cores would provide useful information on the [[Earth:Paleoatmosphere|paleoatmosphere]], but it was not until the late 1970s that a reliable extraction method was developed.  Early results included a demonstration that the {{chem|C|O|2}} concentration was 30% less at the [[Earth:Last Glacial Maximum|last glacial maximum]] than just before the start of the industrial age.  Further research has demonstrated a reliable correlation between {{chem|C|O|2}} levels and the temperature calculated from ice isotope data.<ref name=":17">{{harvnb|Jouzel|2013}}, p. 2534.</ref>

Because {{chem|C|H|4}} (methane) is produced in lakes and [[Earth:Wetland|wetland]]s, the amount in the atmosphere is correlated with the strength of [[Earth:Monsoon|monsoon]]s, which are in turn correlated with the strength of low-latitude summer [[Astronomy:Solar irradiance|insolation]].  Since insolation depends on [[Earth:Milankovitch cycles|orbital cycles]], for which a timescale is available from other sources, {{chem|C|H|4}} can be used to determine the relationship between core depth and age.<ref name=":13" /><ref name=Ruddiman/>  {{chem|N|2|O}} (nitrous oxide) levels are also correlated with glacial cycles, though at low temperatures the graph differs somewhat from the {{chem|C|O|2}} and {{chem|C|H|4}} graphs.<ref name=":17" /><ref>{{Cite journal|last1=Schilt|first1=Adrian|first2=Matthias|last2=Baumgartner|first3=Thomas|last3=Blunierc|first4=Jakob|last4=Schwander|first5=Renato|last5=Spahni|first6=Hubertus|last6=Fischer|first7=Thomas F.|last7=Stocker|year=2009|title=Glacial-interglacial and millennial-scale variations in the atmospheric nitrous oxide concentration during the last 800,000 years|url=https://ic.ucsc.edu/~acr/ocea285/articles/Schiltetal2010.pdf|journal=Quaternary Science Reviews|volume=29|issue=1–2|pages=182–192|doi=10.1016/j.quascirev.2009.03.011|access-date=2 June 2017|archive-url=https://web.archive.org/web/20170808205625/https://ic.ucsc.edu/~acr/ocea285/articles/Schiltetal2010.pdf|archive-date=8 August 2017|url-status=dead}}</ref> Similarly, the ratio between {{chem|N|2}} (nitrogen) and {{chem|O|2}} (oxygen) can be used to date ice cores: as air is gradually trapped by the snow turning to firn and then ice, {{chem|O|2}} is lost more easily than {{chem|N|2}}, and the relative amount of {{chem|O|2}} correlates with the strength of local summer insolation.  This means that the trapped air retains, in the ratio of {{chem|O|2}} to {{chem|N|2}}, a record of the summer insolation, and hence combining this data with orbital cycle data establishes an ice core dating scheme.<ref name=":13" /><ref>{{harvnb|Landais|Dreyfus|Capron|Pol|2012}}, p. 191.</ref>

[[Physics:Diffusion|Diffusion]] within the firn layer causes other changes that can be measured.  Gravity causes heavier molecules to be enriched at the bottom of a gas column, with the amount of enrichment depending on the difference in mass between the molecules.  Colder temperatures cause heavier molecules to be more enriched at the bottom of a column.  These [[Fractionation|fractionation]] processes in trapped air, determined by the measurement of the {{chem|15|N}}/{{chem|14|N}} ratio and of [[Chemistry:Neon|neon]], [[Chemistry:Krypton|krypton]] and [[Chemistry:Xenon|xenon]], have been used to infer the thickness of the firn layer, and determine other palaeoclimatic information such as past mean ocean temperatures.<ref name=":15">{{harvnb|Jouzel|2013}}, p. 2532.</ref> Some gases such as [[Chemistry:Helium|helium]] can rapidly diffuse through ice, so it may be necessary to test for these "fugitive gases" within minutes of the core being retrieved to obtain accurate data.<ref name=":8" /> [[Earth:Chlorofluorocarbon|Chlorofluorocarbon]]s (CFCs), which contribute to the [[Earth:Greenhouse effect|greenhouse effect]] and also cause [[Earth:Ozone depletion|ozone loss]] in the [[Earth:Stratosphere|stratosphere]],<ref name=":20">{{Cite book|title=Climate Change and Climate Modeling|last=Neelin|first=J. David|publisher=Cambridge University Press|year=2010|isbn=978-0-521-84157-3|location=Cambridge|page=9}}</ref> can be detected in ice cores after about 1950; almost all CFCs in the atmosphere were created by human activity.<ref name=":20" /><ref>{{cite journal|last1=Martinerie|first1=P.|last2=Nourtier-Mazauric|first2=E.|last3=Barnola|first3=J.-M.|last4=Sturges|first4=W. T.|last5=Worton|first5=D. R.|last6=Atlas|first6=E.|last7=Gohar|first7=L. K.|last8=Shine|first8=K. P.|last9=Brasseur|first9=G. P.|title=Long-lived halocarbon trends and budgets from atmospheric chemistry modelling constrained with measurements in polar firn|journal=Atmospheric Chemistry and Physics|date=17 June 2009|volume=9|issue=12|pages=3911–3934|doi=10.5194/acp-9-3911-2009|bibcode=2009ACP.....9.3911M|doi-access=free}}</ref>

Greenland cores, during times of climatic transition, may show excess {{CO2}} in air bubbles when analysed, due to {{CO2}} production by acidic and alkaline impurities.<ref>{{Cite journal | doi=10.1034/j.1600-0889.1993.t01-3-00006.x| title=A natural artefact in Greenland ice-core {{CO2}} measurements| year=1993| last1=Delmas| first1=Robert J.| journal=Tellus B| volume=45| issue=4| pages=391–396}}</ref>

{{Clear}}

=== Glaciochemistry ===
Summer snow in Greenland contains some sea salt, blown from the surrounding waters; there is less of it in winter, when much of the sea surface is covered by pack ice.  Similarly, [[Chemistry:Hydrogen peroxide|hydrogen peroxide]] appears only in summer snow because its production in the atmosphere requires sunlight.  These seasonal changes can be detected because they lead to changes in the [[Physics:Electrical conductivity|electrical conductivity]] of the ice.  Placing two [[Physics:Electrode|electrode]]s with a high voltage between them on the surface of the ice core gives a measurement of the conductivity at that point. Dragging them down the length of the core, and recording the conductivity at each point, gives a graph that shows an annual periodicity.  Such graphs also identify chemical changes caused by non-seasonal events such as forest fires and major volcanic eruptions.  When a known volcanic event, such as the [[Earth:Laki#1783 eruption|eruption of Laki]] in Iceland in 1783, can be identified in the ice core record, it provides a cross-check on the age determined by layer counting.<ref>{{harvnb|Alley|2000}}, pp. 51–55.</ref> Material from Laki can be identified in Greenland ice cores, but did not spread as far as Antarctica; the 1815 eruption of Tambora in Indonesia injected material into the stratosphere, and can be identified in both Greenland and Antarctic ice cores.  If the date of the eruption is not known, but it can be identified in multiple cores, then dating the ice can in turn give a date for the eruption, which can then be used as a reference layer.<ref name=":22" /> This was done, for example, in an analysis of the climate for the period from 535 to 550 AD, which was thought to be influenced by an otherwise unknown tropical eruption in about 533 AD; but which turned out to be caused by two eruptions, one in 535 or early 536 AD, and a second one in 539 or 540 AD.<ref>{{cite journal|last1=Sigl|first1=M.|last2=Winstrup|first2=M.|last3=McConnell|first3=J. R.|last4=Welten|first4=K. C.|last5=Plunkett|first5=G.|last6=Ludlow|first6=F.|last7=Büntgen|first7=U.|last8=Caffee|first8=M.|last9=Chellman|first9=N.|last10=Dahl-Jensen|first10=D.|last11=Fischer|first11=H.|last12=Kipfstuhl|first12=S.|last13=Kostick|first13=C.|last14=Maselli|first14=O. J.|last15=Mekhaldi|first15=F.|last16=Mulvaney|first16=R.|last17=Muscheler|first17=R.|last18=Pasteris|first18=D. R.|last19=Pilcher|first19=J. R.|last20=Salzer|first20=M.|last21=Schüpbach|first21=S.|last22=Steffensen|first22=J. P.|last23=Vinther|first23=B. M.|last24=Woodruff|first24=T. E.|title=Timing and climate forcing of volcanic eruptions for the past 2,500 years|journal=Nature|date=8 July 2015|volume=523|issue=7562|pages=543–549|doi=10.1038/nature14565|pmid=26153860|bibcode=2015Natur.523..543S|s2cid=4462058|url=https://pure.qub.ac.uk/portal/en/publications/timing-and-climate-forcing-of-volcanic-eruptions-for-the-past-2500-years(04c84f13-a3c3-48e4-81ca-1507cdd4359d).html}}</ref> There are also more ancient reference points, such as the eruption of [[Earth:Lake Toba|Toba]] about 72,000 years ago.<ref name=":22">{{harvnb|Legrand|Mayewski|1997}}, pp. 222, 225.</ref>

Many other elements and molecules have been detected in ice cores.<ref name=":18" /> In 1969, it was discovered that [[Chemistry:Lead|lead]] levels in Greenland ice had increased by a factor of over 200 since pre-industrial times, and increases in other elements produced by industrial processes, such as [[Chemistry:Copper|copper]], [[Chemistry:Cadmium|cadmium]], and [[Chemistry:Zinc|zinc]], have also been recorded.<ref>{{harvnb|Legrand|Mayewski|1997}}, pp. 231–232.</ref> The presence of nitric and sulfuric acid ({{chem|link=nitric acid|H|N|O|3}} and {{chem|link=Sulfuric acid|H|2|S|O|4}}) in precipitation can be shown to correlate with increasing fuel [[Physics:Combustion|combustion]] over time.  [[Chemistry:Mesylate|Methanesulfonate]] (MSA) ({{chem|C|H|3|S|O|3|-}}) is produced in the atmosphere by marine organisms, so ice core records of MSA provide information on the history of the oceanic environment.  Both hydrogen peroxide ({{chem|link=hydrogen peroxide|H|2|O|2}}) and formaldehyde ({{chem|link=formaldehyde|H|C|H|O}}) have been studied, along with organic molecules such as [[Chemistry:Carbon black|carbon black]] that are linked to vegetation emissions and forest fires.<ref name=":18">{{harvnb|Legrand|Mayewski|1997}}, p. 221.</ref> Some species, such as [[Chemistry:Calcium|calcium]] and [[Chemistry:Ammonium|ammonium]], show strong seasonal variation.  In some cases there are contributions from more than one source to a given species: for example, Ca<sup>++</sup> comes from dust as well as from marine sources; the marine input is much greater than the dust input and so although the two sources peak at different times of the year, the overall signal shows a peak in the winter, when the marine input is at a maximum.<ref>{{harvnb|Legrand|Mayewski|1997}}, p. 222.</ref> Seasonal signals can be erased at sites where the accumulation is low, by surface winds; in these cases it is not possible to date individual layers of ice between two reference layers.<ref name=":19">{{harvnb|Legrand|Mayewski|1997}}, p. 225.</ref>

Some of the deposited chemical species may interact with the ice, so what is detected in an ice core is not necessarily what was originally deposited.  Examples include HCHO and {{chem|H|2|O|2}}.  Another complication is that in areas with low accumulation rates, deposition from fog can increase the concentration in the snow, sometimes to the point where the atmospheric concentration could be overestimated by a factor of two.<ref>{{harvnb|Legrand|Mayewski|1997}}, pp. 227–228.</ref>
{| class="wikitable"
|+Soluble impurities found in ice cores<ref>{{harvnb|Legrand|Mayewski|1997}}, p. 228.</ref>
!Source
!Via
!Measured in polar ice
|-
|Oceans
|Waves and wind
|Sea salt: {{chem|Na|+}}, {{chem|Cl|-}}, {{chem|Mg|2+}}, {{chem|Ca|2+}}, {{chem|S|O|4|2-}}, {{chem|K|+}}
|-
|Land
|Aridity and wind
|Terrestrial salts: {{chem|Mg|2+}}, {{chem|Ca|2+}}, {{chem|C|O|3|2-}}, {{chem|S|O|4|2-}}, [[Chemistry:Aluminosilicate|aluminosilicate]]s
|-
|Human and biological gas emissions: {{chem|S|O|2}}, {{chem|(|C|H|3|)|2|S}}, {{chem|H|2|S}}, {{chem|C|O|S}}, {{chem|N|O|x}}, {{chem|N|H|3}}, [[Chemistry:Hydrocarbon|hydrocarbon]]s and halocarbons 
|Atmospheric chemistry: {{chem|O|3}}, {{chem|H|2|O|2}}, {{chem|O|H}}, {{chem|R|O|2|link=Organic peroxide}}, {{chem|N|O|3}}, 
|{{chem|H|+}}, {{chem|N|H|4|+}}, {{chem|Cl|-}}, {{chem|N|O|3|-}}, {{chem|S|O|4|2-}}, {{chem|C|H|3|S|O|3|-}}, {{chem|F|-}}, {{chem|H|C|O|O|-}}, other organic compounds
|}

=== Radionuclides ===
[[File:Upper Fremont glacier ice cl36.gif|thumb|[[Chemistry:Chlorine|<sup>36</sup>Cl]] from 1960s nuclear testing in US glacier ice.|alt=Graph showing abundance of <sup>36</sup>Cl against snow depth, showing a spike at the time of above-ground nuclear testing|300x300px]]

Galactic cosmic rays produce {{chem|10|Be}} in the atmosphere at a rate that depends on the solar magnetic field.  The strength of the field is related to the intensity of [[Physics:Solar radiation|solar radiation]], so the level of {{chem|10|Be}} in the atmosphere is a [[Earth:Proxy (climate)|proxy]] for climate.  [[Physics:Accelerator mass spectrometry|Accelerator mass spectrometry]] can detect the low levels of {{chem|10|Be}} in ice cores, about 10,000 atoms in a gram of ice, and these can be used to provide long-term records of solar activity.<ref>{{Cite journal|last=Pedro|first=J.B.|year=2011|title=High-resolution records of the beryllium-10 solar activity proxy in ice from Law Dome, East Antarctica: measurement, reproducibility and principal trends|journal=Climate of the Past|volume=7|issue=3|pages=707–708|doi=10.5194/cp-7-707-2011|bibcode=2011CliPa...7..707P|doi-access=free}}</ref> [[Earth:Tritium radioluminescence|Tritium]] ({{chem|3|H}}), created by nuclear weapons testing in the 1950s and 1960s, has been identified in ice cores,<ref>{{cite journal|last1=Wagenhach|first1=D.|last2=Graf|first2=W.|last3=Minikin|first3=A.|last4=Trefzer|first4=U.|last5=Kipfstuhl|first5=J.|last6=Oerter|first6=H.|last7=Blindow|first7=N.|title=Reconnaissance of chemical and isotopic firn properties on top of Berkner Island, Antarctica|journal=Annals of Glaciology|date=20 January 2017|volume=20|pages=307–312|doi=10.3189/172756494794587401|doi-access=free}}</ref> and both [[Physics:Chlorine-36|<sup>36</sup>Cl]] and {{Chem|link=Plutonium-239|239|Pu}} have been found in ice cores in Antarctica and Greenland.<ref>{{cite journal|last1=Arienzo|first1=M. M.|last2=McConnell|first2=J. R.|last3=Chellman|first3=N.|last4=Criscitiello|first4=A. S.|last5=Curran|first5=M.|last6=Fritzsche|first6=D.|last7=Kipfstuhl|first7=S.|last8=Mulvaney|first8=R.|last9=Nolan|first9=M.|last10=Opel|first10=T.|last11=Sigl|first11=M.|last12=Steffensen|first12=J.P.|title=A Method for Continuous Pu Determinations in Arctic and Antarctic Ice Cores|journal=Environmental Science & Technology|date=5 July 2016|volume=50|issue=13|pages=7066–7073|doi=10.1021/acs.est.6b01108|pmid=27244483|bibcode=2016EnST...50.7066A|s2cid=206558530 |url=http://nora.nerc.ac.uk/id/eprint/513803/7/Arienzo_et_al_NWT_May2016_V1.pdf}}</ref><ref>Delmas et al. (2004), pp. 494–496.</ref><ref>{{Cite web|url=http://wwwbrr.cr.usgs.gov/projects/SW_corrosion/icecore/futurework.shtml|title=Future Work|date=14 January 2005|publisher=US Geological Survey Central Region Research|archive-url=https://web.archive.org/web/20050913192339/http://wwwbrr.cr.usgs.gov/projects/SW_corrosion/icecore/futurework.shtml|archive-date=13 September 2005}}</ref> Chlorine-36, which has a half-life of 301,000 years, has been used to date cores, as have krypton ({{Chem|link=krypton-85|85|Kr}}, with a half-life of 11 years), lead ({{Chem|link=lead-210|210|Pb}}, 22 years), and silicon ({{Chem|link=silicon-32|32|Si}}, 172 years).<ref name=":19" />

===  Other inclusions ===
Meteorites and micrometeorites that land on polar ice are sometimes concentrated by local environmental processes.  For example, there are places in Antarctica where winds evaporate surface ice, concentrating the solids that are left behind, including meteorites.  Meltwater ponds can also contain meteorites.  At the South Pole Station, ice in a well is melted to provide a water supply, leaving micrometeorites behind. These have been collected by a robotic "vacuum cleaner" and examined, leading to improved estimates of their flux and mass distribution.<ref>{{harvnb|Alley|2000}}, p. 73.</ref> The well is not an ice core, but the age of the ice that was melted is known, so the age of the recovered particles can be determined. The well becomes about 10 m deeper each year, so micrometeorites collected in a given year are about 100 years older than those from the previous year.<ref>{{cite report |last1=Taylor|first1=Susan |last2=Lever |first2=James H. |last3=Harvey |first3=Ralph P. |last4=Govoni |first4=John|date=May 1997 |title=Collecting micrometeorites from the South Pole Water Well|url=http://apps.dtic.mil/dtic/tr/fulltext/u2/a327829.pdf |archive-url=https://web.archive.org/web/20171011080819/http://www.dtic.mil/dtic/tr/fulltext/u2/a327829.pdf |url-status=live |archive-date=11 October 2017 |publisher=Cold Regions Research and Engineering Lab, Hanover, NH |pages=1–2 |docket=97–1 |access-date=14 September 2017 }}</ref> [[Biology:Pollen|Pollen]], an important component of sediment cores, can also be found in ice cores.  It provides information on changes in vegetation.<ref>{{cite journal|last1=Reese|first1=C.A.|last2=Liu|first2=K.B.|last3=Thompson|first3=L.G.|title=An ice-core pollen record showing vegetation response to Late-glacial and Holocene climate changes at Nevado Sajama, Bolivia|journal=Annals of Glaciology|date=26 July 2017|volume=54|issue=63|page=183|doi=10.3189/2013AoG63A375|doi-access=free}}</ref>

===  Physical properties ===
In addition to the impurities in a core and the isotopic composition of the water, the physical properties of the ice are examined.  Features such as crystal size and axis orientation can reveal the history of ice flow patterns in the ice sheet.  The crystal size can also be used to determine dates, though only in shallow cores.<ref>{{cite journal|last1=Okuyama|first1=Junichi|last2=Narita|first2=Hideki|last3=Hondoh|first3=Takeo|last4=Koerner|first4=Roy M.|title=Physical properties of the P96 ice core from Penny Ice Cap, Baffin Island, Canada, and derived climatic records|journal=Journal of Geophysical Research: Solid Earth|pages=6–1–6–2|date=February 2003|volume=108|issue=B2|doi=10.1029/2001JB001707|bibcode=2003JGRB..108.2090O|doi-access=free}}</ref>

== History ==

=== Early years ===
[[File:2000 core-repository02 hg.jpg|thumb|A store of core samples|alt=A man on a walkway between two high shelf racks loaded with ice core samples]]

In 1841 and 1842, Louis Agassiz drilled holes in the Unteraargletscher in the [[Place:Alps|Alps]]; these were drilled with iron rods and did not produce cores.  The deepest hole achieved was 60&nbsp;m.  On Erich von Drygalski's Antarctic expedition in 1902 and 1903, 30&nbsp;m holes were drilled in an iceberg south of the Kerguelen Islands and temperature readings were taken.  The first scientist to create a snow sampling tool was James E. Church, described by Pavel Talalay as "the father of modern snow surveying".  In the winter of 1908–1909, Church constructed steel tubes with slots and cutting heads to retrieve cores of snow up to 3&nbsp;m long.  Similar devices are in use today, modified to allow sampling to a depth of about 9&nbsp;m.  They are simply pushed into the snow and rotated by hand.<ref>{{harvnb|Talalay|2016}}, pp. 9–11.</ref>

The first systematic study of snow and firn layers was by Ernst Sorge, who was part of the Alfred Wegener Expedition to central Greenland in 1930–1931.  Sorge dug a 15&nbsp;m pit to examine the snow layers, and his results were later formalized into Sorge's Law of Densification by Henri Bader, who went on to do additional coring work in northwest Greenland in 1933.<ref>{{harvnb|Langway|2008}}, pp. 5–6.</ref> In the early 1950s, a SIPRE expedition took pit samples over much of the Greenland ice sheet, obtaining early oxygen isotope ratio data.  Three other expeditions in the 1950s began ice coring work: a joint Norwegian-British-Swedish Antarctic Expedition (NBSAE), in Queen Maud Land in Antarctica; the Juneau Ice Field Research Project (JIRP), in [[Earth:Alaska|Alaska]]; and Expéditions Polaires Françaises, in central Greenland.  Core quality was poor, but some scientific work was done on the retrieved ice.<ref>{{harvnb|Langway|2008}}, p. 7.</ref>

The [[Earth:International Geophysical Year|International Geophysical Year]] (1957–1958) saw increased [[Earth:Glaciology|glaciology]] research around the world, with one of the high priority research targets being deep cores in polar regions.  SIPRE conducted pilot drilling trials in 1956 (to 305 m) and 1957 (to 411 m) at Site 2 in Greenland; the second core, with the benefit of the previous year's drilling experience, was retrieved in much better condition, with fewer gaps.<ref>{{harvnb|Langway|2008}}, pp. 9–11.</ref> In Antarctica, a 307&nbsp;m core was drilled at Byrd Station in 1957–1958, and a 264&nbsp;m core at Little America V, on the [[Earth:Ross Ice Shelf|Ross Ice Shelf]], the following year.<ref>{{harvnb|Langway|2008}}, pp. 14–15.</ref> The success of the IGY core drilling led to increased interest in improving ice coring capabilities, and was followed by a CRREL project at Camp Century, where in the early 1960s three holes were drilled, the deepest reaching the base of the ice sheet at 1387&nbsp;m in July 1966.<ref>{{harvnb|Langway|2008}}, pp. 17–20.</ref> The drill used at Camp Century then went to Byrd Station, where a 2164&nbsp;m hole was drilled to bedrock before the drill was frozen into the borehole by sub-ice meltwater and had to be abandoned.<ref>{{harvnb|Langway|2008}}, p. 23.</ref>

French, Australian and Canadian projects from the 1960s and 1970s include a 905&nbsp;m core at [[Place:Dome C|Dome C]] in Antarctica, drilled by CNRS; cores at [[Earth:Law Dome|Law Dome]] drilled by ANARE, starting in 1969 with a 382&nbsp;m core; and Devon Ice Cap cores recovered by a Canadian team in the 1970s.<ref name=":10" />

=== Antarctica deep cores ===
[[File:Co2 glacial cycles 800k.png|thumb|Composite data for Dome C, CO<sub>2</sub> levels (ppm) going back nearly 800,000 years, and related glacial cycles.|left|alt=Graph showing CO<sub>2</sub> levels, highlit to indicate glacial cycles|300x300px]]

[[Place:Soviet Union|Soviet]] ice drilling projects began in the 1950s, in Franz Josef Land, the Urals, Novaya Zemlya, and at Mirny and Vostok in the Antarctic; not all these early holes retrieved cores.<ref>{{harvnb|Ueda|Talalay|2007}}, pp. 3–5.</ref> Over the following decades work continued at multiple locations in Asia.<ref>{{harvnb|Ueda|Talalay|2007}}, pp. 50–58.</ref> Drilling in the Antarctic focused mostly on Mirny and Vostok, with a series of deep holes at Vostok begun in 1970.<ref>{{harvnb|Ueda|Talalay|2007}}, pp. 3–26.</ref> The first deep hole at Vostok reached 506.9&nbsp;m in April 1970; by 1973 a depth of 952&nbsp;m had been reached.  A subsequent hole, Vostok 2, drilled from 1971 to 1976, reached 450&nbsp;m, and Vostok 3 reached 2202&nbsp;m in 1985 after six drilling seasons.<ref>{{harvnb|Ueda|Talalay|2007}}, p. 11.</ref> Vostok 3 was the first core to retrieve ice from the previous glacial period, 150,000 years ago.<ref name=":11" /> Drilling was interrupted by a fire at the camp in 1982, but further drilling began in 1984, eventually reaching 2546&nbsp;m in 1989. A fifth Vostok core was begun in 1990, reached 3661&nbsp;m in 2007, and was later extended to 3769&nbsp;m.<ref name=":10">{{harvnb|Jouzel|2013}}, p. 2527.</ref><ref name=":11" /> The estimated age of the ice is 420,000 years at 3310&nbsp;m depth; below that point it is difficult to interpret the data reliably because of mixing of the ice.<ref name=":12">{{harvnb|Jouzel|2013}}, p. 2529.</ref>

[[File:EPICA delta D plot.svg|thumb|The EPICA Dome C and Vostok ice cores compared|400px]]

EPICA, a European ice coring collaboration, was formed in the 1990s, and two holes were drilled in East Antarctica: one at Dome C, which reached 2871&nbsp;m in only two seasons of drilling, but which took another four years to reach bedrock at 3260 m; and one at Kohnen Station, which reached bedrock at 2760&nbsp;m in 2006.  The Dome C core had very low accumulation rates, which mean that the climate record extended a long way; by the end of the project the usable data extended to 800,000 years ago.<ref name=":12" />

Other deep Antarctic cores included a Japanese project at [[Place:Dome F|Dome F]], which reached 2503&nbsp;m in 1996, with an estimated age of 330,000 years for the bottom of the core; and a subsequent hole at the same site which reached 3035&nbsp;m in 2006, estimated to reach ice 720,000 years old.<ref name=":12" /> US teams drilled at [[Engineering:McMurdo Station|McMurdo Station]] in the 1990s, and at Taylor Dome (554&nbsp;m in 1994) and [[Place:Siple Dome|Siple Dome]] (1004&nbsp;m in 1999), with both cores reaching ice from the last glacial period.<ref name=":12" /><ref>{{Cite journal|last1=Bentley|first1=Charles R.|last2=Koci|first2=Bruce R.|year=2007|title=Drilling to the beds of the Greenland and Antarctic ice sheets: a review|journal=Annals of Glaciology|volume=47|issue=1|pages=3–4|doi=10.3189/172756407786857695|bibcode=2007AnGla..47....1B|doi-access=free}}</ref> The West Antarctic Ice Sheet (WAIS) project, completed in 2011, reached 3405 m; the site has high snow accumulation so the ice only extends back 62,000 years, but as a consequence, the core provides high resolution data for the period it covers.<ref name=":13">{{harvnb|Jouzel|2013}}, p. 2530.</ref> A 948&nbsp;m core was drilled at Berkner Island by a project managed by the British Antarctic Survey from 2002 to 2005, extending into the last glacial period;<ref name=":13" /> and an Italian-managed ITASE project completed a 1620&nbsp;m core at [[Place:Talos Dome|Talos Dome]] in 2007.<ref name=":13" /><ref>{{Cite web|url=http://www.taldice.org/site/index.php|title=TALos Dome Ice CorE – TALDICE|last=Iaccarino|first=Tony|publisher=Talos Dome Ice Core|access-date=28 May 2017}}</ref>

In 2016, cores were retrieved from the Allan Hills in Antarctica in an area where old ice lay near the surface.  The cores were dated by potassium-argon dating; traditional ice core dating is not possible as not all layers were present.  The oldest core was found to include ice from 2.7 million years ago—by far the oldest ice yet dated from a core.<ref>{{Cite news|url=https://www.science.org/content/article/record-shattering-27-million-year-old-ice-core-reveals-start-ice-ages|title=Record-shattering 2.7-million-year-old ice core reveals start of the ice ages|date=14 August 2017|work=Science |publisher= AAAS|access-date=30 August 2017|language=en}}</ref>

=== Greenland deep cores ===
In 1970, scientific discussions began which resulted in the [[Earth:Greenland Ice Sheet Project|Greenland Ice Sheet Project]] (GISP), a multinational investigation into the Greenland ice sheet that lasted until 1981.  Years of field work were required to determine the ideal location for a deep core; the field work included several intermediate-depth cores, at Dye 3 (372&nbsp;m in 1971), Milcent (398&nbsp;m in 1973) and Crete (405&nbsp;m in 1974), among others.  A location in north-central Greenland was selected as ideal, but financial constraints forced the group to drill at Dye 3 instead, beginning in 1979.  The hole reached bedrock at 2037&nbsp;m, in 1981.  Two holes, 30&nbsp;km apart, were eventually drilled at the north-central location in the early 1990s by two groups: GRIP, a European consortium, and GISP-2, a group of US universities.  GRIP reached bedrock at 3029&nbsp;m in 1992, and GISP-2 reached bedrock at 3053&nbsp;m the following year.<ref>{{harvnb|Langway|2008}}, pp. 27–28.</ref> Both cores were limited to about 100,000 years of climatic information, and since this was thought to be connected to the topography of the rock underlying the ice sheet at the drill sites, a new site was selected 200&nbsp;km north of GRIP, and a new project, [[Earth:North Greenland Ice Core Project|NorthGRIP]], was launched as an international consortium led by Denmark.  Drilling began in 1996; the first hole had to be abandoned at 1400&nbsp;m in 1997, and a new hole was begun in 1999, reaching 3085&nbsp;m in 2003.  The hole did not reach bedrock, but terminated at a subglacial river.  The core provided climatic data back to 123,000 years ago, which covered part of the last interglacial period.  The subsequent North Greenland Eemian (NEEM) project retrieved a 2537&nbsp;m core in 2010 from a site further north, extending the climatic record to 128,500 years ago;<ref name=":11">{{harvnb|Jouzel|2013}}, p. 2528.</ref> NEEM was followed by [[Earth:East Greenland Ice-Core Project|EastGRIP]], which began in 2015 in east Greenland and was planned to be completed in 2020.<ref>{{Cite web|url=http://eastgrip.org/documentation/|title=Documentation|last=Madsen|first=Martin Vindbæk|date=15 March 2016|publisher=East Greenland Ice Core Project|language=en|access-date=17 March 2017|archive-url=https://web.archive.org/web/20170318090450/http://eastgrip.org/documentation/|archive-date=18 March 2017|url-status=dead}}</ref>
In March 2020, the 2020 EGRIP field campaign was cancelled due to the ongoing COVID-19 pandemic. EastGRIP reopened for field work in 2022, where the CryoEgg reached new depths in the ice, under pressures in excess of 200 bar and temperatures of around -30c.<ref>{{cite web|url=https://eastgrip.org/FieldDiaries/2022diaries/2022-05-07.html|title=Finally, put in at EGRIP|access-date=2023-08-21}}</ref><ref>{{Cite web|url=https://protronix.co.uk/surviving-harsh-operating-conditions-how-protronix-ems-is-powering-cutting-edge-research-in-east-greenland/|title=Surviving Harsh Operating Conditions: How Protronix EMS is Powering Cutting-Edge Research in East Greenland &#124; Protronix EMS|website=protronix.co.uk/}}</ref>

=== Non-polar cores ===
Ice cores have been drilled at locations away from the poles, notably in the Himalayas and the [[Place:Andes|Andes]].  Some of these cores reach back to the last glacial period, but they are more important as records of [[Earth:El Niño|El Niño]] events and of monsoon seasons in south Asia.<ref name=":13" /> Cores have also been drilled on [[Earth:Mount Kilimanjaro|Mount Kilimanjaro]],<ref name=":13" /> in the Alps,<ref name=":13" /> and in Indonesia,<ref>{{harvnb|MacKinnon|1980}}, p. 41.</ref> New Zealand,<ref>{{harvnb|MacKinnon|1980}}, p. 42.</ref> Iceland,<ref>{{harvnb|MacKinnon|1980}}, p. 36.</ref> Scandinavia,<ref>{{harvnb|MacKinnon|1980}}, p. 39.</ref> Canada,<ref>{{harvnb|MacKinnon|1980}}, p. 26-29.</ref> and the US.<ref>{{harvnb|MacKinnon|1980}}, p. 30.</ref>

== Future plans ==
IPICS (International Partnerships in Ice Core Sciences) has produced a series of white papers outlining future challenges and scientific goals for the ice core science community.  These include plans to:<ref>{{Cite news|url=http://pastglobalchanges.org/ini/end-aff/ipics/white-papers|title=IPICS White Papers|publisher=PAGES – Past Global Changes|access-date=17 June 2017|language=en-gb|archive-url=https://web.archive.org/web/20171011080822/http://pastglobalchanges.org/ini/end-aff/ipics/white-papers|archive-date=11 October 2017|url-status=dead}}</ref>
* Retrieve ice cores that reach back over 1.2 million years, in order to obtain multiple iterations of ice core record for the 40,000-year long climate cycles known to have operated at that time.  Current cores reach back over 800,000 years, and show 100,000-year cycles.
* Improve ice core chronologies, including connecting chronologies of multiple cores.
* Identify additional proxies from ice cores, for example for sea ice, marine biological productivity, or forest fires.
* Drill additional cores to provide high-resolution data for the last 2,000 years, to use as input for detailed climate modelling.
* Identify an improved drilling fluid
* Improve the ability to handle brittle ice, both while drilling and in transport and storage
* Find a way to handle cores which have pressurised water at bedrock
* Come up with a standardised lightweight drill capable of drilling both wet and dry holes, and able to reach depths of up to 1000 m.
* Improve core handling to maximise the information that can be obtained from each core.

==See also==
* [[Earth:List of ice cores|List of ice cores]]
* [[Earth:Ice drilling|Ice drilling]]

== References ==
<references />

==Sources==
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{{Refend}}

==External links==
* [https://www.youtube.com/watch?v=JS2PhRd_5NA US National Ice Core Laboratory video showing storage and processing of cores]
* [http://www.ncdc.noaa.gov/paleo/icgate.html Ice Core Gateway]
* [http://www-bprc.mps.ohio-state.edu/Icecore/ Byrd Polar Research Center – Ice Core Paleoclimatology Research Group]
* [https://www.carbonbrief.org/factcheck-what-greenland-ice-cores-say-about-past-and-present-climate-change A misleading graph has been circling the internet since at least 2010]
* [https://www.science.org/content/article/world-s-oldest-ice-core-could-solve-mystery-flipped-ice-age-cycles A 2.7 million year old core]
* [https://www.livescience.com/65188-antarctica-drilling-oldest-ice.html Beyond EPICA-Oldest Ice mission]
* [https://www.sciencedaily.com/releases/2017/12/171213104607.htm Third Pole ice]

{{Chronology}}
{{Glaciers}}


{{DEFAULTSORT:Ice Core}}
[[Category:Water ice|Core]]
[[Category:Glaciology]]

{{Sourceattribution|Ice core}}