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Record of Recent River Channel Instability, Cheakamus Valley, British Columbia

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Record of Recent River Channel Instability, Cheakamus Valley, British Columbia Geomorphology 53 (2003) 317–332 www.elsevier.com/locate/geomorph Record of recent river channel instability, Cheakamus Valley, British Columbia John J. Claguea,b,*, Robert J.W. Turnerb,1, Alberto V. Reyesa,2 a Department of Earth Sciences, Simon Fraser University, Burnaby, British Columbia, Canada V5A 1S6 b Geological Survey of Canada, 101-605 Robson Street, Vancouver, British Columbia, Canada V6B 5J3 Received 14 May 2002; received in revised form 3 October 2002; accepted 4 October 2002 Abstract Rivers flowing from glacier-clad Quaternary volcanoes in southwestern British Columbia have high sediment loads and anabranching and braided planforms. Their floodplains aggrade in response to recurrent large landslides on the volcanoes and to advance of glaciers during periods of climate cooling. In this paper, we document channel instability and aggradation during the last 200 years in lower Cheakamus River valley. Cheakamus River derives much of its flow and nearly all of its sediment from the Mount Garibaldi massif, which includes a number of volcanic centres dominated by Mount Garibaldi volcano. Stratigraphic analysis and radiocarbon and dendrochronological dating of recent floodplain sediments at North Vancouver Outdoor School in Cheakamus Valley show that Cheakamus River aggraded its floodplain about 1–2 m and buried a valley-floor forest in the early or mid 1800s. The aggradation was probably caused by a large (ca. 15–25 Â 106 m3) landslide from the flank of Mount Garibaldi, 15 km north of our study site, in 1855 or 1856. Examination of historical aerial photographs dating back to 1947 indicates that channel instability triggered by this event persisted until the river was dyked in the late 1950s. Our observations are consistent with data from many other mountain areas that suggest rivers with large, but highly variable sediment loads may rapidly aggrade their floodplains following a large spike in sediment supply. Channel instability may persist for decades to centuries after the triggering event. Crown Copyright D 2002 Published by Elsevier Science B.V. All rights reserved. Keywords: Floodplain; Aggradation; Channel instability; Stratigraphy; Little Ice Age British Columbia; Canada 1. Introduction Rivers in British Columbia have responded in a complex manner to linked changes in sediment supply * Corresponding author. Department of Earth Sciences, Simon and climate on time scales ranging from years to Fraser University, Burnaby, British Columbia, Canada V5A 1S6. millennia (Church, 1981; Ryder and Church, 1986; Tel.: +1-604-291-4924; fax: +1-604-291-4198. Desloges and Church, 1987; Gottesfeld and Johnson- E-mail addresses: [email protected] (J.J. Clague), Gottesfeld, 1990; Jordan and Slaymaker, 1991; Ash- [email protected] (R.J.W. Turner), [email protected] (A.V. Reyes). more and Church, 2001). The principal responses have 1 Tel.: +1-604-666-4852; fax: +1-604 666-1124. been changes in river planform and aggradation and 2 Tel.: +1-604-291-3856; fax: +1-604-291-4198. degradation of channels and floodplains. The greatest 0169-555X/02/$ - see front matter. Crown Copyright D 2002 Published by Elsevier Science B.V. All rights reserved. doi:10.1016/S0169-555X(02)00321-5 318 J.J. Clague et al. / Geomorphology 53 (2003) 317–332 changes since the end of the Pleistocene occurred early Ryder, 1972), although conditioned by glaciation, are during postglacial time when rivers rapidly aggraded really delayed, indirect responses to climatic change. their valleys in response to the transfer of large amounts They are more directly linked to sediment availability of sediment to valley floors (Church and Ryder, 1972; than to climate at the time of aggradation or degrada- Clague, 1986). The fills produced by this short-lived tion. phase of aggradation were incised over periods of Lesser changes in river planform and base level centuries to perhaps thousands of years in the early that are more directly linked to climatic change have Holocene after the supply of easily eroded drift became been documented in some river basins in British exhausted. These ‘‘paraglacial’’ effects (Church and Columbia and elsewhere (e.g., Meyer et al., 1992; Fig. 1. Map of the Cheakamus and lower Squamish River watersheds. Black areas are Quaternary volcanic rocks. The west flank of the Mount Garibaldi massif is the principal source of sediment to Cheakamus River. J.J. Clague et al. / Geomorphology 53 (2003) 317–332 319 Huisink, 1999). Some rivers in the Coast Mountains volcanic eruptions (Lipman and Mullineaux, 1981) of British Columbia aggraded their floodplains and may increase sediment delivery to rivers, causing acquired braided planforms during the Little Ice Age them to aggrade their valleys (Jordan and Slay- (Desloges, 1987; Desloges and Church, 1987; Got- maker, 1991). The perturbing event may be tesfeld and Johnson-Gottesfeld, 1990). These rivers short-lived, but its effects can persist for decades incised their floodplains and developed more anab- or even centuries. The cataclysmic eruptions of ranching planforms during the twentieth century, as Mount St. Helens in May 1980 and Mount Pinatubo climate warmed. Other researchers have documented in 1991, for example, triggered debris flows that climatically driven cycles of aggradation and degra- aggraded valleys many tens of kilometres from the dation at longer time scales. Huisink (1999),for volcanoes. The rivers that drain these volcanoes are example, reconstructed the complex response of the still adjusting to the eruptions (Simon, 1999; Hayes Maas River to alternating warm and cool intervals et al., 2002). during the Pleistocene–Holocene transition. Meyer This paper documents and attempts to explain a et al. (1992) attributed periods of late Holocene period of channel instability and aggradation in the alluvial fan growth and floodplain aggradation in Cheakamus River valley in southwestern British Yellowstone National Park to climatically driven Columbia. We date the perturbation and ascribe it to forest fire cycles. a large landslide at the head of a tributary of Chea- Other, more local factors can alter the equili- kamus River, 15 km north of our study area, in the brium of rivers, triggering base level and morpho- middle 1800s. We suggest that the river was still logical changes. Notably, large landslides (Hewitt, adjusting to this perturbation as late as the 1950s 1998), human disturbance (Knighton, 1989),and when it was dyked. Fig. 2. Shaded-relief, digital elevation model showing localities mentioned in the paper. 320 J.J. Clague et al. / Geomorphology 53 (2003) 317–332 Fig. 3. Map of the study area showing the known extent of the buried forest, giant living red cedars, and large cut cedar and hemlock stumps. J.J. Clague et al. / Geomorphology 53 (2003) 317–332 321 2. Setting Garibaldi massif (Fig. 2). Mount Garibaldi is a Pleistocene volcano that last erupted 11,000– Cheakamus River drains 1070 km2 of the Coast 12,000 years ago during deglaciation of the region Mountains of southwestern British Columbia (Fig. 1). (Mathews, 1952a). The western slopes of the vol- It is a major tributary of Squamish River, which it cano are steep and prone to landsliding. Near the enters 9 km north of Squamish at the head of Howe head of Rubble Creek is a near-vertical cliff in Sound. Cheakamus River and its tributaries head in highly jointed basalt. The cliff, which is named The alpine basins, many of which presently contain gla- Barrier, formed about 12,000 years ago when a lava ciers. flow erupted from a cone on the flank of Mount Of particular importance for our study are three Garibaldi and terminated against glacier ice filling tributaries of Cheakamus River, Rubble Creek, Cull- Cheakamus and Rubble Creek valleys (Mathews, iton Creek, and Cheekye River, which drain the 1952b). Large landslides from The Barrier have west flank of the snow- and ice-covered Mount swept down Rubble Creek to Cheakamus River Fig. 4. Lowermost Cheakamus River valley in 1947 (BC400-74) and 1996 (BCB96099-59); compare with Fig. 5. Note wide, braided and anabranching channel pattern in 1947. The active channel is narrower and more stable in 1996. 322 J.J. Clague et al. / Geomorphology 53 (2003) 317–332 many times in the Holocene, most recently in 1855 or 1856 (Moore and Mathews, 1978). The upper reach of Culliton Creek contains a similar cliff developed in fractured basalts (Mathews, 1952b). This cliff, like The Barrier, is vulnerable to land- slides, although neither it nor the valley has been studied. Cheekye River heads in steep slopes devel- oped in late Pleistocene pyroclastic rocks. These slopes formed when the west half of Mount Gar- ibaldi volcano collapsed into Cheakamus Valley during deglaciation. A large fan (Cheekye fan, Fig. 2) has formed over Holocene time at the mouth of Cheekye River from hundreds of debris flows derived from the head of the basin. The most recent Cheekye debris flow to reach Cheakamus River occurred in 1958 (Jones, 1959). Our study area is located on the grounds of the North Vancouver Outdoor School (NVOS) about 4 km northeast of the confluence of Cheakamus and Squamish River, and 3 km north of Cheekye fan (Figs. 2 and 3). This part of Cheakamus valley is up to 850 m wide and is floored by a floodplain underlain by thick Quaternary sediments (Jordan- Knox et al., 2001). Bedrock slopes and the Cheekye fan constrict the floodplain to a width of about 100 m at the south, or downstream, end of the study area. The valley also narrows north of the mouth of Culliton Creek, and from there north to near Rubble Creek, Cheakamus River flows in a bedrock canyon (Cheakamus Canyon). A dam, built in 1955 to generate electricity, blocks Cheakamus River just north of Rubble Creek (Fig. 2). 3. Methods Historic changes in the planform of Cheakamus River at NVOS were documented by comparing British Columbia Government aerial photographs dating from 1947 to 1996.
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