Glaciers in North America
From Climate Change Reconsidered, a work of the Nongovernmental International Panel on Climate Change
Model studies indicate that CO2-induced global warming will result in significant melting of earth’s glaciers, contributing to a rise in global sea level. Global data on glaciers do not support claims made by the IPCC that most glaciers are retreating or melting.
North American Glaciers
The history of North American glacial activity also fails to support the claim that anthropogenic CO2 emissions are causing glaciers to melt. Dowdeswell et al. (1997) analyzed the mass balance histories of the 18 Arctic glaciers with the longest observational records, finding that just over 80 percent of them displayed negative mass balances over the last half of the twentieth century. However, they note that “ice-core records from the Canadian High Arctic islands indicate that the generally negative glacier mass balances observed over the past 50 years have probably been typical of Arctic glaciers since the end of the Little Ice Age.” They say “there is no compelling indication of increasingly negative balance conditions which might, a priori, be expected from anthropogenically induced global warming.”
Clague et al. (2004) documented glacier and vegetation changes at high elevations in the upper Bowser River basin in the northern Coast Mountains of British Columbia, based on studies of the distributions of glacial moraines and trimlines, tree-ring data, cores from two small lakes that were sampled for a variety of analyses (magnetic susceptibility, pollen, diatoms, chironomids, carbon and nitrogen content, 210Pb, 137Cs, 14C), similar analyses of materials obtained from pits and cores from a nearby fen, and by accelerator mass spectrometry radiocarbon dating of plant fossils, including wood fragments, tree bark, twigs and conifer needles and cones. All this evidence suggested a glacial advance that began about 3,000 years ago and may have lasted for hundreds of years, which would have placed it within the unnamed cold period that preceded the Roman Warm Period. There was also evidence for a second minor phase of activity that began about 1,300 years ago but was of short duration, which would have placed it within the Dark Ages Cold Period. Finally, the third and most extensive Neoglacial interval began shortly after AD 1200, following the Medieval Warm Period, and ended in the late 1800s, which was, of course, the Little Ice Age, during which time Clague et al. say “glaciers achieved their greatest extent of the past 3,000 years and probably the last 10,000 years.”
These data clearly depict the regular alternation between non-CO2-forcecd multi-century cold and warm periods that is the trademark of the millennial-scale oscillation of climate that reverberates throughout glacial and interglacial periods alike. That a significant, but by no means unprecedented, warming followed the most recent cold phase of this cycle is in no way unusual, particularly since the Little Ice Age was likely the coldest period of the last 10,000 years.
Alaska, Calkin et al. (2001) reviewed the most current and comprehensive research of Holocene glaciation along the northernmost portion of the Gulf of Alaska between the Kenai Peninsula and Yakutat Bay, where several periods of glacial advance and retreat were noted during the past 7,000 years. Over the latter part of this record, there was a general glacial retreat during the Medieval Warm Period that lasted for a few centuries prior to A.D. 1200, after which there were three major intervals of Little Ice Age glacial advance: the early fifteenth century, the middle seventeenth century, and the last half of the nineteenth century. During these latter time periods, glacier equilibrium line altitudes were depressed from 150 to 200 m below present values as Alaskan glaciers also “reached their Holocene maximum extensions.”
Wiles et al. (2004) derived a composite Glacier Expansion Index (GEI) for Alaska based on “dendrochronologically derived calendar dates from forests overrun by advancing ice and age estimates of moraines using tree-rings and lichens” for three climatically distinct regions—the Arctic Brooks Range, the southern transitional interior straddled by the Wrangell and St. Elias mountain ranges, and the Kenai, Chugach, and St. Elias coastal ranges—after which they compared this history of glacial activity with “the 14C record preserved in tree rings corrected for marine and terrestrial reservoir effects as a proxy for solar variability” and with the history of the Pacific Decadal Oscillation (PDO) derived by Cook (2002).
As a result of their efforts, Wiles et al. discovered that “Alaska shows ice expansions approximately every 200 years, compatible with a solar mode of variability,” specifically, the de Vries 208-year solar cycle; and by merging this cycle with the cyclical behavior of the PDO, they obtained a dual-parameter forcing function that was even better correlated with the Alaskan composite GEI, with major glacial advances clearly associated with the Sporer, Maunder, and Dalton solar minima.
Wiles et al. said “increased understanding of solar variability and its climatic impacts is critical for separating anthropogenic from natural forcing and for predicting anticipated temperature change for future centuries.” They made no mention of possible CO2-induced global warming in discussing their results, presumably because there was no need to do so. Alaskan glacial activity, which in their words “has been shown to be primarily a record of summer temperature change (Barclay et al., 1999),” appears to be sufficiently well described within the context of centennial (solar) and decadal (PDO) variability superimposed upon the millennial-scale (non-CO2-forced) variability that produces longer-lasting Medieval Warm Period and Little Ice Age conditions.
Pederson et al. (2004) used tree-ring reconstructions of North Pacific surface temperature anomalies and summer drought as proxies for winter glacial accumulation and summer ablation, respectively, to create a 300-year history of regional glacial Mass Balance Potential (MBP), which they compared with historic retreats and advances of Glacier Park’s extensively studied Jackson and Agassiz glaciers in northwest Montana..
As they describe it, “the maximum glacial advance of the Little Ice Age coincides with a sustained period of positive MBP that began in the mid-1770s and was interrupted by only one brief ablation phase (~1790s) prior to the 1830s,” after which they report “the mid-19th century retreat of the Jackson and Agassiz glaciers then coincides with a period marked by strong negative MBP.” From about 1850 onward, they note “Carrara and McGimsey (1981) indicate a modest retreat (~3-14 m/yr) for both glaciers until approximately 1917.” At that point, they report that “the MBP shifts to an extreme negative phase that persists for ~25 yr,” during which period the glaciers retreated “at rates of greater than 100 m/yr.”
Continuing with their history, Pederson et al. report that “from the mid-1940s through the 1970s retreat rates slowed substantially, and several modest advances were documented as the North Pacific transitioned to a cool phase [and] relatively mild summer conditions also prevailed.” From the late 1970s through the 1990s, they say, “instrumental records indicate a shift in the PDO back to warmer conditions resulting in continuous, moderate retreat of the Jackson and Agassiz glaciers.”
The first illuminating aspect of this glacial history is that the post-Little Ice Age retreat of the Jackson and Agassiz glaciers began just after 1830, in harmony with the findings of a number of other studies from various parts of the world (Vincent and Vallon, 1997; Vincent, 2001, 2002; Moore et al., 2002; Yoo and D’Odorico, 2002; Gonzalez-Rouco et al. 2003; Jomelli and Pech, 2004), including the entire Northern Hemisphere (Briffa and Osborn, 2002; Esper et al., 2002). These findings stand in stark contrast to what is suggested by the IPCC-endorsed “hockeystick” temperature history of Mann et al. (1998, 1999), which does not portray any Northern Hemispheric warming until around 1910.
The second illuminating aspect of the glacial record is that the vast bulk of the glacial retreat in Glacier National Park occurred between 1830 and 1942, over which time the air’s CO2 concentration rose by only 27 ppm, which is less than a third of the total CO2 increase experienced since the start of glacial recession. Then, from the mid-1940s through the 1970s, when the air’s CO2 concentration rose by another 27 ppm, Pederson et al. report that “retreat rates slowed substantially, and several modest advances were documented.”
The first 27 ppm increase in atmospheric CO2 concentration coincided with the great preponderance of glacial retreat experienced since the start of the warming that marked the “beginning of the end” of the Little Ice Age, but the next 27 ppm increase in the air’s CO2 concentration was accompanied by little if any additional glacial retreat, when, of course, there was little if any additional warming.
Something other than the historic rise in the air’s CO2 content was responsible for the disappearing ice fields of Glacier National Park. The historical behavior of North America’s glaciers provides no evidence for unprecedented or unnatural CO2-induced global warming over any part of the twentieth century.
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Calkin, P.E., Wiles, G.C. and Barclay, D.J. 2001. Holocene coastal glaciation of Alaska. Quaternary Science Reviews 20: 449-461.
Carrara, P.E. and McGimsey, R.G. 1981. The late neoglacial histories of the Agassiz and Jackson Glaciers, Glacier National Park, Montana. Arctic and Alpine Research 13: 183-196.
Clague, J.J., Wohlfarth, B., Ayotte, J., Eriksson, M., Hutchinson, I., Mathewes, R.W., Walker, I.R. and Walker, L. 2004. Late Holocene environmental change at treeline in the northern Coast Mountains, British Columbia, Canada. Quaternary Science Reviews 23: 2413-2431.
Climate Change Reconsidered: Website of the Nongovernmental International Panel on Climate Change. http://www.nipccreport.org/archive/archive.html
Cook, E.R. 2002. Reconstructions of Pacific decadal variability from long tree-ring records. EOS: Transactions, American Geophysical Union 83: S133.
Dowdeswell, J.A., Hagen, J.O., Bjornsson, H., Glazovsky, A.F., Harrison, W.D., Holmlund, P., Jania, J., Koerner, R.M., Lefauconnier, B., Ommanney, C.S.L. and Thomas, R.H. 1997. The mass balance of circum-Arctic glaciers and recent climate change. Quaternary Research 48: 1-14.
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Vincent, C. 2001. Fluctuations des bilans de masse des glaciers des Alpes francaises depuis le debut du 20em siecle au regard des variations climatiques. Colloque SHF variations climatiques et hydrologie. Paris, France, pp. 49-56.
Vincent, C. 2002. Influence of climate change over the 20th century on four French glacier mass balances. Journal of Geophysical Research 107: 4-12.
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