Motivation

The Journal of Glaciology is a disciplinary or archival journal. More often than not, papers with the highest impact and highest press coverage are published elsewhere, but the fundamental science underlying those ‘news’ papers is published in the Journal or the Annals of Glaciology. The value of such disciplinary journals is too often under estimated; they represent an absolutely essential part of science.

Based on anecdotal evidence and personal experience, I doubt that the public has ever had a deep and broad understanding of the large number and great strength of the procedures we scientists use to make it as hard as possible for us to fool ourselves. However, I believe that over my career there has been a decrease in the number of people willing to assume that we have such procedures and that we do due diligence implementing them.

Consider one example of many. Recently, I was quoted in public discussing how ice-shelf loss from warming removes ‘frictional’ buttressing, allowing faster flow of non-floating ice streams contributing to sea level rise. A correspondent then suggested that I should go back to school and learn what ‘to float’ means, arguing that melting of an ice cube in a glass does not raise the water level, so melting of an ice shelf cannot possibly raise sea level, so I must be deeply confused or worse. In my experience, in previous decades the correspondent might have assumed that flotation was part of my education, and thus might have paid attention at least long enough to hear the explanation about friction and ice streams, rather than immediately assuming that I must be wrong or mendacious.

Among many implications of this shift in the response of at least some members of the public to science, I believe that all of us in the scientific community, with special emphasis on our students, must improve our ability and willingness to explain: (1) the scientific basis of our particular public statements; and (2) the basis of science testing hypotheses against nature, peer -reviewed publication with sufficient details to allow replication, actual replication, and unpaid public assessment of science as practiced by the national academies of science or the Intergovernmental Panel on Climate Change (IPCC). Additional elements of our science are also worth communicating, including peer-reviewed funding, long apprenticeships typically involving more than one advisor, interlaboratory comparisons, international collaboration and our practice of giving our biggest awards and honors to those who demonstrate the shortcomings of their elders.

Students may find it enjoyable to learn much of this information by considering history, and 200 issues of the Journal of Glaciology over 60years offer an excellent opportunity to review some of that history. I was asked here to review some aspects of ice-core science. Consistent with other subdisciplines covered by the Journal, ice-core science is broadly important, underlying key parts of the wider science of climate change and figuring prominently in assessments such as the IPCC reports. Like those other subdisciplines, the quality of ice-core science is outstanding. Important parts of that history have been written in disciplinary journals such as the Journal and Annals of Glaciology, including the two Annals volumes dedicated to ice cores (Reference OeschgerOeschger, 1988; Reference WolffWolff, 2002; with a third planned for the 2012 International Partnerships in Ice-Core Science meeting). Here, after brief mention of some general ice-core history, I will highlight a few of the many reasons why ice- core results are so highly reliable through review of some of the historically key advances. My presentation is meant to be informative rather than exhaustive.

Ice Coring

The fascinating history of ice-core science is being written, if slowly. The recent contributions by Reference DansgaardDansgaard (2005) and Reference LangwayLangway (2008) are especially relevant. The interested reader may enjoy exploring the web resources at the American Institute of Physics (http://www.aip.org/history/sloan/icedrill/index.html). (Additional historical insights by one of the pioneers were originally scheduled for this volume, but outgrew the venue and are being prepared for publication elsewhere.)

Ice ‘coring’ is often traced back to Ernst Sorge, who overwintered at Eismitte in Greenland during the 1930/31 expedition led by Alfred Wegener (Reference LangwayLangway, 2008). There, Sorge excavated by hand a 15 m deep snow pit without falling in and damaging himself. He identified annual layers, measured densities and collected the data that led to Sorge’s law, calculating the densification rate from the modern depth-density profile and accumulation rate by assuming steady state (Reference BaderBader, 1954).

As reported by Reference Coachman, Enns and ScholanderLangway (2008), subsequent notable efforts in about 1950 led to ice coring to ˜100m by the Norwegian-British-Swedish Antarctic Expedition along the Dronning Maud Land coast, by the Juneau Ice Field Research Project on Taku Glacier in Alaska and by the Expeditions Polaires Francaises at Camp VI and Station Central in Greenland. Reference Coachman, Enns and ScholanderLangway (2008, p. 7) noted that all three involved ‘exhaustive efforts and marginal success’ in recovering high-quality core rapidly. I have been involved in ice-core science in some capacity for over 30 years and have heard many people say some version of ‘This should be easy’ – but it isn’t! The successes achieved are testament to triumphs in science, engineering, organization, funding, international collaboration and more, by people who combined brilliance with remarkable tenacity (Fig. 1).

Fig. 1. The late Bruce Koci, one of the unsung heroes of ice-core science, recovering a ˜100m core at site A, Greenland, 1985. Photograph by R. Alley.

Corings through the Greenland ice sheet at Camp Century by 1966 and through the Antarctic ice sheet at Byrd Station in 1968 were highly successful and contributed important scientific results. Numerous people made these triumphs possible: H. Ueda, D. Garfield, C. Langway and Seligman Crystal recipients A.J. Gow and L. Hansen are among those deserving special mention. H. Bader, also a recipient of the Seligman Crystal, was instrumental in the deep drilling. The contributions of numerous other ice-core pioneers, including Seligman laureates W. Dansgaard, H. Oeschger, S.J. Johnsen, C.J. Lorius, L.G. Thompson and P.A. Mayewski, deserve further attention.

Many of these contributions were made as part of a string of large and highly successful deep coring projects. In Greenland (Fig. 2), these include GRIP (e.g. Reference JohnsenJohnsen and others, 1992), GISP2 (e.g. Reference TaylorTaylor and others, 1993) and NorthGRIP (e.g. NorthGRIP Members, 2004);in Antarctica, these include Vostok (e.g. Reference PetitPetit and others, 1999), EPICA Dome C (e.g. EPICA Community Members, 2004), EPICA Dronning Maud Land (e.g. EPICA Community Members, 2006), WAISCORES (e.g. Reference Severinghaus, Beaudette, Headly, Taylor and Brook.Severinghaus and others, 2009) and Dome F (e.g. Reference KawamuraKawamura and others, 2007). These projects have demonstrated the tight coupling between climate and CO₂ over 800 000years, the hugely anomalous nature of the recent rise in CO₂ compared with natural shifts over that time, the reality of abrupt climate change and the global reach of its effects, and so much more. Such results are among the most important parts of climate science, and surely deserve a more thorough historical treatment.

Fig. 2. Drill camp at site A, Greenland, 1985. The cold central regions of Greenland are ideal for borehole thermometry and other techniques of ice-core paleoclimatology. Site A was studied by European and US teams as part of the site-selection activities for GRIP and GISP2. Photograph by R. Alley.

Here, however, I wish to focus on the reliability of the paleoclimatic records, rather than on the heroics of obtaining them or their immense value. Reliability was a main focus of those Seligman laureates and of many other researchers. Ice-core data enjoy a special place in discussions of paleoclimatology by providing especially reliable multi-parameter reconstructions with small quantifiable uncertainties. The small uncertainties in turn are achieved by developing indicators that are more actualistic than uniformitarian, as discussed next.

The Ice-Core History of Local Temperature and Snowfall

Geologists have often distinguished between actualism, the assumption of constancy of physical law, and uniformitarianism, the assumption of near-constancy of rates or intensities of processes over time (e.g. Reference Bates and JacksonBates and Jackson, 1980). There is no sharp line separating these, but we can usually tell where we are on the continuum between them.

Consider paleothermometry from tree-ring width, which is an indicator toward the uniformitarian end of the spectrum (e.g. see Reference BradleyBradley, 1999). In cold places, a tree may grow more rapidly in a warmer year, for biologically sensible reasons. A regression of recent growth rates against recent temperatures will calibrate the relationship. Normally, some data will be held out of the calibration and used to test the relation. If the test is successful, the calibration can be applied to a longer history of ring widths to reconstruct temperatures prior to instrumental data, assuming that the calibration has remained unchanged over time.

Tree growth may respond to changes in many other factors, however, including moisture availability, nutrient supply, weather extremes, seasonality of climate, atmospheric composition, pests, competition including introduced species, pollutants, and much more. It is not hard to think of many ways in which a change in tree growth could deviate from the recent instrumental calibration. Of course, the scientists working on tree rings are very well aware of this and are careful in site selection, searching for other causes, and replicating in many places. Comparison of several independent indicators in a region is especially valuable. For example, agreement among tree rings, pollen spectra, chironomids and other archives makes it more likely that the desired climate signal is being extracted. Still, ‘maybe something in addition to temperature changed’ is a hard argument to refute.

The δ¹⁸O or δD of ice-core ice is another indicator on the uniformitarian end of the spectrum. The physical basis for a dependence on temperature is very strong, surveys over short times and over space show good correlations, and atmospheric models of varying complexity tend to confirm this behavior (e.g. see Reference JouzelJouzel and others, 1997; Reference Alley, Cuffey, Valley and ColeAlley and Cuffey, 2001). As with tree rings, reconstructions of climate with very high time resolution are possible. However, changing source location or source temperature for the moisture in snowfall, seasonality of accumulation and other processes can also shift those isotopic ratios, so interpretation of past temperature from isotopic ratios alone includes possible systematic errors that may be difficult to evaluate but large compared with measurement or calibration errors.

Borehole temperatures offer a more-nearly actualistic indicator: the ice 100 m down in Greenland has not finished warming from the Little Ice Age, the ice halfway to the bed has not finished warming from the Ice Age, and these temperature anomalies are strong indications of the former cold. Heat flow is a well-understood physical process, and the effects of ice flow are often not unduly complicating (e.g. Reference RobinRobin, 1955). Ice-core observations reveal clearly whether significant melting has occurred and whether widespread crevassing occurred (e.g. Reference Voigt, Alley, Anandakrishnan and SpencerVoigt and others, 2003);in their absence, air temperatures and near-surface snow temperatures are similar. The possibility of using the borehole temperatures in hypothesis-testing about past climate changes has long been clear and compelling (Reference JohnsenJohnsen, 1977). A major difficulty is the low time resolution of the borehole record, together with the non-uniqueness of mathematical inversions to learn the past surface-temperature history from the modern temperature-depth profile.

One of the seminal papers in paleoclimatology, Reference Paterson and ClarkePaterson and Clarke (1978), showed a novel path to solving the challenge of interpreting temperature profiles. They combined borehole and oxygen-isotopic paleothermometry, adjusting the relation between δ⁸O and temperature to obtain an optimal fit of modeled to measured temperature- depth profiles; the history of δ¹⁸O provided the time schedule and relative amplitude for climate changes, and the borehole thermometry provided the absolute calibration. The Devon Island (Canada) sites they studied experienced notable melting, and the effects of that melting on the temperature profile proved to be more important than the detailed calibration of the isotopic record. Reference Paterson and ClarkePaterson and Clarke (1978) thus noted, ‘this test shows that the Devon Island boreholes are unsuitable for testing the applicability of any particular value of b [the intercept in the assumed linear relation between δ¹⁸O and temperature]. This is because variations in the latent heat released by refreezing of meltwater are much more important than variations in surface temperature in determining the temperature distribution. Such a test should be made at a place where melting is negligible’ (p. 629-630).

Clearly, central Greenland satisfies the criterion suggested by Reference Paterson and ClarkePaterson and Clarke (1978). Reference Cuffey, Alley, Grootes and AnandakrishnanCuffey and others (1992, Reference Cuffey, Alley, Grootes, Bolzan and Anandakrishnan1994, Reference Cuffey, Clow, Alley, Stuiver, Waddington and Saltus1995) and Reference Johnsen, Dahl-Jenson, Dansgaard and GundestrupJohnsen and others (1995) applied the Paterson-Clarke technique to the GISP2 and GRIP sites, respectively. They showed successfully that calibration of the modern isotopic ratios using spatial covariation can lead to twofold or larger errors, that the uniformitarian hypothesis introduces much larger errors than indicated by a formal statistical analysis of the calibration, and thus that factors in addition to temperature change were recorded in the isotopic record. (Changes in seasonality of precipitation seem to have been especially important;e.g. Reference Fawcett, Agustsdottir, Alley and ShumanFawcett and others, 1997.)

It is instructive to note that when I was writing this (21 October 2010), the ISI Web of Science listed just 23 citations of the seminal paper of Paterson and Clarke suggesting the idea of joint interpretation of the isotopic and borehole-temperature records. (Ten of those citations were from papers published in the Journal of Glaciology or Annals of Glaciology.) An additional 75 citations were indexed to the Reference Cuffey, Alley, Grootes, Bolzan and AnandakrishnanCuffey and others (1994) paper in the Journal of Glaciology reintroducing the technique in the context of Greenland (seven of those citations were from papers in the Journal or Annals of Glaciology; this put the Cuffey and others paper as one of the more highly cited in Journal history). However, 249 citations were indexed to the Reference Cuffey, Alley, Grootes, Bolzan and AnandakrishnanCuffey and others (1995) paper and 304 to the Reference Johnsen, Dahl-Jenson, Dansgaard and GundestrupJohnsen and others (1995) paper demonstrating just how cold the Ice Age was in Greenland (with just over 7% of those from the Journal or Annals of Glaciology). This demonstrates that citation counts do not provide a complete picture of the progress of science. (As a historical note, the collaboration of Stan Paterson, now Honorary Member of the International Glaciological Society, and Garry Clarke, uniquely holding all three awards of Honorary Membership, Richardson Medal and Seligman Crystal, was already a successful one at the time Stan invited Garry to help solve the problem of Devon Island borehole temperatures. Kurt Cuffey, who applied the Paterson-Clarke techniques successfully, has carried on the massive work launched by Stan with the Reference Cuffey and PatersonCuffey and Paterson (2010) fourth edition of The physics of glaciers.)

Various other techniques for inversion of borehole temperature profiles to determine past surface-temperature history avoid reliance on the isotopic ratios. These include control methods (Reference MacAyeal, Firestone and WaddingtonMacAyeal and others, 1991) and Monte Carlo techniques (Reference Dahl-JensenDahl-Jensen and others, 1998). Agreement among the different techniques increases confidence in the results.

Since borehole thermometry relies on well-understood physical processes with minimal use of assumed constancy of calibrations, the climatic reconstructions are especially reliable. Joint interpretation of borehole temperatures and isotopic ratios demonstrates that the higher-frequency isotopic oscillations contain temperature information, but suggests that the calibration of the isotopic thermometer may vary with time or with the frequency of the climate changes.

Testing this frequency dependence or time dependence of the isotopic temperature calibration became possible with a different set of tools based on gas isotopic fractionation in firn. Again, the reconstructions rely much more on constancy of physical law than on extrapolation of modern calibrations. A useful starting point for the history of this breakthrough is the discovery of gravitational fractionation of gases in firn by Michael Bender, Todd Sowers and Jakob Schwander (Reference Craig, Horibe and SowersCraig and others, 1988;Reference Schwander, Oeschger and LangwaySchwander, 1989; Reference Sowers, Bender and RaynaudSowers and others, 1989). This experimental demonstration of the strictly limited extent of wind mixing of firn gases opens a wealth of additional actualistic paleoclimatic techniques, some of which are described below.

The other key step was the discovery by Jeff Severinghaus of thermal diffusion in firn. A rapid temperature change at the surface causes a temperature gradient down the firn column, producing very slight separation of gases with the heavy species moving to the cold end within a few years (Reference Severinghaus, Sowers, Brook, Alley and BenderSeveringhaus and others, 1998). The effects of thermal diffusion and gravitation can be evaluated separately if multiple species (such as nitrogen and argon isotopes) are used, because gravitational separation depends solely on mass difference but thermal fractionation is not rigidly mass- dependent and varies with the element involved. The atmospheric residence times of argon and nitrogen are so long that atmospheric composition can be considered constant over the duration of the ice-core record. Thus, very slight compositional differences between the air trapped in bubbles and the free atmosphere reveal the temperature difference across the thickness of the firn.

Since the time for the physical temperature of ice at the bubble-trapping depth to equilibrate with a new surface temperature in central regions of ice sheets is many times longer than the time for diffusive equilibration of the gases in the firn, anomalous gas is trapped for many decades after a surface-temperature change, with the size of the anomaly revealing the temperature difference across the firn (which equals the size of the abrupt change, if the change was sufficiently fast). The position of the gas isotopic anomaly in an ice core reveals where the bubbles were being trapped when the surface-temperature change occurred.

Direct use of the gas isotopic anomalies to learn the temperature difference across the firn required precise laboratory calibration of the behavior of argon and nitrogen isotopes in a temperature gradient, and was achieved by Reference Severinghaus and BrookSeveringhaus and Brook (1999) and Reference Grachev and SeveringhausGrachev and Severinghaus (2003a, Reference Grachev and Severinghausb). In Reference Severinghaus, Sowers, Brook, Alley and BenderSeveringhaus and others (1998), the absolute temperature during the Younger Dryas in central Greenland was estimated from the number of years between the gas-phase and ice-phase indicators of the abrupt climate change that ended the Younger Dryas. Together with the accumulation rate (determined from the annual-layer thickness and an ice-flow model;Reference AlleyAlley and others, 1993;Reference Cuffey and ClowCuffey and Clow, 1997) and an empirically calibrated physical firn- densification model dependent on temperature and accumulation rate (Reference Herron and LangwayHerron and Langway, 1980), this age offset then provided an estimate of the absolute temperature averaged over the time that the firn was being buried to the bubble-trapping depth.

Note also that gravitational fractionation of firn air, which increases with the thickness of the firn in diffusive equilibrium, means that the thickness of the firn can be determined subject to a small uncertainty related to lack of detailed knowledge of the depth of the near-surface ‘convective zone’ associated with wind mixing. The thickness of the firn can be used, together with the accumulation rate and a firn densification model, to learn the absolute temperature averaged over the time during which the firn changed to ice. Advances in the ability to measure the isotopic composition of Ar and N₂ in ice cores have allowed identification of even relatively small surface-temperature changes (both warming and cooling) and their relation to changes in other gas species (CO₂ and CH₄) (Reference Caillon, Jouzel, Severinghaus, Chappellaz and BlunierCaillon and others, 2003a,b; Reference Grachev, Brook and SeveringhausGrachev and others, 2007).

Yet another physically based indicator towards the actualistic end of the spectrum is provided by the number density of bubbles. Firn appears to be geometrically self-similar or nearly so (Reference GowGow, 1968), such that an increase in crystal size at the bubble-trapping depth will produce fewer bigger bubbles without changing the total amount of trapped air. Crystal size at the bubble-trapping depth increases with the crystal growth rate and thus with temperature, and increases with the amount of time required to be buried to the bubble-trapping depth, which increases with decreasing temperature and decreasing accumulation rate. Bubble number density is preserved quantitatively for considerable times in ice, so bubble counts can be used with accumulation-rate estimates and a firn densification model to calculate temperature over the firnification time (Reference Spencer, Alley and FitzpatrickSpencer and others, 2006).

Enough physically based thermometers are available that it should be possible to determine both accumulation rate and temperature from application of the full suite. However, for the more recent parts of the ice-core history (especially since the Last Glacial Maximum, but extending somewhat before), accumulation rate can be estimated accurately from the ice-core dating (see below) corrected for the effects of ice flow (e.g. Reference NyeNye, 1963;Reference Dansgaard and JohnsenDansgaard and Johnsen, 1969; Reference AlleyAlley and others, 1993;Reference Cuffey and ClowCuffey and Clow, 1997) using knowledge from total gas content that the ice-sheet size has not changed hugely (Reference Raynaud, Chappellaz, Ritz and MartinerieRaynaud and others, 1997). The physically based indicators then yield the history of temperature. With increasing age, the uncertainty linked to ice-flow and accumulation-rate issues increases.

For the necessary age estimates, radiometric dating of ice is possible and may prove more valuable in the future. However, most dating now relies primarily on either annual- layer counting or correlation to accurately dated records from elsewhere.

Sorge recognized annual layers in his deep pit. Annual- layer counting has long been a mainstay of ice-core dating (Figs 3 and 4). Increasingly sensitive reproducible multiparameter ways of identifying annual layers have been developed (e.g. Reference McConnell, Lamorey, Lambert and TaylorMcConnell and others, 2002; Reference SvenssonSvensson and others, 2005;Reference RasmussenRasmussen and others, 2006). For situations in which multiple measurements across suites of cores are possible, zero-error dating is achievable, just as for tree rings. However, this is expensive and very time-consuming for deep cores. Counting annual layers with errors of ˜1% or less is straightforward, but achieving and demonstrating zero-error counts over tens of millennia is much harder (Reference MeeseMeese and others, 1997).

Fig. 3. Hoar frost with cross-country ski tracks, GISP2, central Greenland. Photograph by R. Alley.

Fig. 4. Buried hoar frost (light layers), snow pit, GISP2. The photograph is about 10 cm high. Winter snow lacks the strong contrast shown here (e.g. Reference Alley, Saltzman, Cuffey and FitzpatrickAlley and others, 1990). Such differences have been used in annual-layer counting back to Sorge. Photograph by R. Alley.

Increasingly, the ability to measure ages of paleoclimatic events in other archives (e.g. see Reference CaiCai and others, 2006) and to correlate those events to the ice cores and between ice cores (e.g. see Reference Blunier and BrookBlunier and Brook, 2001) means that certain points in ice cores can be dated with errors smaller than the ˜1% error from counting of ice-core layers. 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. This is because the ice cores show that many abrupt climate changes have been very tightly synchronous across broad regions in both high and low latitudes. Synchronous changes in indicators such as methane, δ¹⁸O of O₂, N₂O and others were recorded in the ice cores but were controlled by events far from the ice sheets, demonstrating the common age of the events with much less uncertainty than would be possible by comparing independently dated records from various places.

In turn, this suggests that annual-layer counts in ice cores will be used increasingly to interpolate between the fixed points derived from those best ages for abrupt climate changes. The absolute layer counts in the ice cores will continue to provide a check on ages from elsewhere.

However, if ice-core annual-layer counts are used to interpolate between the fixed points dated by correlation, it becomes useful to be able to re-count quickly and accurately if the ages of the fixed points are adjusted by even better analyses. Such re-counting requires an adaptive scheme to identify optimally the correct number of years between the fixed points from the available data. To this end, development of ‘auto-pickers’ using digital data may offer the best way forward (see Reference TaylorTaylor and others, 2004), implementing a computerized technique (or suite of techniques) with tuneable parameters that can be optimized to give an objective counting match to independent time markers.

Taken together, for cores from regions with little melting, ice-core science provides ages through layer counting or correlations as accurately as for any other archive, and much more accurately than for most. Furthermore, the history of snow accumulation rate and temperature can be determined with little uncertainty, relying primarily on physics rather than correlations, with multiple redundancy and small quantifiable uncertainties. This provides what I believe are the most reliable paleoclimatic records on Earth extending back at least a few tens of thousands of years. This success is based heavily on fundamental glaciological science, including studies of temperature in ice sheets, flow deformation and firn densification.

A Few Results on Trapped Gases

Many other aspects of ice-core science are especially well supported by fundamental science demonstrating the high reliability of the results. In this short historical review, I cannot begin to do justice to the many contributions in the Journal of Glaciology and elsewhere. In my experience, non-glaciologists are most interested in the ice-core records of atmospheric composition, so I will provide a short discussion of the remarkably high reliability of these records based on physics. Please note that I am not trying to provide the most up-to-date references, but a historical perspective instead, to show how long we have known many of these things. With modern citation analysis, an interested reader can find out which more-recent papers have made use of these classic contributions, and thus work up to the present.

Some aspects of the history of atmospheric composition are very difficult to reconstruct in any way except by ice- core measurements, such as the preindustrial history of methyl bromide (Reference Saltzman, Aydin, De Bruyn, King and Yvon-Lewis.Saltzman and others, 2004). Other aspects, such as the CO₂ concentration, can be estimated in many ways (e.g. see Reference JansenJansen and others, 2007, section 6.3.1 and references therein). However, these tend to involve uni- formitarian hypotheses to a considerable degree. Broad agreement among the various techniques is encouraging (Reference JansenJansen and others, 2007, Figure 6.1), but the uncertainties are notably larger than for ice-core records.

For ice cores, the approach is very actualistic. Samples of old air are archived in ice. Recovering and analyzing that air reveals the atmospheric composition in the past. Rather remarkably, this simple statement is a fairly accurate representation of the science, as discussed next.

At least part of the ice-core story of trace gases goes back to work by the late Norwegian Per Scholander on biological adaptation to cold conditions, conducted at the Office of Naval Research’s Arctic Research Laboratory at Point Barrow, Alaska, shortly after World War II (see Reference ShelesnyakShelesnyak, 1948a, Reference Shelesnyakb and the recent report by Reference ElsnerElsner, 2005). Scholander’s interest in the wintertime survival of organisms encased in ice led him to experiment on the diffusion of gases through ice, showing very slow rates and very low solubility (Reference Scholander, Flagg, Hock and Irving.Scholander and others, 1953, section VI). (Many modern students would benefit from reading this paper to see how science is done, how much progress is possible, and the breadth and depth of knowledge required to make that progress.)

A follow-up study by Scholander involved analyzing ice retrieved from icebergs, presumably of Greenlandic origin, along the Labrador coast. As reported in Science: ‘The rate of gas diffusion through ice is not more than 1/40 000 to 1/70 000 as fast as it is through water (citation to Reference Scholander, Flagg, Hock and Irving.Scholander and others, 1953). Considering this extremely slow rate, the relatively enormous diffusion distances in the glacier, and the large quantity of gases held under pressure in the ice, it would seem possible that gas trapped in the glacier would remain unchanged for millennia. Analysis of such gas could therefore give information about the atmospheric composition at the time the ice was formed.’ (Reference Scholander, Kanwisher and NuttScholander and others, 1956, p. 104)

Scholander and co-workers found that the bubbles contained pressurized air. Slight depletion of oxygen was reported, with the suggestion that this might reflect glacial/ interglacial changes, although a subsequent study (Reference Coachman, Hemmingsen, Scholander, Enns and de VriesCoachman and others, 1958b) pointed to oxygen loss from bubbles through solution in small amounts of meltwater produced along the bubble surfaces. Scholander’s research group also studied air and ¹⁴C age of ice from near Thule, Greenland (Reference Coachman, Hemmingsen, Scholander, Enns and de VriesCoachman and others, 1958a). Not surprisingly, Scholander published in the Journal of Glaciology, presenting results on the pressure and composition of bubbles in Greenland icebergs (Reference Scholander and NuttScholander and Nutt, 1960;Reference Scholander, Hemmingsen, Coachman and NuttScholander and others, 1961). He then collaborated with the great Willi Dansgaard, using S¹⁸O as well as ¹⁴C to study ice from Greenland (Reference Scholander, Dansgaard, Nutt, de Vries, Coachman and HemmingsenScholander and others, 1962;see also Reference Schmidt-NielsenSchmidt-Nielsen, 1987).

The point of reviewing the contributions of Per Scholander is not simply to remember a great scientist, but to note that the analysis of ice-core gases started with fundamental physics: the low diffusion rate and solubility of gases in ice meant that the bubbles would preserve accurate records. Only after a range of background research did useful reconstructions of past atmospheres emerge.

The glaciological community greatly extended and improved the pioneering work of Scholander. A good review of some of the efforts expended to ensure reliability of the record is given by Reference Raynaud, Jouzel, Barnola, Chappellaz, Delmas and LoriusRaynaud and others (1993) (see also Reference Raynaud, Barnola, Chappellaz, Blunier, Indermuhle and StaufferRaynaud and others, 2000), and I provide additional insights next.

The simplest, most compelling evidence demonstrating that Scholander accurately foresaw the utility of ice as a bottle for old air is provided empirically. For the key atmospheric trace gases, such as CO₂, CH₄ and N₂O, and for tens of thousands to hundreds of thousands of years we now have multiple records generated by different laboratories on different continents using cores from sites with different accumulation rates, temperatures and impurity loadings, often stored, handled and analyzed in different ways, yet yielding the same history within the combined analytical and dating uncertainties (e.g. see Reference JansenJansen and others 2007, especially Figure 6.4; Reference Ahn and BrookAhn and Brook, 2008). Furthermore, this record overlaps with the instrumental measurements of the free atmosphere, again with beautiful agreement (Reference Neftel, Moor, Oeschger and Stauffer.Neftel and others, 1985;Reference Pearman, Etheridge, de Silva and FraserPearman and others, 1986). There is no plausible way that this agreement could be produced if there are significant problems with the entrapment, storage, recovery or reading of the atmospheric signal in the ice.

Furthermore, because bubbles are trapped at depth but snow is deposited at the surface, a climate change that affects the composition of the ice and of the air is recorded in different places along an ice core, with the offset depending on temperature and accumulation rate. The major changes in gas composition and ice composition are not in the same places in the key climate records from ice cores (e.g. Reference MonninMonnin and others, 2001);within the ice from which the main records are generated, the chemistry changes without affecting the gases, and the gases change without affecting the chemistry.

I could probably stop here, but it is instructive to look more deeply at the great number of underlying tests and the great range of supporting evidence, providing even stronger support for the high reliability of the ice-core record of atmospheric composition. This includes learning not only how to get the best record, but testing the limits of that record by finding out the conditions under which artifacts do occur, so that such conditions can be avoided. A few comments on these additional tests follow.

First, remarkable care goes into generating the records and ensuring their integrity.

The ice-core gas laboratories I have visited are impressive undertakings, with fanatical dedication to avoiding problems from contamination or leaks, and extensive use of laboratory standards and blind laboratory intercomparisons (e.g. Reference SowersSowers and others, 1997).

Some analyses of old ice include searching for human- made chlorofluorocarbons, which are ubiquitous in the environment today but absent from the preindustrial environment – any contamination must introduce these modern ‘tracers’, and absence of them shows that contamination has not been introduced (e.g. Reference Etheridge, Pearman and SilvaEtheridge and others, 1988;see also Reference AydinAydin and others, 2010). Care is taken to monitor transport and storage conditions, and to quantify any post-recovery changes affecting the ice and contained gases (e.g. Reference Bereiter, Schwander, Stocker and LuthiBereiter and others, 2009).

The agreement between atmospheric measurements and concentrations in recently formed bubbles is very good (Reference Etheridge, Steele, Langenfelds, Francey, Barnola and MorganEtheridge and others, 1996;Reference MacFarlingMacFarling and others, 2006). In addition, extensive sampling has been conducted in the firn, extracting air from specific layers, to track the complete transition from free atmosphere to ice-core bubbles in exquisite detail (e.g. Reference SchwanderSchwander and others, 1993;Reference Bender, Sowers, J.M. and ChappellazBender and others, 1994).

Trapping of bubbles is not an instantaneous process, so any sample includes air with a range of ages. The width of that range – typically decades to centuries – has been studied carefully (Reference Schwander and StaufferSchwander and Stauffer, 1984). Short-lived events will be more evident in records from cores with a shorter trapping time, and indeed this is observed in specific cases (Reference Spahni, Schwander, Fluckiger, Stauffer, Chappellaz and RaynaudSpahni and others, 2003). If there were important short-lived climate events that had not been resolved by the ice cores, then markedly increasing variability with increasing time resolution would be evident at many points in the records. Interesting subtle effects may exist for some gases, but the good agreement among records shows that there are no major problems.

Rapid diffusion of gases in the ice would reduce the time resolution of records and give a false impression of smoothness, but this can be excluded with high confidence. The early work of Scholander, described above, shows that the science of ice-core gases started with the determination that diffusion is slow, and subsequent work supports this. A fascinating demonstration comes from clever use of a different potential problem: melt layers.

When melting occurs at the ice-sheet surface, the water typically refreezes into a bubble-poor layer that has an elevated concentration of CO₂ due to its high solubility in water (Reference Stauffer, Neftel, Oeschger, Schwander, Langway, Oeschger and DansgaardStauffer and others, 1985). Refrozen meltwater is readily apparent by inspection of bubbly ice, and indeed its occurrence can be used as a paleoclimatic indicator. Cores with extensive melting are avoided for studies of past atmospheric composition, and even small amounts of meltwater are problematic for highly soluble gases such as CO₂.

However, the high CO₂ concentration in the melt layers provides a tracer for diffusion. For sites with little melting, such as Siple Dome, Antarctica, the occurrence of meltwater is restricted to regions in or nearthe melt layer that ultimately forms (Reference Das and AlleyDas and Alley, 2005), and can be recognized by excess heavy noble gases as well as CO₂. Measuring the modern width of the resulting CO₂ anomaly compared with the original width from the visible melt layer provides an estimate of the diffusion. This rate is such that diffusion in very old, warm ice will have smoothed thin features, but the main results that have been presented to the public have not been significantly affected (Reference Ahn and BrookAhn and others, 2008).

At sufficiently great depth and pressure, the bubbles in ice cores disappear as solid air clathrates develop. The transformation is not instantaneous, and some gases preferentially fractionate into the solid phase or the gas phase in the zone where solid and gas coexist as dictated by the phase diagram for the particular gas (Reference IkedaIkeda and others, 1999). If an analytical technique is used that does not recover all of the gas in the solid phase in this region of coexisting clathrate and bubbles, then gases that preferentially enter the solid phase will appear anomalously depleted, while gases that preferentially remain in the gas phase will appear anomalously enriched. Indeed, such behavior is observed for N₂O, with reduced concentration measured using a dry extraction technique in the clathrate- formation zone in comparison to a different core with the same-age ice completely above the zone of clathrate formation; however, comparisons outside this zone of clathrate formation do not find anomalies (Reference Sowers, Alley and JubenvilleSowers and others, 2003;see also Reference LüthiLüthi and others, 2010).

Warming and increasing impurity levels both tend to favor biological activity or chemical reactions that could obscure the environmental record in ice cores. As noted above, the onset of melting is especially problematic, and any trace-gas record from ice with evidence of melting is viewed with extreme caution. Ice that is especially impure and warm, up to and including ice containing dead bugs, is found to contain highly anomalous gas concentrations reflective of processes in the ice (e.g. Reference Souchez, Lemmens and Chappellaz.Souchez and others, 1995;Reference Campen, Sowers and AlleyCampen and others, 2003). Furthermore, small CO₂ anomalies are observed in ice containing especially high levels of both carbonate dust and sulfuric acid, and likely resulting from CO₂-liberating reactions between these in the ice (Reference Stauffer, Hofer, Oeschger, Schwander and SiegenthalerStauffer and others, 1984;Reference DelmasDelmas, 1993). However, as noted above, the trace-gas histories of atmospheric composition are independent of chemistry and temperature of ice for all colder, cleaner sites.

Taking all of these investigations together, fundamental scientific understanding indicates that trace-gas records from cold, clean sites on Greenland and especially Antarctica should provide accurate records of atmospheric composition with very little uncertainty. The published literature documents the great care taken by the relevant laboratories to achieve this goal, and the results show that different laboratories using different ice cores with different temperatures, accumulation rates and impurity loadings produce the same atmospheric histories, which agree with instrumental data. Combining these trace-gas results with the multiply duplicated determinations of age, temperature and accumulation rate allows especially reliable reconstructions of climate history, and hypothesis-testing regarding cause and effect in climate change.

More work remains to be done, and as increasingly precise measurements on increasingly small samples are developed, some of the issues discussed above may become more important. However, the main results of ice-core science have not been overturned despite being tested in many ways by many groups over many years and decades, and the main results are based strongly on physical understanding of relatively simple systems. Thus, these results are especially robust.

Knowledge of history, including the history of papers published in the Journal of Glaciology, shows that ice-core science is indeed reliable. The value of disciplinary journals such as the Journal of Glaciology is shown very clearly.