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Thermo-Erosion Gullies Boost the Transition from Wet to Mesic Tundra Vegetation

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Thermo-Erosion Gullies Boost the Transition from Wet to Mesic Tundra Vegetation Biogeosciences, 13, 1237–1253, 2016 www.biogeosciences.net/13/1237/2016/ doi:10.5194/bg-13-1237-2016 © Author(s) 2016. CC Attribution 3.0 License. Thermo-erosion gullies boost the transition from wet to mesic tundra vegetation Naïm Perreault1,2, Esther Lévesque1,2, Daniel Fortier2,3, and Laurent J. Lamarque1,2 1Département des sciences de l’environnement, Université du Québec à Trois-Rivières, Trois-Rivières, QC, G9A 5H7, Canada 2Centre d’études nordiques, Université Laval, Québec, QC, G1V 0A6, Canada 3Département de géographie, Université de Montréal, Montréal, QC, H2V 2B8, Canada Correspondence to: Esther Lévesque ([email protected]) and Laurent J. Lamarque ([email protected]) Received: 29 June 2015 – Published in Biogeosciences Discuss.: 5 August 2015 Revised: 24 January 2016 – Accepted: 1 February 2016 – Published: 1 March 2016 Abstract. Continuous permafrost zones with well-developed mation on a relative short period of time for High Arctic polygonal ice-wedge networks are particularly vulnerable to perennial plant communities (5 to 10 years). Such succession climate change. Thermo-mechanical erosion can initiate the towards mesic plant communities can have substantial con- development of gullies that lead to substantial drainage of sequences on the food availability for herbivores and carbon adjacent wet habitats. How vegetation responds to this par- emissions of Arctic ecosystems. ticular disturbance is currently unknown but has the poten- tial to significantly disrupt function and structure of Arc- tic ecosystems. Focusing on three major gullies of By- lot Island, Nunavut, we estimated the impacts of thermo- 1 Introduction erosion processes on plant community changes. We explored over 2 years the influence of environmental factors on plant Warming in the Arctic is occurring twice as fast as the species richness, abundance and biomass in 62 low-centered global average (USGCRP, 2009; New et al., 2011; NOAA, wet polygons, 87 low-centered disturbed polygons and 48 2014). Perennially frozen ground (permafrost) has conse- ◦ mesic environment sites. Gullying decreased soil moisture by quently warmed by 2 C over the last 20 to 30 years (Chris- 40 % and thaw-front depth by 10 cm in the center of breached tiansen et al., 2010; Romanovsky et al., 2010), and there is polygons within less than 5 years after the inception of ice now evidence of a decrease in both permafrost area extent wedge degradation, entailing a gradual yet marked vegeta- across the Northern Hemisphere and permafrost thickness at tion shift from wet to mesic plant communities within 5 to the local scale (Beilman and Robinson, 2003; Payette et al., 10 years. This transition was accompanied by a five times 2004; Smith, 2011). decrease in graminoid above-ground biomass. Soil moisture Permafrost is tightly associated with biophysical compo- and thaw-front depth changed almost immediately following nents such as air temperatures, soil conditions, surface water, gullying initiation as they were of similar magnitude between groundwater, snow cover and vegetation (Jorgenson et al., older (> 5 years) and recently (< 5 years) disturbed polygons. 2010; Sjöberg, 2015). Permafrost impedes water to drain to In contrast, there was a lag-time in vegetation response to the deeper soil layers and maintains a perched water table and altered physical environment with plant species richness and saturated soils which favors the existence of wetlands (Woo, biomass differing between the two types of disturbed poly- 2012; Natali et al., 2015). Permafrost degradation that would gons. To date (10 years after disturbance), the stable state increase subsurface drainage and reduce the extent of lakes of the mesic environment cover has not been fully reached and wetlands at high latitudes (Avis et al., 2011; Jorgenson yet. Our results illustrate that wetlands are highly vulnerable et al., 2013; Beck et al., 2015) would thus have major conse- to thermo-erosion processes, which drive landscape transfor- quences on ecosystem structure and function (Collins et al., 2013; Jorgenson et al., 2013). It would also strongly influ- Published by Copernicus Publications on behalf of the European Geosciences Union. 1238 N. Perreault et al.: Thermo-erosion gullies boost vegetation transition ence variations of active layer depths (Wright et al., 2009; 2 decades (Allard, 1996; Fortier and Allard, 2004; Gauthier Shiklomanov et al., 2010; Gangodagamage et al., 2014), as et al., 2013; Godin et al., 2014), offered a unique opportunity illustrated by long-term monitoring sites throughout the cir- to specifically assess the response of wetlands to gullying. cumpolar North (Tarnocai et al., 2004; Nelson et al., 2008; The following questions were addressed: (1) to what extent Smith et al., 2009; Shiklomanov et al., 2010). thermo-erosion gullying modifies environmental conditions Several forms of ground and massive ice can be found of low-centered wetland polygons? (2) How do plant com- within permafrost (Rowland et al., 2010), especially ice munities cope with these geomorphological changes, i.e. do wedges in regions where winter temperatures enable ther- we observe shifts in plant diversity, abundance and produc- mal contraction cracking (Fortier and Allard, 2005; Kokelj et tivity? al., 2014; M. T. Jorgenson et al., 2015; Sarrazin and Allard, 2015). Continuous permafrost zones with well-developed polygonal ice-wedge networks are particularly vulnerable to 2 Methods climate change because ice wedges are usually found near 2.1 Study area the top of permafrost (Smith et al., 2005; Jorgenson et al., 2006; Woo et al., 2008; Vonk et al., 2013). In these regions, This study took place in the Qarlikturvik valley of Bylot Is- thawing permafrost can result in ground ice erosion and dis- land, Nunavut, Canada (73◦090 N, 79◦570 W; Fig. 1a). Bound placement of sediments, carbon and nutrients by drainage to the North and South by plateaus < 500 m a.s.l., it con- (Rowland et al., 2010; Godin et al., 2014; Harms et al., 2014). nects C-79 and C-93 glaciers to the Navy Board Inlet sea This thermo-erosion process has especially been observed via a proglacial river. The sampling sites were specifically across North-America (Grosse et al., 2011), in Siberia (Gün- located on the valley floor (ca. 65 km2/, which is character- ther et al., 2013) and in the Antarctic Dry Valleys (Levy ized by a low-centered polygon landscape that has resulted et al., 2008). On Bylot Island, Nunavut, thermo-mechanical from ice wedges development and sediment accumulation erosion by water has initiated permafrost tunneling and the during the late Holocene (Ellis and Rochefort, 2004; Fortier development of gully networks in aeolian, organic and collu- and Allard, 2004; Fortier et al., 2006; Ellis et al., 2008). Two 2 vial depositional environments of nearly 158 000 m (Fortier baseline vegetation types can be recognized. Wetlands, of- et al., 2007; Godin and Fortier, 2012a; Godin et al., 2014; ten associated with intact low-centered polygons, represent Veillette et al., 2015). A fine-scale spatio-temporal monitor- ca 23 % of the valley area (Hughes et al., 1994) and are ing of the six largest gullies showed that their development dominated by sedges (Carex aquatilis, Eriophorum angus- −1 −1 rates ranged from 14 to 25 m yr going up to 80 m yr dur- tifolium, Eriophorum scheuchzeri), grasses (Dupontia fish- ing their inception (Godin and Fortier, 2012b), leading to eri, Pleuropogon sabinei; Gauthier et al., 1995) and fen substantial changes in the drainage network and increasing mosses (Drepanocladus spp.; Ellis et al., 2008; Pouliot et eroded area throughout the valley (Godin et al., 2014). To al., 2009). Mesic environments, such as low-centered poly- date, the contribution of thermal-erosion and lateral erosion gon rims, gently sloping terrain and hummocky tundra, sup- processes in permafrost feedbacks to climate has yet to be port a more diverse group of species including Salix spp., documented. Vaccinium uliginosum, Arctagrostis latifolia, Poa arctica and Many observational and experimental studies have high- Luzula confusa with Aulacomnium spp. as dominant moss lighted shifts in tundra plant community structure and plant species (Zoltai et al., 1983). As a result, the valley houses species productivity in response to warming temperatures many herbivores such as snow geese (in summer) and brown (Jonsdottir et al., 2005; Hudson and Henry, 2010; Epstein and collared lemmings (Gauthier et al., 1995; Gruyer et al., et al., 2013; Naito and Cairns, 2015). In contrast, little is 2008), thus representing a critical environment for tundra known about how thermo-erosion gullying affects plant com- food web (Gauthier et al., 2011; Legagneux et al., 2012). munity structure and plant species abundance. Yet, this in- formation is urgently needed as vegetation plays an impor- 2.2 Field sites tant role in structuring Arctic ecosystems and regulating per- mafrost response to climate change (Jorgenson et al., 2010; Our work was specifically conducted around three gullies Gauthier et al., 2011; Legagneux et al., 2012). Wetlands that were selected among the 36 identified in the valley serve as preferred grounds for Arctic herbivores such as snow (Godin and Fortier, 2012b). These gully networks have orig- geese (Gauthier et al., 1996; Massé et al., 2001; Doiron et inated from snowmelt water infiltration into cavities of the al., 2014). They are also expected to produce more methane frozen active layer and the subsequent formation of under- compared to shrub-dominated areas (Olefeldt et al., 2013; ground tunnels that have ended up collapsing (Fortier et al., Nauta et al., 2015; Treat et al., 2015). 2007; Godin and Fortier, 2010). The gullies R08p and R06, The present study aimed at examining plant community respectively 835 and 717 m long, are characterized by on- patterns following thermo-erosion gullying processes. By- going thermo-erosion processes (Fortier et al., 2007; Godin lot Island, where geomorphological and ecological processes and Fortier, 2012b) whilst the gully RN08, 180 m long, has in response to climate change have been monitored for over not been actively eroding in recent years.
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