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A Fresh Perspective on the Cordilleran Ice Sheet Ingrid Hendy Department of Geological Sciences, University of Michigan, Ann Arbor, Michigan 48109, USA

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A Fresh Perspective on the Cordilleran Ice Sheet Ingrid Hendy Department of Geological Sciences, University of Michigan, Ann Arbor, Michigan 48109, USA A fresh perspective on the Cordilleran Ice Sheet Ingrid Hendy Department of Geological Sciences, University of Michigan, Ann Arbor, Michigan 48109, USA The fate of Earth’s cryosphere in the coming SMOW; Flower et al., 2004). These depleted decades to centuries is a current topic of great values can be attributed to ice forming in a debate within the climate science community high-latitude, continental climate with a distal and wider public arena. The advance and retreat moisture source. Conversely, southern CIS ice of past ice sheets can shed new light on our formed from snow falling at signifi cantly lower understanding of the cyrosphere. The response latitudes close to a maritime moisture source of a temperate ice mass, like the Cordilleran (Clague, 1981). The δ18O of modern glacial Ice Sheet (CIS), to climate forcing contributes ice in coastal southern Alaska is −17.8‰ at the important clues to what scenario best fi ts the Columbia Glacier and −22.6‰ (SMOW) at future. One such scenario involves the potential the Harvard Glacier (Kipphut, 1990). Finally, role of melting ice sheets (namely the Greenland the environmental preferences of planktonic Ice Sheet) injecting freshwater into the Atlan- foraminifera make it unlikely that they would tic Ocean, leading to deep-water shutoff and a have inhabited a meltwater plume, unlike other frigid eastern North America and Europe. This marine plankton such as diatoms (Lopes and Figure 1. Map of northwestern American mar- scenario occurred repeatedly during the last gla- Mix, 2009; p. 79 in this issue) or dinofl agellates gin showing location of the southern lobes of the Cordilleran Ice Sheet at 17 ka, Lake cial interval. Evidence has been easy to fi nd for that are tolerant of low-salinity conditions. Missoula (light shading), the Scablands (dark these freshwater events in the Atlantic, in the The new study by Lopes and Mix (2009) pub- shading; Waitt, 1985), and locations of the form of ice-rafted debris (IRD) layers and anom- lished in this issue of Geology fi nds evidence for deep sea cores. The maximum extent of alous negative δ18O values found in planktonic the elusive low-salinity melt water discharge from the Cordilleran Ice Sheet at 25 ka (heavy dashed white line) and at 17 ka (3-dimensional foraminifera (Hemming, 2004). Similar fresh- the eastern lobes of the CIS (Fig. 1). Freshwater white shading) is indicated (Clague and water events in the Pacifi c Ocean have proven diatoms transported by meltwater discharge are James, 2002). ODP—Ocean Drilling Program. more elusive and have been largely overlooked, found in southern Oregon sediments starting at although the existence of glacial outburst fl ood- ca. 33 ka, ~2.5 k.y. before glacimarine sedimen- ing into the Pacifi c has been known for some time tation began on the continental slope of Van- Island (Herzer and Bornhold, 1982). The CIS (Atwater , 1984; Bretz et al., 1956; Shaw et al., couver Island (Cosma and Hendy, 2008). These reached its maximum extent by 17.5 ka in 1999). Consequently the effects of the impressive results are important, fi rst because they suggest Washington (Porter and Swanson, 1998). At this Lake Missoula fl oods events on the northeastern that the continental side of the CIS advanced time, the CIS extended westward to the edge of Pacifi c Ocean remain poorly understood. earlier than the marine border (with a caveat, the continental shelf in the Juan de Fuca Lobe, Harlen Bretz (Bretz et al., 1956) identifi ed however, that dating errors may allow for a syn- and south in several large lobes, including the evidence of catastrophic fl oods in the 1920s, chronous advance). Second, outburst fl ooding Puget, Okanogan, Columbia River, Purcell based on morphological features in the Chan- maybe a long-standing feature of the CIS, with Trench, and Flathead lobes (Fig. 1; Porter and neled Scablands, the Columbia Gorge, and dammed glacial lakes similar to Lake Missoula Swanson, 1998; Waitt, 1985). In contrast to the the Willamette Valley (Fig. 1). These features appearing far earlier than previously believed. well-constrained chronology of the western CIS, included gigantic water-carved channels, enor- Our present understanding of the CIS sug- Fraser Glaciation timing east of the Cascades mous dry cataracts, overtopped drainage divides, gests that glaciers of the Coast, Selkirk, and and Coast Mountains is poorly constrained, with and huge gravel bars (Bretz et al., 1956). Bretz, Olympia mountains advanced during the Fraser an advance to within 100 km of the ice limit at however, could not explain the source of such a Glaciation at ca. 30 ka, and by ca. 25 ka had 17.2 ka (Booth et al., 2004). large volume of water, and what followed was coalesced to form the incipient CIS (Hicock On the Eastern CIS, pro-glacial Lake Mis- an acrimonious 40 yr debate over the origin of and Armstrong, 1981). This initial expansion of soula formed at the leading edge of the CIS when the Scablands. We now know that the fl oods glaciers was accompanied by an increase in gla- the Purcell Trench Lobe blocked drainage to the were produced by melting the eastern lobes of cial erosion and the deposition of large outwash northeastern Pacifi c (Porter and Swanson, 1998). the CIS—the much smaller, little-known west- sheets such as Quadra Sand (Clague, 1976). Between 18.6 and 15.9 ka, repeated failure of ern neighbor of the Laurentide Ice Sheet. The The glacial sequences in northern Washington the ice dam (~89 times; Atwater, 1984) resulted CIS initially grew in the north (Alaska) but and southern British Columbia were probably in 2500 yr of freshwater input to the northeast- spread south during the last (Fraser) glaciation, deposited under climatic conditions similar to ern Pacifi c Ocean. The timing (19–17 ka) of reaching its maximum extent (~4000 km wide) temperate glaciers in the present-day Gulf of these ice dam failures closely corresponds to in southern British Columbia and northern Alaska, as glacimarine sediment records sug- signifi cant low-salinity anomalies inferred by Washington (Fig. 1; Booth et al., 2004). gest a signifi cant meltwater discharge with a Lopes and Mix (2009). Outburst fl oods contain- Evidence for these outburst fl oods has been high suspended load (Domack, 1983). ing fresh water and entrained sediment reached hard to fi nd in the Pacifi c Ocean. First, a CIS The CIS advanced into the Pudget Lowland the northeastern Pacifi c via the Columbia River meltwater signal could be diffi cult to detect and Juan de Fuca Strait shortly after 21 ka (Atwater, 1984), with the largest fl ood volume relative to the Laurentide Ice Sheet. Estimated (Porter and Swanson, 1998), while to the west estimated at ~2,500 km3 (Ostlund et al., 1987). δ18 Lauren tide Ice Sheet Oice was probably it coalesced with a large independent glacier Later fl oods were probably smaller in volume ~−25 to −35‰ (Standard Mean Ocean Water, in Barclay Sound after overtopping Van couver and more frequent. Large sediment loads from © 2009 The Geological Society of America. For permission to copy, contact Copyright Permissions, GSA, or [email protected]. GEOLOGY,Geology, January January 2009; 2009 v. 37; no. 1; p. 95–96; doi: 10.1130/focus012009.1. 95 Downloaded from http://pubs.geoscienceworld.org/gsa/geology/article-pdf/37/1/95/3536880/i0091-7613-37-1-95.pdf by guest on 24 September 2021 these fl oods were deposited over the southern REFERENCES CITED Atlantic and their global climate imprint: Cascadia Basin, and the adjacent abyssal plain Atwater, B.F., 1984, Periodic floods from Gla- Reviews of Geophysics, v. 42, RG1005, doi: cial Lake Missoula into the Sanpoil arm 10.1029/2003RG000128. off the western North American margin (Brunner of Gla cial Lake Columbia: Geology, v. 12, Hendy, I.L., and Cosma, T., 2008, Vulnerability of et al., 1999; Normark and Reid, 2003). p. 464–467, doi: 10.1130/0091–7613(1984)12 the Cordilleran Ice Sheet to iceberg calving The timing of outburst fl ooding may have <464:PFFGLM>2.0.CO;2. during late Quaternary rapid climate change been different further north on the marine Blais-Stevens, A., Clague, J.J., Mathewes, R.W., events: Paleoceanography, v. 23, PA2101, doi: boundary of the CIS, where fl oods appear to Hebda, R.J., and Bornhold, B.D., 2003, Record 10.1029/2008PA001606. of large, Late Pleistocene outburst fl oods pre- Herzer, R.H., and Bornhold, B.D., 1982, Glaciation be only associated with a fully developed ice served in Saanich Inlet sediments, Vancouver and post-glacial history of the continental shelf sheet (Cosma et al., 2008). At ca. 19.5 ka, Island, Canada: Quaternary Science Reviews, off southwestern Vancouver Island, British cyclic (~80 yr return interval) outburst fl ood- v. 22, p. 2327–2334, doi: 10.1016/S0277– Columbia: Marine Geology, v. 48, p. 285–319, ing abruptly began at core MD02–2496 3791(03)00212–9. doi: 10.1016/0025–3227(82)90101–3. Booth, D.B., Troost, K.G., Clague, J.J., and Waitt, Hicock, S.R., and Armstrong, J.E., 1981, Coquitlam (Cosma and Hendy, 2008). Repeated cycles of R.B., 2004, The Cordilleran Ice Sheet: Chapter Drift—A pre-Vashon Fraser Glacial forma- sediment input are recorded in the ~2-cm-thick 2, in Gillespie, A.R., Porter, S.C., and Atwater, tion in the Fraser Lowland, British Columbia: sediment layers on the continental slope off B.F., eds., The Quaternary Period in the United Canadian Journal of Earth Sciences, v. 18, Vancouver Island. After 17 ka, outburst fl oods States: International Union for Quaternary p. 1443–1451.
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