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Taiga Shield Ecozone+ Evidence for Key Findings Summary

Theme: Biomes

 

Forests

Key finding 1
Theme: Biomes

National key finding
At a national level, the extent of forests has changed little since 1990; at a regional level, loss of forest extent is significant in some places. The structure of some Canadian forests, including species composition, age classes, and size of intact patches of forest, has changed over longer time frames.

Forest-tundra zone

The northern boundary of the Taiga Shield is defined by the treeline – which is not a sharp line where trees end, but rather a zone of transition from increasingly sparse trees to tundra. The emerging picture for this forest-tundra zone is one of change, but not a uniform expansion of treeline.

West of Hudson Bay

The forest-tundra zone averages 145 km in width in the western Taiga Shield.Footnote21 The presence or absence of trees at points within this transition zone depends on microclimate and topography,Footnote22 as well as on past climatic conditions.Footnote23 An analysis of the treeline zone for Canada west of Hudson Bay (including the treeline zone in the Taiga Plains and Taiga Cordillera ecozones+) shows no net increase in conifers, but significant changes in other land cover types (see box).

East of Hudson Bay

In the Quebec part of the eastern Taiga Shield, trees in the forest-tundra zone have grown faster and taller since the 1970sFootnote24 but distribution of trees has not changed greatly,Footnote25 although white spruce has recently (over the past 50 years) expanded along the east coast of Hudson Bay.Footnote26 In Labrador, treelines have expanded northward and up slopes over the past 50 years along the coast, but not inland.Footnote27

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The forest-tundra zone west of Hudson Bay
Figure 4: Vegetation changes in the treeline zone, west of Hudson Bay 1985-2006

Mean change over 22 years based on analysis of early spring and summer satellite images. The inset map, adapted from Olthof and Pouliot, 2010,Footnote28 shows the area analysed.
graph
Source: data from Olthof and Pouliot, 2010Footnote28
Long Description for Figure 4.

This graph shows the following information:

-Mean percent change
Bare-0.094
Lichen-0.039
Conifer0.005
Herb0.124
Shrub0.150

The inset map depicts the area analysed in the study, which extends along the treeline zone from the northern part of the Yukon across the Northwest Territories and into the southeastern Nunavut/northern Manitoba.

A study using satellite imagery to look at recent trends along the treeline zone west of Hudson Bay found only a small net increase in tree cover, but major changes in vegetation cover (Figure 4).Footnote28 Tree cover increased in the northern half of the zone, but this was mainly offset by decreases in the southern half. The changes were more pronounced to the west of the Taiga Shield, especially west of the Mackenzie Delta, likely related to drier conditions due to the marked warming trends in these regions.Footnote29 The biggest changes were an increase in shrubs and, in the northwest of the treeline zone, a replacement of lichen cover and bare land with small, non-woody plants (herbs).

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Wetlands

Key finding 3
Theme: Biomes

National key finding
High loss of wetlands has occurred in southern Canada; loss and degradation continue due to a wide range of stressors. Some wetlands have been or are being restored.

Wetlands cover roughly 13% of the surface area of the Taiga Shield, Footnote18 and trends in the total wetlands area are unknown. Ponds are increasing in parts of Quebec and Manitoba, and probably elsewhere in the Ecozone+ due to melting of frozen peatlands (see Permafrost trends on page 17). This wetland expansion is related to changes in temperature and precipitation patterns. Some reduction of wetlands area has resulted from hydroelectric developments in northern Quebec (see Ecosystem Conversion on page 23). Among the documented changes associated with hydroelectricity development east of James Bay is a reduction in the area of string bogs (narrow, low ridges with wet depressions or pools) in Quebec's Lake Plateau area. These wetlands provide habitat for shorebirds and bald eagles.Footnote30 Both the James Bay (Quebec)Footnote31 and Churchill River (Newfoundland and Labrador)Footnote32 hydro projects will be expanded in the next few years-including development of two substantial reservoirs and diversion of half the flow of the Rupert River-which is likely to have a further impact on wetlands in the eastern Taiga Shield.

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Lakes and Rivers

Key finding 4
Theme: Biomes

National key finding
Trends over the past 40 years influencing biodiversity in lakes and rivers include seasonal changes in magnitude of stream flows, increases in river and lake temperatures, decreases in lake levels, and habitat loss and fragmentation.

Changes in hydrology on unmanaged streams within the Ecozone+ vary. The streams to the west of the Ecozone+ are part of the Mackenzie River Basin, which has, overall, experienced climate-related increases in streamflow, (1970-2000) while much of the drainage to the east is to Hudson and James bays, which have experienced no net change in total freshwater input (1964-2010). Major changes in the seasonal flow patterns of several rivers, especially those draining to James Bay, have resulted from dams and diversions, starting in 1973.

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Regional trends

Large-scale trends relevant to the Taiga Shield Ecozone+ are:
Mackenzie River Basin: increase in annual winter flows and in annual minimum flows from 1970 to 2000, and earlier spring peak flows. Flows in early summer and late fall, as well as the annual mean flow, decreased slightly. The trends correlate with warmer winters and springs, less winter snow, and more spring rain.Footnote33 Hudson Bay watershed: discharge declined from the mid-1960s to the mid-1980s, followed by a period of relatively high flows and an upward trend (Figure 5). It is unclear to what degree these trends are related to climate change and/or decadal climate oscillations.Footnote34 While there was no trend in total discharge over the entire period, streamflow increased in the winter and decreased in the summer from 1964 to 2008. This seasonal shift is attributed to the strong influence of increasing flow regulation in this watershed: water stored in spring and summer is released in the winter for power generation.Footnote34

Figure 5: Total annual discharge into Hudson and James bays, 1964-2010.

Total discharge is estimated based on records from 23 rivers, including the regulated La Grande Rivière.
Graph
Source: Déry et al., 2011Footnote34 with 2009 and 2010 data provided by S.J. Déry
Long Description for Figure 5.

This line graph shows the following information:

YearTotal discharge (km3)
1964518
1965544
1966605
1967527
1968578
1969601
1970542
1971527
1972493
1973493
1974558
1975529
1976456
1977486
1978515
1979591
1980454
1981410
1982463
1983507
1984490
1985561
1986545
1987488
1988489
1989446
1990473
1991450
1992532
1993498
1994493
1995507
1996525
1997554
1998475
1999530
2000546
2001526
2002548
2003485
2004551
2005635
2006550
2007592
2008616
2008603
2009631
2010498

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Trends within the ecozone+: streams with natural flow regimes

This section is based on Canada-wide analyses performed by Cannon et al. 2011Footnote35 for the 2010 Ecosystem Status and Trends Report.

Within both eastern and western parts of the Taiga Shield, hydrometric records are sparse and often too short to detect trends. Only two stations (Camsell River, NWT, and Seal River, Manitoba) – both in the western Taiga Shield – have adequate stream discharge and climate records (1961-2003) to examine trends over the annual cycle.Footnote35 Both of these streams showed significant streamflow increases throughout the year, with the exception of spring (streamflow for Camsell River is shown in Figure 6). These changes could be due to a combination of the increased precipitation coupled with the warmer winters and springs recorded in the vicinity of the streams.Footnote35

Figure 6: Streamflow change at Camsell River, 1961-1982 compared with 1983-2003

Streamflow change at Camsell River, 1961-1982 compared with 1983-2003. Streamflow was analyzed in 5-day periods, comparing 73 periods over the annual cycle.
graph
Source: Cannon et al., 2011Footnote35
Long Description for Figure 6

A graph comparing streamflow in the Camsell River shows that recent years (1983-2003) have experienced higher streamflow than previous years (1961-1982). Streamflow has been significantly higher through most of the year, except in the spring (May and June). The data is taken from a gauging station on the Camsell River in the Northwest Territories and the analyzed in 5 day periods, comparing 73 periods over an annual cycle.

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Trends within the ecozone+: streams with managed flow regimes

Several major hydroelectricity developments, mainly in the eastern part of the ecozone+, have altered flow regimes since the 1970s. The La Grande (James Bay) hydroelectric development in Quebec has resulted in dramatic changes to some rivers in the eastern Taiga Shield. The complex was constructed in two phases, the first one during 1973-1985 and the second one during 1987-1996. Three main rivers were diverted into La Grande River: the Eastmain, Opinaca, and Caniapiscau. As a result of these diversions, the mean annual flow of La Grande River at its mouth doubled and its mean winter flow increased more than tenfold.Footnote30

Main impacts from these diversions include changes to estuarine, coastal and marine systems from the increased under-ice freshwater plume of La Grande RiverFootnote36 (see Coastal on page 15).

Fishing yields fluctuated after diversions were put in place, but, overall, yields stabilized at levels above or close to those found under natural conditions.Footnote37 In general, fish species composition and growth rates in the reduced-flow rivers were similar before and after the flow reductions.

Changes to fish populations in rivers with altered flow include:

  • La Grande River: displacement of species that are not tolerant of cold water – walleye (Sander viterus) and cisco (Coregonus sp.) – by cold-water tolerant species – round whitefish (Prosopium cylindraceum) and brook trout (Salvelinus fontinalis).Footnote37 Mean maximum summer water temperatures in the river were lowered from 16°C to 8°C following development.Footnote37
  • Eastmain River: lake sturgeon (Acipenser fulvescens) numbers declined, related to flow reduction and habitat fragmentation by weirs.Footnote37, Footnote38 Fishing pressure may also have been a factor in this decline.Footnote37, Footnote38 The James Bay population of lake sturgeon was assessed as being of Special Concern by COSEWIC in 2005, confirmed in 2006,Footnote38 citing declines in habitat and possibly abundance, related to existing and projected hydroelectric development.

Changes affecting fish in the reservoirs are discussed under Dams and reservoirs on page 28.

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Coastal

Key finding 5
Theme: Biomes

National key finding
Coastal ecosystems, such as estuaries, salt marshes, and mud flats, are believed to be healthy in less-developed coastal areas, although there are exceptions. In developed areas, extent and quality of coastal ecosystems are declining as a result of habitat modification, erosion, and sea-level rise.

The eastern Taiga Shield Ecozone+ has coastlines along James and Hudson Bays, Ungava Bay, and the Atlantic Ocean. Little information on status and trends in coastal ecosystems was found for this report. The James and Hudson bays region is undergoing a high rate of isostatic rebound, meaning that new soil and vegetation zones are forming. Eelgrass beds, formerly extensive along the James Bay coast, declined rapidly in the late 1990s, recovering somewhat to 2011. Footnote39

A severe reduction in eelgrass (Zostera marina) along the James Bay coast was reported by Cree residents of the region in 1998; this decline was also detected in monitoring conducted by Hydro Québec. Footnote40 By 2004, monitoring indicated that some recovery had taken place, confirmed by further monitoring in 2009 (Figure 7)Footnote41 and 2011. Footnote39

Eelgrass beds were among the most extensive in North America, distributed all along the east coast of James Bay, covering 250 km2, and found at depths of 0.5 to 4 mFootnote42 prior to their rapid decline in density and biomass around 1998 (Figure 7). Eelgrass in James Bay provides shelter for small fish and invertebrates and is important food and habitat for migrating and wintering waterfowl, Canada geese (Branta canadensis) and Brant geese (Branta bernicla) in particular, and provides foraging areas for Arctic terns.Footnote43 Footnote44 Footnote45 Eelgrass distribution and growth are influenced by salinity;Footnote45 low salinity or high temperatures can make eelgrass vulnerable to disease.Footnote43

Figure 7: Decline of eelgrass in James Bay: example of monitoring results for leaf biomass and shoot density, Kakassituq station, 1988-2009.

Samples were taken at several depths at 6 sites – this figure shows results typical at all depths for 5 of the 6 sites. The 6th site (Dead Duck Bay, the station furthest to the south of the La Grande River mouth) showed no change.
Graph
Source: GENIVAR, 2009Footnote41
Long Description for Figure 7.

Three bar graphs showing the following information:

a) 0.5 m
YearMean dry biomass (g/m2)Mean number of shoots (N/m2)
1988194983
19892631,641
1990234836
1991189931
19933821,737
19943541,039
19954561,751
1999737
2000656
200936292
b) 1.0 m
YearMean dry biomass (g/m2)Mean number of shoots (N/m2)
1988472689
1989358880
1990272578
1991294699
1993415887
1994295665
19955591,108
19991843
20001272
2009112429
c) 1.5 m
YearMean dry biomass (g/m2)Mean number of shoots (N/m2)
1988399512
1989387833
1990317516
1991392757
1993361787
1994298617
1995548948
19996375
2000840
2009124409

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Explanations advanced for the decline include:

  1. a disease outbreak triggered by unusually high summer and winter temperatures, along with changes in the coast from isostatic rebound and other changes related to a warming climate;Footnote40
  2. impaired growth and survival due to reduced salinity of water in James Bay resulting from larger and more frequent discharges of fresh water via the La Grande River (due to diversions, see Dams and diversions, page 25).Footnote45

As of 2011, vast eelgrass beds can be seen at various locations along James Bay. Distribution and abundance of eelgrass has not recovered to pre-decline levels, however, and recovery is not uniform along the coast.Footnote39

Ice across biomes

Key finding 7
Theme: Biomes

National key finding
Declining extent and thickness of sea ice, warming and thawing of permafrost, accelerating loss of glacier mass, and shortening of lake-ice seasons are detected across Canada's biomes. Impacts, apparent now in some areas and likely to spread, include effects on species and food webs.

Lake ice trends

An analysis of seven large lakes in or at the edges of the ecozone+, between 1970 and 2004, showed variable trends in timing of freeze-up and ice break-up, with few changes being statistically significant.Footnote46 National trends are towards an earlier break-up of lake ice, with less consistent trends in freeze-up timing (1960s or 1970s to 1990s, when most lake ice monitoring was discontinued).Footnote17

Permafrost trends

Permafrost is thawing at a rapid rate in the eastern Taiga Shield, resulting in a change in the landscape from dry, lichen-heath ecosystems supporting black spruce trees and dotted with ponds to wetter landscapes with ponds, and characterized by fen and bog vegetation.Footnote47-Footnote49 As well as altering habitats, these changes affect carbon flux as the thawing of peat and formation of ponds releases carbon to the atmosphere, while the subsequent transition to fen/bog vegetation stores carbon. Permafrost is also degrading in peatlands in northern Manitoba (based on field investigations over the latter half of the 20th century).Footnote50 This trend is likely becoming more widespread in the western Taiga Shield as well, although data are not available.

Broad-scale permafrost distribution in the Taiga Shield ecozone+ differs between east and west of Hudson Bay, with the east having less extensive permafrost (Figure 8). In the eastern Taiga Shield, the sporadic permafrost zone is characterized by frozen peat plateaus and palsas (mounds of peat or soil containing ice lenses). Formation and degradation of these permafrost landforms are influenced by air temperature and by insulation from snow cover and from peat.Footnote47 When the permafrost is degraded, the resulting melted ice forms ponds (called thermokarst ponds).

Figure 8: Permafrost distribution, Taiga Shield ecozone+.
Map
Source: adapted from Smith, 2011Footnote11
Long Description for Figure 8.

This map shows the distribution of permafrost zones in northern Canada and highlights the differences in permafrost in the eastern and western parts of the Taiga Shield Ecozone+. The eastern section is dominated by sporadic permafrost, with only a small area of extensive discontinuous permafrost in the north. In contrast, in the west, only areas in the south of the ecozone+ (sections in Alberta, Saskatchewan and Manitoba) are classified as sporadic permafrost; discontinuous permafrost and continuous permafrost dominate in the western Taiga Shield.

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Three studies in Quebec show the extent of change in permafrost in the past 50 years (summarized in Figure 9).

  1. A study mapping palsas and thermokarst ponds along the Boniface River in the discontinuous permafrost zone at the northern edge of the ecozone+ (site A, Figure 9)Footnote47 found that the area occupied by palsas decreased by 23% between 1957 and 2001, while 76% of present-day thermokarst pond area had formed since 1957. No new palsas developed along the river during this period. Permafrost degradation was most severe close to the river where water fluctuations had a strong influence.
  2. A study mapping change in a peatland east of Hudson Bay (site B, Figure 9)Footnote48 found that the area was mainly frozen in 1957, with about 18% of the surface covered in thermokarst ponds. Palsa mounds, being well-drained, supported growth of lichens and black spruce trees. By 2003 only 13% of the surface area remained as permafrost, with the remainder being a mix of thermokarst ponds and fen/bog vegetation (sedges and Sphagnum moss). Fen/bog vegetation was virtually absent in 1957 but covered half the study area by 2003. Spruce trees died as the permafrost decayed and their roots became flooded. The annual rate of permafrost degradation approximately doubled in the last decade of the study to -5.3% per year; this acceleration in melt rate was likely related to increasing trends in summer temperatures and precipitation since the mid-1990s.
  3. A survey over a broad area of the James Bay regionFootnote49 showed that changes documented at the above sites are widespread. The landscape in the zone of sporadic permafrost is in transition from dry, lichen-covered palsas interspersed with ponds to a wetter ecosystem dominated by larger ponds, bogs and fens. The southern limit of permafrost has moved about 130 km north, mainly within about the past 50 years. North of the current permafrost boundary (in the vicinity of "C" on Figure 9), permafrost is in an advanced state of degradation – palsas in bogs observed and surveyed in this region up to 2004 had shrunk or disappeared by 2005.

Lichens, important forage for caribou (Rangifer tarandus), are maintained in the James Bay area by periodic fire and by permafrost – both of which create dry micro-environments. If, as seems likely, the permafrost continues to degrade and disappears within a few years, the resulting wetter bog ecosystems will lead to widespread declines in lichen.Footnote49

Figure 9: Change in permafrost landforms, thermokarst ponds and extent in permafrost in three studies in northern Quebec.

Studies A and B are based on ground surveys and 1957 air photos.
Study C involved helicopter surveys along two 350 km north-south transects conducted in 2004 and 2005. These were supplemented with ground surveys, defined the northern extent of permafrost by the presence of palsas and the southern extent of thermokarst ponds (the latter indicating the presence of permafrost within about the past 50 years). "C" indicates the approximate location of palsa/thermokarst pond study sites.
Map
Source: Study A. Vallée and Payette, 2007;Footnote47 Study B. Payette et al., 2004;Footnote48 and Study C. Thibault and Payette, 2009Footnote49
Long Description for Figure 9.

This figure includes a map and two graphs documenting changes in the total area, land cover, and permafrost limits in three studies from northern Quebec. The bar graph on the top left depicts a 23% decrease in the total area of palsas (mounds of peat or soil containing ice lenses) and a 76% increase in pond area between 1957 and 2001; the location of the study site is indicated on the map at point "A", along the Boniface River. The line graph on the top right shows the following information:

Yearpermafrostpondsfen
195782%18%0%
198338%32%28%
199328%30%42%
200313%37%50%

In addition to showing the locations of the three studies, the map at the bottom also depicts a 130 km northward change in the southern permafrost limit, documented in a more recent study (study "C", 2004 and 2005), which defined the southern extent of areas which were formerly permafrost by the presence of thermokarst ponds.

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Footnotes

Footnote 11

Smith, S. 2011. Trends in permafrost conditions and ecology in Northern Canada. Canadian Biodiversity: Ecosystem Status and Trends 2010, Technical Thematic Report No. 9. Canadian Councils of Resource Ministers. Ottawa, ON. iii + 22 p.

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Footnote 17

Monk, W.A. and Baird, D.J. 2011. Biodiversity in Canadian lakes and rivers. Canadian Biodiversity: Ecosystem Status and Trends 2010, Technical Thematic Report No. 19. Canadian Councils of Resource Ministers. Ottawa, ON. Draft report.

Return to footnote 17

Footnote 18

Wiken, E., Moore, H. and Latsch, C. 2004. Peatland and wetland protected areas in Canada. Wildlife Habitat Canada Science Report. Wildlife Habitat Canada. Ottawa, ON. 18 p.

Return to footnote 18

Footnote 21

Timoney, K.P., Roi, G.H.L., Zoltai, S.C. and Robinson, A.G. 1992. The high Subarctic forest-tundra of northwestern Canada: position, width, and vegetation gradients in relation to climate. Arctic45:1-9.

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Footnote 22

Timoney, K.P. 1995. Tree and tundra cover anomalies in the Subarctic forest-tundra of northwestern Canada. Arctic48:13-21.

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Footnote 23

Nichols, H. 1976. Historical aspects of the northern Canadian treeline. Arctic29:38-47.

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Footnote 24

Gamache, I. and Payette, S. 2004. Height growth response of tree line black spruce to recent climate warming across the forest-tundra of eastern Canada. Journal of Ecology92:835-845.

Return to footnote 24

Footnote 25

Gamache, I. and Payette, S. 2005. Latitudinal response of Subarctic tree lines to recent climate change in eastern Canada. Journal of Biogeography32:849-862.

Return to footnote 25

Footnote 26

Laliberte, A.C. and Payette, S. 2008. Primary succession of Subarctic vegetation and soil on the fast-rising coast of eastern Hudson Bay, Canada. Journal of Biogeography35:1989-1999.

Return to footnote 26

Footnote 27

Payette, S. 2007. Contrasted dynamics of northern Labrador tree lines caused by climate change and migrational lag. Ecology88:770-780.

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Footnote 28

Olthof, I. and Pouliot, D. 2010. Treeline vegetation composition and change in Canada's western Subarctic from AVHRR and canopy reflectance modeling. Remote Sensing of Environment114:805-815.

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Footnote 29

Pisaric, M.F.J., Carey, S.K., Kokelj, S.V. and Youngblut, D. 2007. Anomalous 20th century tree growth, Mackenzie Delta, Northwest Territories, Canada. Geophysical Research Letters34, L05714, 5 p..

Return to footnote 29

Footnote 30

Hayeur, G. 2001. Summary of knowledge acquired in northern environments from 1970 to 2000. Hydro-Québec. Montréal, QC. x + 110 p. .

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Footnote 31

Hydro-Québec. 2010. Eastmain-1-A/Sarcelle/Rupert project [online]. Hydro-Québec. (accessed December, 2010).

Return to footnote 31

Footnote 32

Nalcor Energy and Government of Newfoundland and Labrador. 2011. Report of the Joint Review Panel -- Lower Churchill hydroelectric generation project. Government of Canada and Government of Newfoundland and Labrador. Ottawa, ON and St. John's, NL. 355 p.

Return to footnote 32

Footnote 33

Abdul Aziz, O.I. and Burn, D.H. 2006. Trends and variability in the hydrological regime of the Mackenzie River Basin. Journal of Hydrology319:282-294.

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Footnote 34

Déry, S.J., Mlynowski, T.J., Hernández-Henríquez, M.A. and Straneo, F. 2011. Interannual variability and interdecadal trends in Hudson Bay streamflow. Journal of Marine Systems88:341-351-.

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Footnote 35

Cannon, A., Lai, T. and Whitfield, P. 2011. Climate-driven trends in Canadian streamflow, 1961-2003. Canadian Biodiversity: Ecosystem Status and Trends 2010, Technical Thematic Report No. 19. Canadian Councils of Resource Ministers. Ottawa, ON. Draft report.

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Footnote 36

Hydro-Québec and GENIVAR Groupe Conseil inc. 2005. Environmental monitoring of the La Grande-2-A and La Grande-1 projects: abridged summary report 1987-2000: La Grande Rivière winter plume. Joint report by Hydro-Québec and GENIVAR Groupe Conseil Inc. 27 p. + appendix.

Return to footnote 36

Footnote 37

Therrien, J., Verdon, R. and Lalumière, R. 2004. Environmental monitoring at the La Grande complex. Changes in fish communities. Summary report 1977-2000. GENIVAR Groupe Conseil Inc. and Direction Barrages et Environnement, Hydro-Québec Production. 129 p. + appendices.

Return to footnote 37

Footnote 38

COSEWIC. 2006. COSEWIC assessment and update status report on the lake sturgeon Acipenser fulvescens in Canada. Committee on the Status of Endangered Wildlife in Canada. Ottawa, ON. xi + 107 p.

Return to footnote 38

Footnote 39

Consortium Waska-GENIVAR. 2011. Centrales de l'Eastmain-1-A et de la Sarcelle et dérivation Rupert. Suivi de la zostère marine de la côte nord-est de la baie James. Rapport d'étude 2011. Rapport du Consortium Waska-GENIVAR inc. pour Hydro-Québec Production. 57 p.  + appendices.

Return to footnote 39

Footnote 40

Hydro-Québec and GENIVAR Groupe Conseil inc. 2005. Environmental monitoring at the La Grande complex: abridged summary report 1988-2000: eelgrass meadows of the northeast coast of James Bay. Joint report by Hydro-Québec and GENIVAR Groupe Conseil Inc. 42 p. + appendices.

Return to footnote 40

Footnote 41

GENIVAR. 2010. Centrales de l'Eastmain-1-A et de la Sarcelle et dérivation Rupert. Suivi de la zostère marine de la côte nord-est de la baie James. État de référence 2009. Rapport de GENIVAR Société en commandite pour Hydro-Québec et la Société d'énergie de la Baie James. 54 p. + appendices.

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Footnote 42

Lalumière, R., Messier, D., Fournier, J.J. and Mcroy, C.P. 1994. Eelgrass meadows in a low Arctic environment, the northeast coast of James Bay, Quebec. Aquatic Botany47:303-315.

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Footnote 43

Standing Committee on Fisheries and Oceans. 2008. Fifth report of the Standing Committee on Fisheries and Oceans to the House of Commons. Government of Canada. Ottawa, ON. 2 p.

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Footnote 44

Hanson, A.R. 2004. Status and conservation of eelgrass (Zostera marina) in eastern Canada. Technical Report Series No. 412. Environment Canada, Canadian Wildlife Service, Atlantic Region. Sackville, NB. 40 p.

Return to footnote 44

Footnote 45

Short, F.T. 2008. Report to the Cree Nation of Chisasibi on the status of eelgrass in James Bay. Jackson Estuarine Laboratory. Durham, NH. 30 p.

Return to footnote 45

Footnote 46

Latifovic, R. and Pouliot, D. 2007. Analysis of climate change impacts on lake ice phenology in Canada using the historical satellite record. Remote Sensing of Environment106:492-507.

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Footnote 47

Vallée, S. and Payette, S. 2007. Collapse of permafrost mounds along a Subarctic river over the last 100 years (northern Québec). Geomorphology90:162-170.

Return to footnote 47

Footnote 48

Payette, S., Delwaide, A., Caccianiga, M. and Beauchemin, M. 2004. Accelerated thawing of Subarctic peatland permafrost over the last 50 years. Geophysical Research Letters31:1-4.

Return to footnote 48

Footnote 49

Thibault, S. and Payette, S. 2009. Recent permafrost degradation in bogs of the James Bay area, northern Quebec, Canada. Permafrost and Periglacial Processes20:383-389.

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Footnote 50

Camill, P. 2005. Permafrost thaw accelerates in boreal peatlands during late-20th century climate warming. Climatic Change 68:135-152.

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