RECONNAISSANCE STUDY OF
SOILS AND VEGETATION
OF SOMERSET AND
PRINCE OF WALES ISLANDS, N .W .T .
by
V . W00
Soil Science Department
University of Manitoba TABLE OF CONTENTS
Page No .
1 . INTRODUCTION ...... 1
2 . OBJECTIVES ...... 1
3 . STATE OF KNOWLEDGE ...... 4 3 .1 Climate ...... 4 3 .2 Geology ...... 5 3 .3 Physiography ...... 8 3 .4 Glacial History ...... 3 .5 Soils ...... 12 3 .6 Vegetation ...... 12 3 .7 Wildlife ...... 14
4 . METHODOLOGY ...... 15 4 .1 Sampling ...... 15 4 .2 Detailed Sites ...... 16 4 .3 Laboratory Analytical Procedures ...... 19 4 .4 Nomenclature and Identification of Vegetation . . . . . 19
5 . RESULTS 5 .1 System of Soil Classification ...... 20 5 .2 Use of Soils - Vegetation Map ...... 21 5 .3 Ecological Regions ...... 24 5 .4 Ecological Districts ...... 25 5 .41 Ecological Districts of Somerset . Island . . . . . 25 5 .42 Ecological Districts of Prince of Walies Island . 35 5 .5 Soil Associations of Somerset and Prince of Wales Islands ...... 43 5 .6 Chemical Properties of Some Major Soil Associations . . 72 5 .7 Vegetation Communities ...... 76 5 .71 Polar Desert Type ...... 76 5 .72 Moss-Grass Vegetation Type ...... 76 5 .73 Dwarf-Shrub Vegetation Type ...... 77 5 .74 Sedge Meadow Vegetation Type ...... 82 5 .8 Species List of Vegetation ...... 86
6 . DISCUSSIONS AND ADDITIONAL RESULTS ...... 94 6 .1 Soil Forming Processes ...... 94 6 .2 Rheotropic Soils ...... 98 6 .3 Earth Hummocks ...... 100 6 .4 Organo Cryosols ...... 104 6 .5 Soil Development and Chronology ...... 107 TABLE OF CONTENTS (cont'd)
Page No .
6 .6 Radiocarbon Age Determinations ...... 109 6 .7 Vegetation Survival in the Arctic Environment . . . . . 111 6 .8 Vegetation and Cryoturbation ...... 114 6 .9 Vegetation Distribution and Petrology ...... 116 6 .10 Wildlife ...... 117
7 . RECOMMENDATIONS ...... 119 7 .1 Sensitive Environments ...... 119 7 .11 Tabular Ground Ice ...... 119 7 .12 Vegetation Cover ...... 122 7 .13 Frost heaving ...... 123 7 .14 Mass Wasting ...... , ...... 123 7 .15 Rheotropic Soils ...... 124 7 .16 Wildlife Habitats ...... 125
8 . CONCLUSIONS ...... 126
9 . REFERENCES ...... 127 Page No .
Descriptions of Ecological Districts of Somerset Island : 25 High Arctic Ecoregion ...... 25 Hl Central Plateau ...... 25 H2 West Somerset Upland ...... 27 H3 Cunningham Inlet ...... 28
Mid-Arctic Ecoregion ...... 29 Ml Cape Garry Plateau ...... 29 M2 South Somerset Till Plain ...... 30 M3 South Somerset Ranges ...... 31 M4 Central Creswell Valley ...... 31 M5 Creswell Lowland ...... 32 M6 Stanwell-Fletcher Basin ...... 32 M7 Hazard Inlet Beaches ...... 33
Descriptions of Ecological Districts of Prince of Wales Island : 35 High Arctic Ecoregion ...... 35 Hl Cape Hardy Highlands ...... 35 H2 North Central Uplands ...... 35 H3 Drake Bay Uplands ...... 36 H4 Mount Clarendon Lowlands ...... 36 H5 Back Bay Lowlands ...... 37
Mid-Arctic Ecoregion ...... 37 Ml East Prince of Wales Highlands ...... 37 M2 Cape Henry Kellett Uplands ...... 38 143 Central Prince of Wales Lowlands ...... 38 M4 Mount Cowie Lowlands ...... 39 M5 Fisher Lake Lowlands ...... 39 M6 Prescott Island Uplands ...... 40
Descriptions of Soil Associations of Somerset and Prince of Wales Islands : Aston Association (As) ...... 43 Batty Bay Association (Ba) ...... 43 Baring Channel Association (Bc) ...... 44 Birmingham Bay Association (Br) ...... 45 Cape Garry Association (Cg) ...... 46 Cape Hardy Association (Ch) ...... 47 Cape Granite Association (Cg) ...... 48 Creswell Association (Cr) ...... 49 Elwin River Association (El) ...... 50 Fearnall Bay Association (Fb) ...... 51 Fiona Lake Association (Fo) ...... 52 Page No .
Fitz Roy Association (Fz) ...... 53 Four Rivers Association (Fr) ...... 54 Fury Association (Fu) ...... 55 Garnier Bay Association (Gb) ...... 55 Gifford Point Association (Gf) ...... 58 Howe Harbour Association (Hw) ...... 58 Hunting Association (Hn) ...... 59 Leopold Association (Lp) ...... 60 Lyons Point Association (ly) ...... 61 Mount Clarendon Association (Mc) ...... 62 Mount Matthias Association (Mm) ...... , . . . . . 62 Otrick Island Association (0t) ...... 64 Palmerston Point Association (Pr) ...... 64 Prince Regent Association (Pg) ...... 64 Scarp Brook Association (Sb) ...... 66 Stanwell Fletcher Association (SO ...... 67 Transition Bay Association (Tb) ...... 68 Two Rivers Association (Tw) ...... 69 Wadworth Island Association NO ...... 70
Descriptions of Vegetation Communities : 76
Polar Desert Type ...... 76 Papaver-Draba Community (1 .1) ...... 76 Rhizocarpon-Umbellicaria Community (1 .2) ...... 76
Moss-Grass Vegetation Type ...... 76 Polyblastia-Poa Community (1 .3) ...... 76 Polyblastia-Cephaloziella Community (1 .4) ...... 77 Héirochloe-Pleuropogon Community (1 .5) ...... 77
Dwarf-Shrub Vegetation Type ...... 77 Saxifraga-Draba Community (2 .1) ...... 77 Saxifraga-Papaver Community (2 .2) ...... 79 Saxifraga-Dryas Community (2 .3) ...... 79 Saxifraga-Salix Community (2 .4) ...... 79 Salix-Dryas Community (2 .5) ...... 80 Salix Alopecurus Community (2 .6) ...... 80 Cetraria-Saxifraga Community (2 .7) ...... 80 Cetraria-Cassiope Community (2 .8) ...... 80 Salix-Dicranum Community (2 .9) ...... 81 Saxifraga-Polyblastia Community (2 .10) ...... 81
Sedge Meadow Vegetation Type ...... 82 Carex-Arctagrostis Community (3 .1) ...... 82 Carex-Drepanocladus Community (3 .2) ...... 82 ACKNOWLEDGEMENTS
Logistical support in the field was supplied by the Terrain Sciences
Division of the Geological Survey of Canada . J .A. John Netterville,
A .S . Dyke, R .D . Thomas, K .A . Drabinsky and J .J . Viellette provided invaluable assistance and stimulating discussions . The active interests and advice of S .C . Zoltai and C . Tarnocai were most appreciated .
J . Barlow and J . Griffiths prepared the maps and drawings . Miss . B . Stupak typed the manuscript . This study was funded by a grant from the Canada
Department of Agriculture .
CORRECTIONS
Page Line Error Correction
48 3 & 4 gneiss gruss 62 21 Permafrost Frost 72 22 Mathias Matthias 79 25 Table Table 29 80 24 fule rule 82 6 Arctagnostis Arctagnostis 100 20 stable unstable 124 13 contens contents 1 . INTRODUCTION
In Canada there are 2 .5 sq . km (900,000 sq . mi .) of land lying north of the tree line (Porsild, 1964) . Of these, 1 .42 million sq . km comprise the group of islands known as the Canadian Archipelago which span from Banks Is . in the west to Baffin Is . in the east . Somerset and Prince of Wales are adjacent islands occupying the centre of the Canadian Arctic
Islands (Figure 1) . Somerset Is . (72 ° 00' to 74° 10'N, 90° 00' to 96°00'W) les just north of Boothia Peninsula and is separated from the latter by the narrow Bellot Strait . Saville (1959) estimated the area of Somerset Is . at approximately 24,000 sq . km (9,450 sq . mi .) . The area of Prince of
Wales Is . (71°20' to 74 ° 05'N, 96 ° 10' to 102°50'W) is estimated to be
32,500 sq . km (12,700 sq . mi .) .
These islands lie in the path of a gas pipeline proposed for the
Canadian Arctic (Hindle, 1975) (Figure 2) . The history of gas discoveries in the region and the logistical problem of transporting gas to southern markets have been discussed to some detail by Rohmer (1973) . More than half of the 30 trillion cu . ft . of gas necessary to justify the pipeline has been found . Recently the important strike of oil on Cameron Island confirms the importance of the region as a reservoir of fossil fuels .
Concerns over the implications of energy development in the arctic have prompted the Canadian Government to sponsor social and environmental research of which the present study is one contribution .
2 . OBJECTIVES
The objectives of the present study are to provide reconnaissance information on the vegetation and soils of Somerset and Prince of Wales
Islands, and to point out areas which require special considerations
North west Terrjtrries
:...... ". . . .:: : ...... ".Y8°° ' ,
HUDSON
BAY
FIG . ( I ) STUDY AREA
LEGEND SCALE 1 240 MILES = I INCH
STUDY AREA
FIG. ( 2) PROPOSED AIftlC PIPELINE
LEGEND SCALE 1240 MILES " I INCH ® PIPELINE ALTERNATIVE ROUTES
in routing the proposed pipeline . This study will also review current
thoughts on pedogenesis in the Arctic and discuss their merits based on
field observations .
3 . STATE OF KNOWLEDGE
3 .1 Climate
Rae (1951) has dealt with the climate of the Canadian Arctic
Archipelago to some depth . Meteorological data were collected at Fort Ross
from 1938 to 1950 . On Somerset, most of the land mass is closer to Resolute
Bay than to Fort Ross ; thus, data from the former settlement may better
characterize the climate of Somerset . On the other hand, the climate of
Prince of Wales would be similar to that of Fort Ross, due to resemblence
in altitude and latitude .
According to Rae,in winter Somerset Is . marks the western limit of
cyclonic activities characteristic of the eastern Arctic Islands . Con-
sequently, winter temperatures are consistently low and mild spells in
mid-winter are infrequent . Temperature recordings at Resolute and Fort
Ross may be summarized as follows :
Table 1 Monthly and Annual Averages of Daily Mean Temperatures (° C)
Jan . Feb . Mar . Apr . May June July Aug . Sept . Oct . Nov . Dec . Year Range
Resolute -34 -36 -31 -25 -11 1 4 4 -5 -21 -22 -28 -17 41 Fort Ross -29 -32 -26 -22 - 9 0 4 2 -4 -12 -22 -26 -15 36
The highest diurnal fluctuation of temperature occurs in March .
Yet, on an annual basis temperatures only fluctuate over a mean of 36 ° C
which is a result of the maritime influence . Below-freezing temperatures
occur in all months of the year and July is the only month in which mean
daily minimum stays above freezing ; these are two factors which are
significant to vegetation survival . Most of the precipitation on Somerset is in the form of snow .
Rain falls only between May and September and the intensity is usually low .
Snow falls every month of the year, but the overall accumulated precipitation remains low . The Resolute Bay data may be summarized as follows :
Table 2 . Average Monthly and Annual Precipitation
Jan . Feb . Mar . Apr . May June .July Aug . Sept . Oct . Nov . Dec . Year Rainfall 0 .0 0 .0 0 .0 0 .0 9 .6 3 .0 18 .4 10 .0 T 0 .0 0 .0 68 .0 Resolute (mm) 0 .0 Snowfall (cm) 1 .8 3 .6 5 .1 3 .3 16 .5 7 .6 1 .3 7 .9 20 .0 14 .0 6 .9 2 .5 89 .0 Rainfall 0 .0 0 .0 0 .0 0 .0 2 .6 12 .5 21 .8 35 .0 0 .0 0 .0 0 .0 0 .0 69 .0 Fort Ross (mm) Snowfall (cm) 17 .0 7 .6 20 .0 8 .4 11 .2 13 .5 1 .0 1 .5 29 .2 31 .2 23 .0 8 .2 160 .0
The prevalent winter wind direction for the Central Arctic Islands is northerly to northwesterly . In summer the entire Arctic Archipelago is often situated in a fairly uniform high pressure system ; wind directions are thus influenced by local topography . Contrary to common belief, the mean annual wind speed is only 12 .2 mph which is comparable to southern stations . Rae (1951) attributed the feeling of windiness in the Arctic to the lack of tree cover .
3 .2 Geology
The rock formations of Somerset and Prince of Wales Is . are quite varied ; these include igneous, metamorphic and sedimentary rocks of two eras . These formations are presented in Figure 3 . Paleozoic limestones and sandstones cover the majority of the area on both Somerset and Prince of
Wales . Yet a series of tectonic upheavals have resulted in the Boothia
Uplift which is an elongate north-pointing extension of the Canadian Shield
(Kerr and Christie, 1965) . Bands of Paleozoic sedimentary rocks flanking
FIG.( 3 ) GEOLOGY OF SOMERSET IS Kilometres 20 40 60 Statute Miles0. 20 " 40 0 OUATERNARY ip 4 DrifI WZ {I5 Eureka Formation . : shale, siltstone and sandstones 0 KSILURIAN AND DEVONIAN 12 Peel Sound Formation: conglomerate sandstone and siltstone SILURIAN 13 Limestone, dolomite ; mainly carbonate, mixture of Peel Sound and 11 Read Bay Formation= limestone, limy dolomite, sholy dolomitic limestone, Read Bay Formations silty limestone CAMBRIAN AND ORDOVICIAN 0 Sandstone, sandy dolomite,dolomite, shay dolomite,intrafomational conglomerate 6 Hunting Formations dolomite, sandy dolomite ; minor shale, sandstone, siltstone, chart Aston Formations quartzite, minor shale, limestone, conglomerate Granitic Rocks Mofie and Felsic Gneiss
U ô rDUATERNARY 14 Drift z ,,, 15 Eureka Formation (7, ), shale, siltstone and sandstones v /SILURIAN AND DEVONIAN 12 Peel Sound Formations conglomerate sandstone and siltstone SILURIAN 13 Limestone, dolomite ; mainly carbonate, mixture of Peel Sound and Read Bay Formations 11 Read Boy Formations limestone, Ilmy dolomite, sholy dolomitic limestone, silty limestone CAMBRIAN AND ORDOVICIAN 10 Sandstone, sandy dolomite, dolomite, shay dolorMe,introfomational conglomerate 6 Hunting Formations dolomite, sandydolomite ; minor shale, sandstone, siltstone, chart Aston Formations quartzite, mina shale, limestone, conglomerate Granitic Rocks Mofic and Felsic Gneiss and pushed up by the Boothia Uplift are known as the Cornwallis foldbelts .
Blackadar (1967) reports that the older igneous rocks of Boothia-
Somerset are similar to many areas of the southern Canadian Shield in that they are dominated by mafic and felsic gniesses which are either banded or homogeneous . These rocks are variable in detail but uniform as a whole .
The rock types include quartz, feldspars, migmatite, pyroxene and biotite .
Occasional outcrops of granite do occur but it is uncertain whether their origins are igneous or metamorphic .
Christie (1967) states that the sedimentary rocks of Somerset and
Prince of Wales are Paleozoic and Proterozoic in age . These are mostly grey, greenish grey or brown limestones and sandstones . Tuke et al .
(1966) reports in northwestern Somerset Is ., Paleozoic quartz sandstones and dolostones are overlain by Ordovician strata which are fossiliferous ; ostracoderms occur in Silurian and Devonian layers of the limestones . It is worth mentioning that kimberlites have also been found in central Somerset
(Mitchell 1975) .
3 .3 Physiography
Blackadar (1967) stated the topography of Somerset and Prince of
Wales for the two islands is strongly influenced by the underlying bedrock .
A full description of the terrain regions of Somerset and Prince of Wales
Is . is being undertaken by Netterville, et al . (1976) . Blackadar
(1967) gave a more concise description composed of three main physiographic regions . These are described as follows :
Northern Somerset as a physiographic region is similar to Brodeur
Peninsula described by Frontier, et al . (1957) . This plateau occupies the eastern two-thirds of Somerset as well as northeastern Prince of Wales . The topography gently undulates between 300 m and 400 m a .s .l ., except for near coastal areas where it ends abruptly forming vertical sea cliffs . The plateau surface is covered with shattered rock fragments and solifluction
features are very common . The rivers have shallow broad valleys but near
the northeastern coast they are embedded in deep gorges .
The second region is the spine of the Precambrian crystalline rocks
extending for the most part along the coasts bordering Peel Sound . This
unit only occupies a limited area along the east coast of Prince of Wales .
On Somerset a 10 km wide strip along the west coast is characterized by
rounded hills and northeast-southwest trending lakes and rivers . However,
further inland and above 300 m a .s .l . northerly trending ridges and
felsenmeer are the dominant features .
Thé third physiographic region covers most of Prince of Wales Is .
except the northeast corner and parts of the east coast . Here, the
drift is continuous and the landscape is characterized by glacial landforms .
Craig (1963) reports on the locations of kames, eskers and moraines
on Prince of Wales .
Another study on the physiography of the study area and Boothia
Peninsula was conducted by the Geography Department of McGill University
under the sponsorship of Rand Corporation (Anonymous, 1963) . It covers
Somerset Is . and Boothia Peninsula but not Prince of Wales Is .
3 .4 Glacial History
The Quaternary geology of the study area is currently being investigated
by the staff of the Geological Survey of Canada . Due to the relevance of
this topic to soil classification, the current ideas on glacial events of the
study area are reviewed here . Prior to the summer of 1975, it was thought 10 that the entire study area was overridden by the Laurentide ice sheet
(Craig, 1963) . Netterville, et al . (1976) hold the view that much of the northern part of Somerset and perhaps northeast Prince of Wales did not experience a stage of glaciation that left prominent features in the southern part, even though the entire surface of both islands was ice-covered at an earlier date . In other words, the glaciation of southern Somerset and most of southern Prince of Wales around 10,000 yrs . B .P . left the northern portion untouched ; erratics found in the northern area can, therefore, be construed as remnants of an earlier Pleistocene episode . Evidence in support of this view lie in the occurrence in the northern area of for-like boulders ; accumulation of large amounts of weathering products rather than till ; and severe solutions features on limestones which were also confirmed by
Smith (1972) .
Another interpretation for a very similar type of landscape is advanced by Blake (1970) and Barnett et al . (1976) for Bathurst and Cornwallis Is .
It is known that during Wisconsin times the northern Queen Elizabeth Islands were covered by the Innutian Ice Sheet based on isostatic rebound measurements
(Blake, 1970 ; Andrew, 1970) . The Innutian Ice Sheet was a thick polar glacier that carried a very small amount of till and flowed by the internal plastic deformation of ice . The characteristics of this ice sheet, therefore, explains the lack of drift deposits and ice-scouring features on Cornwallis and Bathurst Is .
The surface Precambrian erratics found on these islands are believed to have originated from an earlier period when the Laurentide Ice Sheet carried Shield rocks in from the south . Thus far the southern limit of the Innutian Ice
Sheet has been placed on Lowther Is . in the Barrow-Strait (Blake, 1970) ; it is not believed to have landed on Somerset Is . Indications of ice-flow directions reported by Netterville, et al . (1976) seem to support this view. Thus,
74a-
CClarence
W u r
9~ After Netterviile et al 1976 LEGEND KilometresR 20 40 60 20 Generalized ice flow direction sense known - -" - Inferred axes of ice divergence Statute Mile Generalized ice flow direction sense unknown Marine shells -"""- Inferred axes of ice convergence Marine deposits
12
although landforms on Cornwallis Is . and northern Somerset Is . appear to be
very similar, they probably have evolved along different routes during
Holocene times . A map showing the directions of ice-movements during
Pleistocene is shown in Figure 5 .
3 .5 Soils
There has been very little work done on the soils of the Queen
Elizabeth Islands . Cruickshank (1971) mapped the soils and terrain units
around Resolute using a system of classification developed by Tedrow (1966) .
The latter visited Prince Patrick Is . and reported that the major soil type
there is the Polar Desert Soil . McMillan (1960) made some general obser-
vations of the soils of Queen Elizabeth Is . A mapping project has just been
concluded on Boothia Peninsula and preliminary results have been reported
(Tarnocai and Boydell, 1975) . Pawluk and Brewer (1975) studied the micro-
morphology of some soils of Devon and King Christian Islands .
3 .6 Vegetation
Savile (1959) made initial contributions to the botany of Somerset .
While few of the collection sites were too far from the coast, 90 vascular
species and 28 fungi were collected . Next to no published work has been
reported for Prince of Wales Is . Collections made in the 1975 summer
did not reveal too much qualitative difference between the vegetation of the
two islands . Savile (1959) described seven habitat types, some of which
13
represent community types which are quite dominant in the area . These are
limestone barrens (polar desert) characterized by Dryas integrifolia and
Saxifraga oppostifolia ; gravel tundra (polar semi-desert) characterized by
D . integrifolia and S . oppostifolia , and additional species of Draba,
Pedicularis and Salix . On river terraces of sand and gravel Alopecurus
alpinus , Cerastium beeringianum and Arenaria rubella can be found . The
sedge meadows are characterized by-- Eriôghôi-un~ -" tti6te ;-~ Càrex
misandra, C . membranacea, Arctagros tis latifolia, Dupontia Fisheri . On the
marine beaches and tidal flats Savile reports no characteristic flora, but
Cochlearia officinalis , Puccinella Bruggemannii and Stellaria humifusa occur
on the tidal flats and Cerastium Beeringianum , Arenaria rosii and A . rubella
inhabit above the storm line .
Savile (1959) also collected fungi on Somerset Is ., in particular the
parasitic species . He observed that the best sites for vascular plants are
also the richest sites for parasitic fungi . He also pointed out that the
parasitic behavior of fungi in the arctic places emphasized survival,
since pests which require long life cycles within single hosts take on
unnecessary risks .
Botanical studies in adjacent areas have been conducted by Thannheiser
(_1972) who provided a species list for Boothia Peninsula and King William
Schofield and Cody (1955) did a reconnaissance survey on Cornwallis Is .
Biological studies include the work of Brassard and Steere (1968) on
Bathurst Is ., Brassard (1967) on Melville Is . and Steere (1951)
on Cornwallis Is . Thomson (1971) reviewed the distribution of Arctic lichens
including the Central Arctic Islands . Savile (1961) also examined the phyto-
geography of the northwestern Queen Elizabeth Islands and its implication
on Pleistocene events . 14
Numerous articles have also been written on adaptation and survival of vegetation in the arctic ecosystem . Among these are the ones by Bliss
(1971), Bliss, et al . (1973), Polunin (1948) and Porsild (1951) .
3 .7 Wildlife
References to the abundance of wildlife on Somerset and Prince of
Wales Is . are extremely scarce . Tener (1963) has reported a game survey for the Queen Elizabeth Islands which is most likely out-dated . Based on observations in the 1975 summer, the study area is similar to other arctic islands in its animal species . Riewe (1972) summarized the mammals of
Devon Island in the following list :
short-tailed weasel (Mustela ermina) arctic fox (Alopex lagopus ) barren ground wolf (Canis lupus arctos )
The herbivorous mammals aret
arctic hare (Lepus arcticus montrabilis ) snowshoe hare (Lepus americanus ) Greenland collared lemming (Decrostonyx groelandicus ) Peary's caribou (Rangifer p~earyt) : barren gorund caribou (Rangifer tarandrus ) muskox (Ovibus moschatus)
Other microtines such as voles are no doubt present within the study area . Seals, beluga whales (Delphinaterus leucas ) and polar bears
(Ursus maritimus ) were also sighted during the 1975 season .
Reports on the birdlife have to be drawn from observations on neighbouring islands . Sutton (1971) sighted 26 species including greater snow goose (Chen hyperborea atlantica ), red-throated loon (Gavia stellata), rock ptarmigan (Lagopus mutus ), gyrfalcon (Falco rusticolus ) and peregrine
(Falco peregrine) . There are also three species each of gulls and jaegars .
15
Danks and Byers (1972) collected terrestrial arthropods on Bathurst Is .
and listed 78 species in total . There are 14 species of spiders (Arachnida),
13 mites (Acarina) and 61 insects (Insecta) of which 30 are choronomids .
On Somerset and Prince of Wales Is . the list of arthropods will likely be
longer as a great deal of the land area lies within the mid-arctic zone
where climate is more favorable (Downes, 1964) .
4 . METHODOLOGY
4 .1 Sampling
During the 1975 field season, Somerset and northern Prince of Wales Is .
were studied with the logistical support of the Terrain Sciences Division of
Geological Survey of Canada . The bulk of the data was collected during
helicopter traverses in which ground stops were selected subjectively
on air-photo mosaics . At each stop a pit was dug down to the top of the
frost table and the thickness of the active layer measured . Soil morphology,
drainage conditions and site descriptions of slope, patterned gxouAd=:type and
deposition mode were recorded . A sample of the soil parent material was
also collected for laboratory analyses .
Vegetation data were collected at each ground stop as well . In
vegetation sampling the conventional methods involving quadrats and transects
were not used after much consideration . It is well known that sampling
reliability is dependent on both the quadrat size used and the degree of
aggregation of individual plants (Kersaw, 1973 ; Poole, 1974) . While quadrats
and transects may work well in areas which have a fair vegetation cover, it
is difficult to find a fixed-dimension sampling unit that is appropriate
for vegetation cover ranging from 0 to 100 percent . Sampling theory demands
that the sampling unit correspondsto the natural rhythm of variation, which
16
in the present situation is the mean size of the patterned ground unit
(polygons, circles, nets or stripes) (Washburn 1958) . Thus, in places
where there were recognizable patterned ground the sampling unit was the
approximate mean size of the pattern ground unit itself ; this approach is
consistent with the use of the 'pedon'* as the basic sampling unit in the
study of cryoturbated soils . Where no obvious pattern could be detected,
a visually estimated 2 m-diameter circular quadrat was used .
The measure of abundance used for vegetation was the Domin
scale . * Despite its deficiences (Kersaw, 1973 ; Bannister, 1966) it is quite
satisfactory for a reconnaissance study in which the signal (mean estimates)
is as important as the noise (variance estimates) . In addition to overall
cover estimate the abundance of each species was also estimated by the Domin
scale . The distribution of species on various parts of a pattern ground
unit was also noted . A total of over 200 traverse sites were studied .
4 .2 Detailed Sites
A total of 23 detailed sites were studied in the field . These sites
were selected to exemplify various soil associations . At each site a pit
was dug to about 50 cm into the permafrost to expose a control section of
over one meter wide . The morphology of each horizon was then described and
bulk samples taken . Samplings were also taken for determination of water
and ice content . Soil temperate readings were taken at various levels in
the active layer .
* 'The pedon is a 3 dimensional unit of soil' . U .S . Soil Classification System, 7th Approximation . ** A modified Domin Scale is represented in Table 1, Appendix. FIG . (6 ) 20 40 Kilometres 60 20 JO A-SAMPLING LOCATIONS OF Statute Miles SOMERSETISLAND 7 ) OF LOCATIONSWALES ISLANDON Miles 40I
FIG.( Kilometres __L20 "-SAMPLING Statute PRINCE
1 9
4 .3 Laboratory Analytical Procedures
The calcite and dolomite content of the soil was determined
manometrically (Skinner, et al ., 1959) . The Walkley-Black wet oxidation
method with dichromate was used to determine the organic carbon content
(Greweling and Peech, 1965) . The total nitrogen content was obtained by the
modified marco-Kjeldahl method (Jackson, 1958) . The pH was determined
electrometrically in a soil-0 .01 M (1 :2) paste when the CaCl2 soluble salts were not determined (Peech, 1965), and in a saturated soil paste (U .S .
Salinity Lab . Staff, 1954) when the soluble salts were also determined .
The soluble salts were obtained by a conductivity method, using a saturation
extract (U .S . Salinity Lab . Staff, 1954), the Ca, Mg, - Na, and K with an
atomic absorption spectrophotometer, C1 was obtained photometrically
(Jackson, 1958), and SO4 by a turbidimetric method (Chesnin and Yien, 1951) .
The cation exchange capacity and exchangeable cations were measured in
leachates extracted by ammonium acetate, as outlined by Atkinson, et al .
(1958) . The leachate was analyzed for Ca, Mg, Na, and K by atomic absorption,
and H by NH40H titration (Atkinson, et al ., 1958) .
The stones were obtained by sieving the dry soil . For particle size
analysis the organic matter was removed with H202 and the soluble salts
were removed (Day, 1965) . Total sand was- separated and fractioned by wet
sieving . The silt and clay content was determined on some samples by the
Bouyoucos hydrometer sedimentation technique, and on other samples by the
pipet sampling method .
4 .4 Nomenclature and Identification of Vegetation
The nomenclature of vegetation follows that of Porsild (1964)
with the exception of Papaver radicatum which has been named P . lapponicum
20
(Tolm .) Nordh . ssp . occidentale (Lundstr .) by Kiger (1975) . The author
made the initial identifications on the vascular species which were sub-
sequently checked by G . Keleher of the University of Manitoba and Dr .
W .S . Cody of Canada Department of Agriculture . Dr . D .H . Vitt of the
University of Alberta identified the bryophytes and lichens .
5 . RESULTS
5 .1 System of Soil Classification
The classification of soils in the study area follows a system
adopted at the Ninth Meeting of the Canadian Soil Survey Committee
(Tarnocai, et al ., 1973) . Nearly all soils examined in the study area
belong to the Cryosolic Order, having a permafrost table within 1 m of
the surface* . The majority of the soils are in the Turbic Cryosol Great
Group, as they display horizon disruptions exceeding 1/3 of the control
section . Indications of cryoturbation are drawn from organic smears and
intrusions in the mineral layers ; frost sorting of materials of various
particle sizes, and the development of patterned ground on the surface .
A smaller proportion of soils belong to the Static Cryosol Great Group .
In these soils disrupted horizons constitute less than 1/3 of the control
section . Organo Cryosol soils do occur but their distribution is very
limited, their occurrence is discussed in Section 6 .
Three subgroups are encountered in the study area . The Regosolic
Subgroup lacks a B horizon and is, in fact, undifferentiated parent material .
The Brunisolic Subgroup has a Bm horizon more than 10 cm thick . This Bm
horizon is differentiated from the parent material in structure and/or * At the recent Tenth Meeting of the Canadian Soil Survey Committee, a permafrost table 2 m deep is adopted as the diagnostic horizon for the Cryosolic Order . 2 1
chroma . The Bm horizon either has a stronger chroma or it develops a granular structure with clay films surrounding the aggregates . Often on a silty parent material a layer with a vesicular structure can be found within 20 cm of the surface . This structure is probably related to the formation of small ice crystals during a slow freezing process . Chemical analyses show that this vesicular layer is often but not always different from underlying material in carbonate content . In this study, this layer is designated as Bmjy for it is considered to be an indication of cryo- genesis . Such soils are classified as Brunisolic Turbic Cryosols . These soils could probably be classified as Orthic Turbic Cryosol under the new system adopted at the recent Tenth Meeting of the Canadian Soil Survey
Committee . However, since the precise definitions of the Orthic Subgroup has yet to be released this study will follow the older classification system of 1973 .
Lastly, a significant amount of soils belong to the Gleysolic
Subgroup . These are soils of which the profile is dominated by gleization, as expressed by low chroma or distinct mottles in the control section .
About 80 percent of the Gleysolic Cryosol soils belong to the Turbic Great
Group ; Gleysolic Static Cryosol soils are rare . Two modifiers, Lithic and
Saline, are also used in conjunction with the Subgroups in accordance to the official vines .
5 .2 Use of Soils - vegetation Map
Soils-vegetation maps have been prepared for the study using N .T .S . maps at a scale of 1 :125,000 as base maps . These maps have been prepared with the aid of field observations and photo-interpretation of 1 :63,360
B & W air-photos, photo-mosaics at a scale of 1 :125,000 and LANDSAT B & W and color composite imagery . Each map unit represents a qualitative change
22
in soils and/or vegetation ; information is also given on general relief
changes, internal drainage conditions and overall vegetation cover* . The
method of symbolization is explained-in the legend of these maps .
The mapping unit for soils is at the association level . The criteria
for establishing soil associations are, in order of decreasing importance,
% CaCO3 equivalent,textural class and genetic origin of the parent material .
The de-emphasis on the last criterion is due in part to
the Pleistocene chronology of the study area not being fully clear
(Section 3 .4) . Until a satisfactory interpretation of the landscape can
be agreed upon, soil physical and chemical characteristics are considered
to be more reliable indicators for the recognition of associations . In
each map unit the parent material of the soil may be considered to be
generally uniform . On these parent materials a variety of soils may
develop which can be classified into the various subgroups of Cryosols
described earlier .
In this study the author feels it is not necessary to follow any
recognized system of vegetation classification as none of the hierarchical
approaches have proven to be satisfactory . However, for the purpose of
mapping, it is necessary to have groupings of some sort and a limited
amount of terminology for descriptions . The mapping unit is "community"
or "community type", a working definition which is that it is a
recognizable assemblage of mixed vegetation populations having similar
species composition . In a community type the species composition of
individual stands or populations may vary somewhat but there are always a
* Crustose lichens are exempted except in the case of Pôl,yblastia spp . Its ubiquitous occurrence makes it merit consideration .
23
few recurring species which are said to be "dominant" . A community type is,
therefore equivalent to the "association" or "subformation" level of
classification popularly used by European phytosociologists . A community
is named after its dominant species . Community types can also be grouped
into larger classed referred to as "vegetation types" here to minimize the
use of jargon . These are groupings which are roughly equivalent to
"formations" of European workers . In this study four vegetation types are
used ; these are polar desert, moss-grass, arctic dwarf shrubs and sedge
meadows . Their descriptions can be found in Section 5 .6 . Each map unit
contains the symbol for the community most common in the area . Where
complexes of community types occur, they are symbolized in the same way
soils complexes are .
According to conventions of biophysical mapping soils occurring in
different ecoregions (Section 5 .3) cannot carry identical association
names . This rule is only loosely enforced in this study as ecoregion
boundaries are broad zones of transition and it is unnecessary to follow
any delineation too rigidly . For the same reason, community types are
sometimes mapped as occurring somewhat outside the ecoregions they are
native to . In the southern end of Somerset Is . the adoption of soil
association names from northern Boothia Peninsula is justified on the basis
of the physiographic and ecological similarities between the two areas .
Descriptions of these associations can be found in Section 5 .5 .
5 .3 Ecological Regions
While examining the biophysical characteristics of a large area,
certain differences in plant distribution, frequency, or successional
patterns become evident on similar physiographic areas . Such differences
may be recognized as ecological regions (or zones) which may be defined
as land areas within which vegetation growth and pedogenic processes will
be similar on similar physiographic sites, being influenced by a uniform
regional climate (Zoltai and Pettapiece 1973 ; Tarnocai, 1973) . The terms
"ecological region", "ecoregion" and "ecological zone" are synonymous and are
equivalent to the "site region" of Hills (1960) and the "land region" of
Lacate (1969) .
On the basis of these criteria, the study area was divided into two
ecological regions, the High Arctic and the Mid-Arctic Ecological Regions .
This division is in general agreement with an earlier assessment by
Polunin (1951) who used the 75th parallel as a .- regional division of a much
broader scale . The differences between the regions is manifested both in
vegetation and in soil development . The vegetation differences on similar
soil moisture and material classes are manifested in greater ground cover
in the Mid-Arctic Region than in the High Arctic, although the composition
of the communites may be nearly identical . There is indication that some
southern species are more abundant or occur only in the Mid-Arctic Region .
The zonal soil in the High-Arctic Region in the study area is Regosolic
Turbic Cryosol, while in the Mid-Arctic Region Brunisolic Turbic Cryosol
is more common .
25
5 .4 Ecological Districts
Phypiographic differences within regions make it possible to
subdivide them into districts . These districts are equivalent to the
"site districts" of Hills (1960) and the "land districts" of Lacate (1969)
who defined them as subdivisions of land regions based primarily on the
separation of major physiographic and/or geologic patterns which characterize
the region as a whole . Thus, ecological districts are subdivisions of
ecological regions based on significant changes in the nature and relief
of surficial materials .
5 .41 Ecological Districts of Somerset Island (Figure 8)
HIGH ARCTIC ECOREGION
Ecodistrict Hla : Central Plateau
This is an area of great uniformity and it corresponds to terrain
regions 1 and 2 described by Netterville et al . (1976) . It covers the
entire northeastern plateau of Sommerset which gently undulates above
200 m a .s .l . except towards the east where deep canyons are cut into the
limestone and dolostone bedrock . The surface is covered by a mantle of
extremely calcareous loamy silt . Stone content is generally very high
but it varies with the depth to the bedrock (1 to 3 m) . While a very thin
layer of erratics is inevitably present, it is still indeterminate whether
till forms as significant a component of this mantle as weathered bedrock
does (Netterville, et al ., 1976 ; Bird, 1967) . The soil subgroups encountered
here are Brunisolic Turbic Cryosol, Regosolic Turbic Cryosol and Regosolic
Static Cryosol . On long, colluviated slopes Gleysolic Turbic Cryosol may
develop . The surface is usually patterned with circles, nets or stripes at
various degrees of sorting . Ice wedge polygons, on the other hand, are FIG.( 8) ECOLOGICAL DISTRICTS OF Kilometres 0 20 40 60 SOMERSET ISLAND 20 40 Statute Miles "
Ha8ib Northwest Plateau M 2 South Somerset Till Plain H 2 West Somerset Uplain M 3 South Somerset Ranges H 3 Cunningham Inlet M 4 Central Creswell Valley M 5 Creswell Lowland M I Cape Garry Plateau M 6 StonwelI-Fletcher Basin M T Harzord Inlet Beaches 2 7
quite rare in the area . The vegetation cover here is under 10 percent
except on some colluviated slopes . Species encountered include Saxifraga oppo sitifolia, Papaver lapponicum ssp . occidentale , Cerastium beeringianum ,
Drabâ Bellii and Dryas integrifolia .
Ecodistrict Hlb
This area is very similar to District Hla except for the evident marine influence . Consequently the parent material tends to have higher
silt and clay content and is not quite as stony as the rest of the district .
Drainage is often imperfect, and the occurrence of Brunisolic Turbic
Cryosol and Gleysolic Turbic Cryosol is more frequent, even though Rego-
solic Turbic Cryosol and Regosolic Static Cryosol remain the most common
subgroups . Owing to a more uniform texture and less stones, the amount of
frost sorting is less than that observed in District Hla . The vegetation is very similar to District Hla and the overall percentage cover is comparable .
Ecodistrict H2 : West Somerset Upland
This area includes Terrain Region 3 and a portion of 4 in the
physiographic zonation (Netterville, et al ., 1976) . The coastal area which is a strip 8 to 10 km wide, has a very thin and discontinuous layer
of coarse sand over Precambrian gneiss . The sand has originated from the bedrock even though scattered Paleozoic erratics are present . Frost
sorting is intense, and circles and nets, as well as felsenmeer, are common
surface forms . Lithic Regosolic Turbic Cryosol and Regosolic Turbic Cryosol
are most often encountered . In the valleys glaciofluvial and ice contact materials may be found but these deposits are not extensive . Towards the west coast glaciomarine influence has resulted in a thicker and more continuous 28
deposition of unconsolidated material which has developed into Brunisolic
Turbic Cryosol, Brunisolic Static Cryosol and Gleysolic Turbic Cryosol .
At such locations sedge meadows with a cover of 70 to 100 percent are found .
The important species are Carex spp ., Luzula spp ., Eriophorum triste and mosses . The surface forms that associate with sedge meadows are earth hummocks and ice wedge polygons .
East of the coastal strip the Precambrian upland has a more extensive cover of surficial material, consisting of a combination of till and weathered bedrock (Netterville, et al ., 1976) . The gently undulating landscape is marked by felsenmeer with scattered pockets of sandy silt, with erratics scattered on the surface . Tor-like features and bedrock outcrops with altiplanation terraces are very common . Patterned ground is so well developed that the sorting on circles, nets and stripes is nearly perfect . On the fine textured soils Regosolic Turbic Cryosol and
Lithic Regosolic Cryosol are found . The fine textured areas have a high water table perched on permafrost and horizontal internal drainage is quite dominant . On the wet surfaces black crusts formed by the association of
Polyblastia spp ., Blindia acuta and Cephaloziella sp . may cover up to
50 percent of the surface . The gneissic bedrock is barren except for crustose lichens and cushions of Andrae rupestris .
Ecodistrict H3 : Cunningham Inlet
This is a relatively small area in the High Arctic region . Much of the valley is filled with marine silts and clays over 1 metre in thick- ness . However, there are small outcrops of Tertiary sandstone of the
Eureka Sound Formation (Region 10, Netterville, et al ., 1976) . The dominant soils on marine deposits are stone-free Regosolic Static Cryosol and
29
occasionally Brunisolic Turbic Cryosol . Vegetation cover ranges between
0 to 30 percent ; Saxifraga oppositifolia , Salix arctica , Drabs. spp .,
Deschampsia spp . are frequent species .
On poorly drained sites of the valley eroding high centered peat
polygons, all of which have ceased accumulating peat, can be found . These
polygons are eroded actively by the drainage channels running among them.
The Glacic Mesic Organo Cryosol is about one meter thick with a frost . table at 30 cm . Oxyria digyna , Papaver lappdnüéum- -ssp ;._cceidejat ale, and A7.opecurus alpinus occur on the peat, and the surrounding area is dominated by Drepanocladus
spp ., Hierochloe app . and Arctagrostis latifolia .
MID-ARCTIC ECOREGION
Ecodistrict Ml : Cape Garry Plateau
South of Creswell Bay the Paleozoic upland is covered by an
extensive sheet of medium to coarse textured deposits of marine origin . A
similar deposit can be found north of the bay in the catchment area of the
East Creswell River . In both areas kames and ice contact deposits are much
in evidence, indicating the soil parent material is a mixture of marine and
glacial deposits . This material has weathered into Brunisolic Turbic
Cryosol and Gleysolic Turbic Cryosol and Regosolic Turbic Cryosol . Ice
wedge polygons are the most common form of pattern ground . A very distinctive
community of dwarf shrub containing Saxifraga oppositifolia and Polyblastia
spp . cover 30 to 50 percent of the surface of the marine deposits . Sedge
meadows having continuous cover occur on poorly drained Gleysolic soils ;
such areas, however, do not reach a sizable extent . Glaciofluvial deposits,
on the other hand, are locally extensive . They have less than 30 percent
plant cover of species such as Papaver lapponicum ssp . occidentale and
Deschampsia - .ssp .
30
Below 150 m a .s .l . fine to medium texture marine deposits are the
dominant parent material . The raised beach systems that are situated below
this elevation are well separated into ridges of extremely calcareous marine
gravel and sand . Between the ridges fine texture marine deposits are found .
Vegetation cover on the beach ridges is under 20 percent ; but depending on
the moisture regime, sedge meadows and dwarf shrub communities of Salix
arctica may cover up to 100 percent of the inter-beach areas .
Ecodistrict M2 : South Somerset Till Plain
The Precambrian bedrock south of Stanwell-Fletcher Lake is over-
lain by a strongly to extremely calcareous till that is medium to coarse
in texture . This is an area in which the surficial deposit is clearly
unrelated to the bedrock . This parent material often has very rheotropic
properties which makes it sensitive to stress and vibrations . Many of the
long, colluviated slopes are marked by sorted stripes but by far the most
distinctive type of patterned ground is the regularly rectangular ice wedge
polygons -(Fig . 16) . Some of these polygons are high centered with-non-sorted nets
developed on them . Brunisolic Turbic Cryosol , Brunisolic Static Cryosol
and Regosolic Turbic Cryosol soils are commonly found . Vegetation cover ranges
from 30 to 70 percent but may be as low as 5 percent if solifluction is
active locally .
The area west of Stanwell-Fletcher Lake has a much thinner till
cover and the unconsolidated material is coarse textured . In the valleys
facing the west coast ice contact and glaciofluvial materials occur
sporadically . Physical instability of the soil is not pronounced here,
and patterned ground is not well developed . Vegetation cover on well drained
sites is only 10 to 20 percent, consisting of Draba spp ., Papaver lapponicum 31
ssp . occidentale and graminoids . On the wet spots sedge meadows and dwarf shrub communities with Salix arctica are found .
Ecodistrict 143 : South Somerset Ranges
The area at the extreme south of Somerset Island is very similar
to the northern end of Boothia Peninsula in its physiography . This area has
rugged Precambrian ridges separated by narrow valleys . According to
Tarnocai and Boydell (1975) the northern tip of Boothia Peninsula is
covered by a layer of calcareous coarse textured till . This material extends across the Bellot Strait and thins out towards the west and the north . Brunisolic Turbic Cryosol and Regosolic Turbic Cryosol develop
on the extremely stony parent material which is very poorly sorted by frost .
Vegetation cover on unconsolidated material is 30 to 50 percent . The mesic
sites are occupied by ground cover of Cetraria spp and Saxifraga oppositi-
folia . Sedge meadows are found in poorly drained areas of valley floors
and lake edges .
Ecodistrict M4 : Central Creswell Valley
The headwaters of the Central Creswell River consist of a series
of low hills resulting from severe dissection by drainage channels . The
soil parent material is a silt loam to sand, the stone content of which is
dependent on the composition of the underlying Peel Sound Formation
(sandstone, siltstone and conglomerates) . Portions of this parent material
is undoubtedly till as shown by the presence of erratics . Regosolic Turbic
Cryosol , Lithic Regosolic Cryosol and Brunisolic Turbic Cryosol are
common, the last occurring more frequently here than in District Ml .
Patterned ground of all kinds can be found here but the forms are less
32
developed than in Districts M1 and M2 . Vegetation is more luxuriant than
in the High Arctic Ecoregion and vegetation cover in general is about
50 percent . Plant communities containing Saxifraga oppositifolia , Salix
arctica and Dryas int egrifolia are common .
Ecodistrict M5 : Creswell Lowland
The surficial deposits are dominated by marine silts and clays .
Below 150 m a .s .l . numerous relic beaches of sand and gravel rise about
one metre above the surrounding fine textured sediments . Much of the
fine textured material is poorly drained and Gleysolic Turbic Cryosol is
the most common soil . Brunisolic Turbic Cryosol and rarely Regosolic
Turbic Cryosol may be found on the beach ridges . There are also pockets
of Organo Cryosol which form prominent peat polygons . Patterned ground
such as earth hummocks and ice wedge polygons are common . A pattern
unrelated to frost sorting is found on fens where the water table is at the
surface . Vegetation is nearly continuous on the poorly and imperfectly
drained areas, including dwarf shrub communities of Saxifraga oppostifolia on
beach ridges and sedge meadows on the poorly drained areas .
Ecodistrict M6 : Stanwell-Fletcher Basin
The surficial deposits of Stanwell-Fletcher Basin are quite varied :
a large area is covered by a coarse textured till with occasional outcrops
of the Eureka Sound Sandstones . At lower elevations close to the lake
shore and at the south end of the lake fine texture marine deposits are
found . Kames were also found both north and east of the lake . On till
parent material small pockets of Mesic Organo Cryosol may occur, but the
dominant subgroups are the Brunisolic Turbic Cryosol and Gleysolic Turbic
Cryosol . Drilling has discovered ice-rich materials in this area 33
(Veillette, 1976) . Much of the area has a vegetation cover exceeding
70 percent and dwarf shrub communities containing Salix spp . are very
common .
The marine deposits north and south of the lake are very similar
to the materials in the lowland of Creswell Bay . This resemblence extends
to patterned ground types and vegetation . However, the littoral communities
that are found in limited areas of Creswell Bay are not found in the Stanwell-
Fletcher Basin .
The peninsula of Union River area is unique in that it consists
of unweathered gneissic outcrops scattered among marine modified till, the
latter becoming the parent material for Gleysolic Turbic Cryosol . Earth
hummocks and ice wedge polygons are the predominant types of patterned
ground . Species of Carex and Luzula from the base of sedge meadow communities which cover over 70 percent of the unconsolidated material . Where soil has
accumulated on outcrops the growth of Cassiope tetragona and foliose lichens
such as Cetraria spp ; is luxuriant .
Ecodistrict M7 : Hazard Inlet Beaches
This area is similar to Ecodistrict Ma of Boothia Peninsula
(Tarnocai and Boydell, 1975) . The area is dominated by raised beach systems which have developed on Paleozoic bedrock . The area is covered with an
extremely calcareous coarse textured till which may be discontinuous locally .
Regosolic Turbic Cryosols and Brunisolic Cryosols are the common soils
encountered . Vegetation cover on mesic sites ranges between 10 to 30
percent consisting mainly of Saxifraga oppositifolia and Salix arctica
dwarf shrub communities . Patches of sedge meadows are found on poorly
drained areas between beach ridges . FIG.( 9 ) ECOLOGICAL DISTRICTS OF Kilometres 20 4,0 6,0 PRINCE OF WALES ISLAND Statute Miles 2ti0 40
H I Cope Hardy Highlands M I East Prince of Wales Highlands H 2 North Central Uplands M 2 Cape Henry Kellett Uplands H 3 Drake Bay Uplands M 3 Central Prince of Wales Lowlands H 4 Mount Clarendon Lowlands M4 Mount Cowie Lowlands H 5 Back Bay Lowlands M 5 Fisher Lake Lowlands M6 Prescott Island Uplands
35
5 .42 Ecological Districts of Prince of Wales Island (Figure 9)
HIGH ARCTIC ECOREGION
Ecodistrict H1 : Cape Hardy Highlands
The sandstones, dolomites and conglomerates of the Peel Sound
Formation constitute 2/3 of the upland surfaces of this district, the rest
of the area contains an unnamed formation of similar rock types . The soil
materials were derived mainly from these bedrock sources, resulting in a
moderately calcareous loamy parent material, with varying amounts of stones .
High to moderate relief characterizes the area, but deposits of marine silt
and sand occur in local plains . Many bedrock scarps below 90 m a .s .l .
are festooned with marine beaches .
The dominant soils are Regosolic Turbic Cryosol soils with generally
well developed patterned terrain . At lower elevations some Brunisolic
Turbic Cryosols may be found . The vegetation cover is about 10 to 30
percent, consisting mainly of Salix arctica and Saxifraga oppositifolia .
At lower elevations a Salix-Alopecurus community can be found, with a ground
cover varying between 10 and 60 percent . On fine-grained marine sediments
the sedge meadows become continuous .
Ecodistrict H2 : North Central Uplands
The bedrock and parent material of this area is similar to that
of Ecodistrict H1 of Somerset Is . The relief of the district is moderate,
with local differences in elevation seldom exceeding 75 m. Local deposits
of marine sand and silt occur at lower elevations, as do elaborate raised
marine beach complexes .
The dominant soils are Regosolic Turbic Cryosol . Patterned ground,
especially stripes on gentle to moderate slopes, are common . Brunisolic
3 6
Turbic Cryosol occur at lower elevations, whilst Brunisolic Static
Cryosol may be found on some marine sands . Gleysolic Turbic Cryosol are
common on seepage slopes and on marine silts . The vegetation on well
drained areas consists of Salix and-Saxifr4ga communities, having about
10 to 30 percent ground cover . On many slopes communities of 8alix and
Polyblastia may form 50 to-100 percent ground cover . The wet marine
sediments support continuous sedge meadow vegetation . '
Ecodistrict H3 : Drake Bay Uplands
This area of low to moderate relief is underlain by horizontal beds
of carbonate bedrock and is covered by highly calcareous till and rubble .
The texture of this material is generally a silt loam . The area was
inundated by the sea in post-glacial times (Netterville, et al ., 1976),
as shown by numerous raised beaches . In this area no marine fine texture
deposits of any significant extent were found .
The dominant soil is Regosolic Turbic Cryosol, with well developed
frost-sorted micro features . The vegetation cover is usually very sparse,
generally less than 5 percent cover on well to imperfectly drained areas,
but up to 30 percent in poorly drained locations . Saxifraga oppositifolia ,
Papaver lapponicum ssp occi dentale , Salix arctica are-the main species on the
better drained areas, while mosses (B um cryophilum, Philonotis fontana,
Tomenthypnum nitens ) and lichens (Alectoria spp .) may form a 30 to 50
percent cover on poorly drained areas .
Ecodistrict H4 : Mount Clarendon Lowlands
This area is very similar to Ecodistrict H3 but it includes more
extensive marine sand and silt deposits . The till-like surface material is a
highly calcareous silt loam with various amounts of stones .
3 7
The soil and vegetation is similar to that of District H3 . The
medium textured marine deposits are usually poorly drained, with a Gleysolic
Static or Turbic Cryosol soil and a continuous sedge meadow vegetation . On
the coarser marine deposits Brunisolic Turbic Cryosol have developed .
The vegetation here covers about 10 to 30 percent of the surface, consisting
mainly of Salix arctica , grasses and ground lichens .
Ecodistrict H5 : Back Bay Lowlands
These areas are characterized by low relief (usually less than
20 m), consisting mainly of marine sands and silts . Some areas of water-
modified till may also occur . Raised gravelly areas are found at the
foot of the highlands and near the present seashore .
The fine texture marine sediments are usually poorly drained,
with a Gleysolic Turbic or Static Cryosol . The vegetation on the well
drained areas is dominated by Salix arctica and moss and lichen species .
Ground cover is 25 to 40 percent . On poorly drained areas Gleysolic Turbic
or Static Cryosol develop under a continuous Carex-Eriophorum meadow cover .
MID-ARCTIC ECOREGION
Ecodistrict Ml : East Prince of Wales Highlands
This area is underlain by bedrock of the Peel Sound Formation .
The surface materials were derived from the sandstones, dolomites and
conglomerates of this formation, resulting in a moderately calcareous
loamy parent soil material . High to moderate relief characterizes this
area, but some lowlands with marine silt and sand do occur . Raised
marine beaches are found near the base of many escarpments .
The dominant soils are Brunisolic Turbic Cryosol, with Gleysolic
Turbic Cryosol in poorly drained locations . The vegetation on the better
38
drained areas covers 50 to 80 percent of the surface, with Saxifraga
oppositifolia , Dr as integrifolia and Salix arctica as the common species .
In poorly drained locations grass - moss communities may form a nearly
complete cover .
Ecodistrict M2 : Cape Henry Kellett Uplands
This district is similar to Ecodistrict Ml but has only a moderate
relief . The dominant till material is moderately calcareous silt loam,
but local areas of marine silt and sand do occur . Stony and gravelly
raised beaches are also encountered .
The soils are mainly in the Brunisolic Turbic Cryosol subgroup, with
well developed frost sorted micro features . In poorly drained areas the
soil is Gleysolic Turbic Cryosol, with the permafrost table at about 80 cm .
The well drained areas support a 50 to 100 percent cover of Salix arctica ,
Dryas integrifolia , grasses and lichens . On the poorly drained areas
Carex - Drepanocladus communities :-may-form neariy," eomplete - cover'.
Ecodistrict M3 : Central Prince of Wales Lowlands
This area is underlain by flat-lying carbonate bedrock . The
surficial unconsolidated materials were derived chiefly from this material,
resulting in a highly calcareous silty loam . The relief is low to moderate,
with raised marine gravel beaches surrounding many upland areas .
The dominant soils are Brunisolic and Regosolic Turbic Cryosol soils
in about equal proportions . The vegetation cover is generally sparse
(5 to 25 percent cover), with Salix arctica , Dryas integrifolia and
Saxifraga oppositifolia as the dominant species . On poorly drained areas
Gleysolic Turbic or Static Cryosol-3s ,found ; with.-mosses and grasses forming
a sparse (20 to 30 percent) cover .
39
Ecodistrict M4 : Mount Cowie Lowlands
This region is underlain by flat-lying carbonate bedrock, but
was extensively modified during marine transgression . Large raised beach
complexes and extensive marine sand and silt accumulated in many broad
valleys . The till is a highly calcareous silt loam and has a generally
low to moderate relief .
The vegetation on the calcareous till consists of sparse (10 to 30
percent) Salix - Saxifraga communities growing on Regosolic or Brunisolic
Turbic Cryosol . Sandy parent materials generally result in Brunisolic
Turbic or Static Cryosol . The vegetation on the well drained sand is
mainly Salix - Dryas ."arid : on the poorly drained- si-it -sedge meadows
with nearly continuous cover occur .
Ecodistrict M5 : Fisher Lake Lowlands
These areas are characterized by low relief . The unconsolidated
materials are mainly marine medium to coarse texture deposits, but in some
areas, wave-washed till covers extensive areas . The area in the western
most part of the island is nearly completely covered by marine sand . In
this area poorly consolidated sandstones may provide the source of the sand .
On the poorly drained silts the dominant soils are Gleysolic
Static or Turbic Cryosol P with the permafrost table at 40 to 60 cm from
the surface . The vegetation cover is nearly complete, consisting of Carex -
Drepanocladus meadows . 'On the sands Brunisolic Static Cryosol Oevelopnent is common .
Many high-centered polygons were noted where the peat has nearly completely
been eroded or oxidized, exposing the much cryoturbated mineral surface .
The typical vegetation on well drained sands is dominated by Salix -
Dicranum -communities with a 30-to-50-percent cover .
40
Ecodistrict M6 : Prescott Island Uplands .
Much of the surface of this area is occupied by frost-cracked
Precambrian granitic bedrock . Some finer texture material occurs locally
in basins and valleys . The soils in this area are intensely soliflucted .
Typical subgroups are Brunisolic Turbic Cryosol with some Gleysolic Turbic
Cryosol . The vegetation on broken rock surfaces is mainly crustose
lichen . Fruticose lichen such as Cetraria cucullata , C . nivalis , Alectoria
ochroleuca occur locally . On poorly drained soils mosses and grasses
-may form 'a 30-t6 -50 percent' cover . ' -
A summary of the characteristics of ecodistricts in the study area
is presented in Tables 3 and 4 . 41
Table 3 . Characteristics of Ecological Districts on Somerset Island
Ecoregion Ecological District Soil Subgroup Vegetation Type % (% area) (% area) Ground Cover
High Arctic Hla & Hlb Reg . T . Cryosol 80 Polar desert 80 1 Central Plateau Brun . T . Cryosol 10 Dwarf shrubs 10 10 Gley . T . Cryosol 10 Moss-grass 10 50
High Arctic H2 Reg . T . Cryosol 30 Polar desert 20 10 West Somerset Lith . R .T . Cryo . 30 Lichens 30 70 Upland Brun . T . Cryosol 30 Dwarf shrubs 30 25 Gley . T. Cryosol 10 Sedge meadows 20 90
High Arctic M3 Reg . T . Cryosol 50 Polar desert 30 10 Cunningham Inlet Brun . T . Cryosol 20 Dwarf shrubs 40 30 Gley . T . Cryosol 30 Sedge meadows 30 100
Mid=Arctic Ml Brun . T . Cryosol 50 Dwarf shrubs 50 30 Cape Garry Plateau Reg . T . Cryosol 40 Polar desert 50 10 Gley . T . Cryosol 10 Sedge meadows 10 100
Mid-Arctic M2 Brun . T . Cryosol 30 Dwarf shrubs 50 50 South Somerset Till Lith . R .T . Cryo . 20 Lichen 20 75 Plain Rego . T . Cryosol 30 Polar desert 20 50 Gley . T . Cryosol 20 Moss-grass 20 60
Mid-Arctic M3 Brun . T . Cryosol 40 Dwarf shrubs 40 40 South Somerset Rego . T . Cryosol 40 Polar desert 40 10 Ranges Gley . T . Cryosol 20 Meadow 20 100
Mid-Arctic M4 Brun . T . Cryosol 50 Dwarf shrubs 80 50 Central Creswell Rego . T . Cryosol 30 Valley Lith . R .T . Cryo . 10 Lichen 10 30 Gley . T . Cryosol 10 Sedge meadows 10 100
Mid-Arctic M5 Gley . T . Cryosol 60 Sedge meadows 60 100 Creswell Lowland Brun . T . Cryosol 30 Dwarf shrubs 40 45 Rego . T . Cryosol 10
Mid-Arctic M6 Brun . T . Cryosol 60 Dwarf shrubs 70 70 Stanwell-Fletcher Gley . T . Cryosol 30 Sedge meadows 30 100 Basin Rego . T . Cryosol 10
Mid-Arctic M7 Brun . T . Cryosol 40 Dwarf shrubs 70 30 Hazard Inlet Rego . T . Cryosol 40 Beaches Gley . T . Cryosol 20 Sedge meadows 30 100 42
Table 4 . Characteristics of Ecological Districts on Prince of Wales Island
Ecoregion Ecological District Soil Subgroup Vegetation Type % (% area) (% area) Ground Cover
High Arctic Hl Rego.T . Cryosol 50 Polar desert 70 10 Cape Hardy High- Brun . T . Cryosol 20 Dwarf shrubs 20 30 lands Gley . T . Cryosol 10 Moss-grass 10 75
High Arctic H2 Rego . T . Cryosol 60 Polar desert 60 10 North Central Brun . T . Cryosol 20 Dwarf shrubs 10 30 Uplands Gley . T . Cryosol 20 Moss-grass 30 80
High Arctic H3 Rego . T . Cryosol 80 Polar desert 80 1 Drake Bay Uplands Brun . T . Cryosol 10 Dwarf shrubs 10 30 Gley . T . Cryosol 10 Moss-grass 10 80
High Arctic H4 Rego . T . Cryosol 60 Polar desert 60 1 Mount Clarendon Brun . T . Cryosol 20 Dwarf shrubs 20 30 Lowlands Gley . T . Cryosol 20 Sedge meadows 20 100
High Arctic H5 Gley . T . Cryosol 60 Sedge meadows 60 100 Back Bay Lowlands Brun . T . Cryosol 40 Dwarf shrubs 40 30
Mid-Arctic Ml Brun . T . Cryosol 60 Dwarf shrubs 60 50 East Prince of Wales Rego . T . Cryosol 20 Polar desert 20 15 Highlands Gley . T . Cryosol 20 Sedge meadows 20 100
Mid-Arctic M2 Brun . T . Cryosol 70 Dwarf shrubs 80 60 Cape Henry Kellett Gley . T . Cryosol 30 Sedge meadows 20 100 Uplands
Mid-Arctic M3 Rego . T . Cryosol 60 Dwarf shrubs 60 5 Central Prince of Brun . T . Cryosol 20 Dwarf shrubs 20 30 Wales Lowlands Gley . T . Cryosol 20 Moss-grass 20 50
Mid-Arctic M4 Rego . T . Cryosol 40 Dwarf shrubs 40 15 Mount Cowie Low- Brun . T . Cryosol 40 Dwarf shrubs 40 30 lands Gley . T . Cryosol 20 Sedge meadows 20 100
Mid-Arctic M5 Brun . T . Cryosol 60 Dwarf shrubs 60 40 Marine Lowlands Gley . T . Cryosol 40 Sedge meadows 40 100
Mid-Arctic M6 Brun . T . Cryosol 40 Dwarf shrubs 40 60 Prescott Island Lith . R.T . Cryo . 4 0 Lichen 40 50 Uplands Gley . T . Cryosol 20 Sedge meadows 20 100 4 3 5 .5 Soil Associations of Somerset and Prince of Wales Islands
Aston Association
The Aston Association comprisessoils of Regosolic Turbic Cryosol
and Regosolic Static Cryosol of the alluvial terraces in High Arctic areas
of sedimentary bedrock . On broad valley floors where patches of poorly
drained areas are found Gleysolic Turbic Cryosol soils may develop .
Brunisolic Turbic Cryosol soils are not extensive and are limited to the
trenches of ice wedge polygons or the borders of river terrace . The parent material is stratified sand, gravel and silt . Precambrian erratics
of all kinds can be found in abundance . As a whole internal drainage is
good and the active layer is 50 to 60 cm thick . However, near delta areas marine silt and fine sand dominate the parent material and the drainage
conditions are poor . Under such conditions Regosolic Static Cryosol soils
are most common . The river terraces in the interior of Somerset Is . has
10 percent vegetation cover or less but near the coasts plant cover may be as high as 30 to 40 percent composing species such as Saxifraga oppositifolia ,
Dryas integrifolia and Pedicularis spp . The sedge-moss meadows on poorly drained locations occupy only small areas and are seldom fully developed .
Deltas on the seashore are poorly vegetated and have only scattered individuals of Poa spp . and Papaver lapponicum ssp . occidentale .
Batty Bay Association
The Batty Bay Association is comprised of soils of Regosolic Static
Cryosol, Regosolic Turbic Cryosol, Saline Regosolic Static Cryosol and
Brunisolic Static Cryosol developing on marine silts and clays of central and eastern Somerset Island . In contrast to the Garnier Bay Association these soils occur at elevations higher than 150 m a .s .l . The marine sediment is also thicker and more continuous . Internal drainage is imperfect
44
to well drained . While gravel may form a desert pavement on the surface
the active layer is less stony than other areas of the region . The relief
is similar to that of the Garnier Bay Association, namely gently undulating
with scattered small lakes . A Regosolic Static Cryosol developing on thick
marine deposit is described as follows :
Site : W37 Location : 73 ° 08'N 91° 30'W
Cy - 0 to 49 cm, light yellowish brown (l0YR 6/2 dry) silty clay, platy,
plastic, firm when moist, hard when dry ; clear, smooth boundary .
Cz - 49 cm plus, light yellowish brown (l0YR 6/2) frozen silty clay,
well-bonded randomly oriented ice .
The chemical and physical properties of this soil are presented
in Table 2 in the Appendix . The active layer is 40 to 50 cm thick .
Vegetation cover is under 10 percent and includes mainly Draba spp .,
Papaver lapponicum asp . occidentale , and Cerastium alpinum.
Baring Channel Association
The Baring Channel Association is comprised of Regosolic Static
Cryosol and Regosolic Turbic Cryosol soils developing on gravelly marine
beaches . The beach material originated dominantly from calcareous sandstone
or conglomerate . The material is extremely calcareous, being high in
calcite, but low in dolomite . Ice wedge polygons are frequent . Regosolic
Turbic Cryosol soils usually occur under and near the polygon trenches .
The active layer is about 80 to 100 cm thick in early August . Clear ice
occurs under the polygon trenches, but little visible ice is encountered
elsewhere . The vegetation cover is sparse and is mainly confined to the
polygon trenches where mosses, lichens and grasses grow in scattered clumps .
Gravel and boulders may be covered by crustose lichens .
4 5
Birmingham Bay Association
The Birmingham Bay Association resides along the length of the
Precambrian Uplands of northern Somerset Is . It includes soils of Regosolic
Turbic Cryosol, Lithic Regosolic Turbic Cryosol and Brunisolic Turbic
Cryosol forming on the weathering product of Precambrian bedrock . The
parent material is medium to coarse texture and noncalcareous . A small
fraction of this material must have originated from till as gravel-sized
erratics are found on the surface . This layer which is about 1 to 2 m
thick overlies another till layer, which is weakly calcareous . The topo-
graphy is dominated by felsenmeer and tors ; otherwise the surface is very
gently sloping and undulating . An example of a Regosolic Turbic Cryosol
is given below :
Site : W75R Location : 72° 51' 92° 33'
Cy - 0 to 50 cm, dark yellowish brown (l0YR 4/3 moist) sandy loam, single
grained, slightly plastic, firm when moist, hard when dry ; clear,
abrupt boundary .
ICz - 50 to 75 cm, dark yellowish brown (l0YR 4/2) sandy loam, well-bonded
randomly oriented ice ; clear, abrupt boundary .
HC1z- 75 to 105 cm, dark olive (5Y 3/2) sandy loam ; clear, abrupt boundary .
HC2z- 105 to 118 cm plus, olive (5Y 4/2) sandy loam .
Table 3 in the Appendix shows the chemical and physical changes in the parent material . The internal drainage of this material is characterized by horizontal
movement and conditions are imperfect to poor . The active layer is 40
to 50 cm in thickness . Vegetation is very scarce except on the fines where
communities of Polyblastia spp . and Blindia spp . (Figure 7 ) form 50 to 70
percent cover locally . More often a scattered distribution of Poa abbreviata
and Polytrichum s trictum account for much of the natural vegetation .
46
The bedrock surfaces are quite heavily encrusted with crustose
lichens and Andaeae rupestris .
Cape Garry Association
Cape Garry Association is the collection of Brunisolic
Turbic Cryosol, Gleysolic Turbic Cryosol and Regosolic Static Cryosol soils
that develop on the alluvium of the Creswell Basin . As the river systems
here cut through deposits having widely different genetic origins the
properties of the alluvium are quite varied . Nevertheless, the parent
material usually consists of stratified sand, silt and gravel ; their
relative proportions depend on whether the original deposit is marine
sediment or till . Relief changes in this association are gently sloping
to level . Descriptions are given here on a Regosolic Turbic Cryosol
derived from the alluvial deposit of a till .
Site : W119B Location : 72 ° 54'N 93 ° 29'W
C ly- 0 to 15 cm, strong brown (7 .5YR 5/4 moist) loam, much organic intrusions,
massive,plastic,firm when moist, hard when dry ; clear, abrupt
boundary .
C 2y- 15 to 51 cm, yellowish brown (l0YR 5/2 moist) loam, massive, -plastic,
firm when moist, hard when dry ; clear, abrupt boundary .
Cz - 51 cm plus, yellowish brown (l0YR 5/2) loam, well-bonded randomly
oriented ice .
Table 4 in the Appendix shows the physical and chemical properties
of the parent material .
The active layer on well drained or imperfectly drained sites is
50 to 60 cm thick . On poorly drained gleyed soils it is 30 to 40 cm thick . 4 7
Continuous sedge meadows can be found on the older terraces ; however, on the newly deposited sand bars there are only pioneer individuals of Heirochloe spp . and Arc tagrostis lat ifolia .
Cape Hardy Association
This Association comprises frost shattered calcareous sandstone, conglomerate or mudstone bedrock materials . The material is generally extremely calcareous and is high in calcite, but low in dolomite . Frost action is manifested in crudely developed ice wedge polygons . The vegetation is very sparse, except for crustose lichens growing on boulders .
Rhizocarpon geogr aphicum, Lecidea spp . are common .
4 8
Cape Granite Association
The Cape Granite Association is derived from severely weathered
granite on Somerset Is . A layer of very poorly consolidated material occurs
on granite bedrock forming what is known as gneiss . On marine beaches,
however, the gneiss is wave-washed and completely unconsolidated . Its
grain size ranges from 2 mm to 5 mm . This deposit forms the parent material
of soils of Brunisolic Turbic Cryosol, Lithic Regosolic Static Cryosol,
Regosolic Turbic Cryosol and Gleysolic Turbic Cryosol . The topography is
gently sloping, interrupted only by bedrock outcrops . A Gleysolic Turbic
Cryosol soil developing on a marine beach is described as follows :
Site : W77A Location : 73° 40'N 95° 30'W
Cy - 0 to 52 cm, olive brown (2 .5Y 4/4 moist) sandy loam, single grained,
plastic, friable when moist, hard when dry, many organic smears and
intrusions ; clear, smooth boundary .
Cgy - 52 to 64 cm, olive brown (2 .5Y 4/2 moist) sandy loam, abundant
distinct mottles, single grained, plastic, friable when moist, hard
when dry ; clear, smooth boundary .
CZ - 64 cm plus, (2 .5Y 4/4) sandy loam, poorly bonded randomly oriented
ice .
Table 5 in the Appendix gives the physical and chemical character-
istics of the parent material .
Drainage conditions vary from well drained to imperfect . The
active layer is 50 to 60 cm thick . Vegetation on the Brunisolic and
Gleysolic Cryosol cover 50 to 80 percent of the surface ; the community
types are usually Carex meadows or the Cetraria-Saxifraga Community .
On Regosolic Cryosol soils vegetation cover is 10 to 30 percent, the typical
4 9
species include Cassiope tetragona , Dryas integrifolia and crustose lichens
such as Lecidea Dicksoni .
Creswell Association
The Creswell Association includes soils of Brunisolic Turbic Cryosol
and Regosolic Turbic Cryosol developing on marine coarse and medium texture
sediments in the Mid Arctic Ecoregion . This association usually occurs
together with the marine fine texture deposits of the Fury Association in
beach ridge systems or in abandoned marine terraces . Generally there is
low to moderate change in relief . An example profile of a Brunisolic
Turbic Cryosol associating with an ice wedge polygon is described as follows :
Site : W23 Location : 72° 47'N 92° 58'W
Ahy - 0 to 15 cm, discontinuous, dark yellowish brown (l0YR 3/4 moist)
silt loam, single grained, plastic, friable when moist, slightly
hard when dry ; clear, abrupt boundary .
Bmy - 0 to 35 cm, discontinuous, dark yellowish brown (l0YR 4/2 moist)
silt loam, granular, plastic, firm when moist, hard when dry,
organic inclusions present ; clear, abrupt boundary .
Omy - 10 to 25 cm, discontinuous, dark yellowish brown (l0YR 2/2 moist)
moderately decomposed grasses and mosses .
Cy - 0 to 35 cm, yellowish brown (l0YR 5/2 moist) silt loam, massive,
plastic, firm when moist, hard when dry ; clear, smooth boundary .
Cz - 35 cm plus, yellowish brown (l0YR 5/2) silt loam, well-bonded
randomly oriented ice .
The laboratory analyses of the parent material is presented in
Table 6 of the Appendix . The soils of this association are imperfect to
well drained, with an active layer ranging from 40 to 70 cm in thickness .
50
Vegetation covers 30 percent to 50 percent of the surface . The typical
species are Saxifraga oppositifolia , Dryas integrifolia and Polygonum
viviparum.
Elwin River Association
The Elwin River Association is only found in northeastern Somerset .
The main subgroup in this association is Brunisolic Turbic Cryosol,
Regosolic Static Cryosol and Regosolic Turbic Cryosol soils . The parent
material of this association is strongly to very strongly calcareous material
of high silt content . This association can be distinguished from the Howe
Harbour Association by a lower dolomite content in the former case .
Stones, including erratics, are plentiful on the surface . The parent material
is derived mostly from the underlying bedrock with some addition of till .
Topography is moderately sloping and gently rolling . The morphological
descriptions of a Brunisolic Turbic Cryosol is given as follows :
Site : W32 Location : 73° 23'N 92° 55'W
Bmjy- 0 to 22 cm, dark yellowish brown (l0YR 4/3 moist) loam, vesicular
structure, plastic, friable when moist, firm when dry ; clear,
smooth boundary .
Cy - 22 to 37 cm, dark yellowish brown (l0YR 4/3 moist) loam, single grained,
plastic, friable when moist, firm when dry ; clear, smooth boundary .
Cz - 37 cm plus, dark yellowish brown (l0YR 4/3) loam, well-bonded
randomly oriented ice .
The active layer thickness of these soils is between 40 to 50 cm .
Drainage conditions vary from imperfect to well drained . Vegetation cover
is between 50 to 70 cm and consists mostly of Polyblastia ssp ., Draba spp .
and grasses . Laboratory analyses of the active layer profile is presented
in Table 7 in the Appendix .
Fearnall Bay Association
The Fearnall Bay Association includes soils of Brunisolic Turbic
Cryosol and Regosolic Turbic Cryosol in Ecodistrict M1 of Somerset Is .
The parent material of this association is an extremely calcareous marine
modified till which is loam to sandy loam in texture . The evidence of marine
influence lies in the abundance of marine shells and low stone content in the
active layer . This deposit forms a fairly continuous layer at an elevation
above 150 m a .s .l . The topography is gently rolling and undulating . An
example profile of a Brunisolic Turbic Cryosol developing in an ice-wedged
polygon is given below :
Site : W73 Location : 72° 51'N 92° 33'W
Bmjy - 0 to 12 cm, dark yellowish brown (l0YR 4/3 moist) loam, vesicular,
plastic, firm when moist, hard when dry ; gradual, smooth boundary .
Cy - 12 to 55 cm, dark yellowish brown (l0YR 4/.3 moist) loam, massive,
plastic, firm when moist, hard when dry ; abrupt, smooth boundary .
Cz - 55 cm plus, dark yellowish brown (l0YR 4/3 moist) loam, well-bonded
randomly oriented ice .
The laboratory analyses of the unfrozen layers are presented in
Table 8 in the Appendix .
The internal drainage of this association is imperfect to well
drained . The active layer thickness is between 50 to 70 cm . Vegetation
on these soils is characterized by the very distinctive Saxifraga-Polyblastia
Community . The occurrence of this community type is generally an indication
of low calcium carbonate content in the substrate . The total percent cover
is in the 70 to 80 percent range . Dwarf shrub communities of Salix spp .,
particularly along ice-wedged polygon trenches, account for much of the
remaining vegetation .
52
Fiona Lake Association
The Fiona Lake Association includes soils of Brunisolic Turbic
Cryosol and Regosolic Turbic Cryosol soils in the Precambrian areas of the
High Arctic . The parent material of this association is a moderately
to strongly, calcareous till which in most areas is under 2 m thick . This
till layer is quite extensive and Gleysolic Turbic Cryosol soils do develop
in areas of poor local drainage, e .g . valley floors or lake edges . The
texture of the parent material is a very stony sandy loam . The relief is undulating
to hilly with frequent outcrops of Precambrian gneiss and schists . A Brunisolic
Turbic Cryosol on very thin till is described below . Note the change from
a noncalcareous ICy horizon to a strongly calcareous ICy horizon
(Table 9 in the Appendix) .
Site : W60 Location : 73° 32'N 95° 24'W
Ahy - 0 to 9 cm, discontinuous, dark yellowish brown (l0YR 3/2 moist)
loam, single grained, slightly plastic, friable when moist, loose
when dry ; clear, abrupt boundary .
Bmy - 9 to 19 cm, discontinuous, dark yellowish brown (l0YR 4/2 moist)
sandy loam, single grained, plastic, firm when moist, firm when dry ;
clear, smooth boundary .
ICY - 19 to 83 cm, dark yellowish brown (l0YR 3/3 moist) sandy loam,
single grained, plastic, firm when moist, firm when dry ; clear,
abrupt boundary .
IICY - 83 to 89 cm, olive brown (2 .5Y 4/4 moist) sandy loam, plastic,
firm when moist, firm when dry ; clear, abrupt boundary .
IICy3- 89 cm plus, olive brown (2 .5Y 4/4) sandy loam, well-bonded ice
veinlets and crystals .
5 3
On Brunisolic Cryosol and Regosolic Cryosol the active layer
ranges from 60 to 90 cm thick depending on local drainage conditions which
are well to imperfectly drained . On the heavily vegetated Gleysolic Turbic
Cryosol soils the active layer is shallower . In most areas vegetation cover
is 30 to 50 percent consisting of Saxifraga oppositifolia , Cetraria spp .,
and Pedicularis spp . Where there is a better supply of moisture Salix
arctica , Luzula confusa , Saxifraga cernus and Alopecurus alpinus may cover
up to 70 percent of the surface .
Fitz Roy Association
The Fitz Roy Association refers to Brunisolic Turbic Cryosol,
Regosolic Turbic Cryosol soils and a small amount of local Gleysolic Turbic
Cryosol soils . The parent material of this association is a medium to
coarse texture very strongly to extremely calcareous till overlying
Precambrian bedrock . This deposit covers most of the Precambrian areas
south of Stanwell Fletcher Lake on Somerset and varies in thickness from
1 to 5 m . The relief is moderately sloping and undulating . Much of the
area is covered with very regular ice wedge polygons, many of which have
developed active thaw flow-slides . Rheotropism is also common on many of
the colluviated slopes . Such a Regosolic Turbic Cryosol is described below :
Site : W117 Location : 72° 38'N 95° 02'
Cy - 0 to 70 cm, light olive brown (2 .5Y 5/4 moist) loam, massive,
plastic, firm when moist, hard when dry ; clear, abrupt boundary .
Cz - 70 cm plus, light olive brown (2 .5Y 5/4 moist) loam, well-bonded
randomly oriented ice .
Laboratory analyses of the parent material is presented in Table 10
in the Appendix . 54
The active layer in this association is between 60 to 70 cm thick .
Internal conditions range from well-drained to poor, but imperfect drainage is the most common case . Vegetation cover ranges from 30 to 70 percent in most areas . Continuous sedge meadows only occur on poorly drained valley floors and lake borders . However, on the most active solifluction slopes plant cover is only about 5 percent . -The recurring-species in the typical locations are Saxifragaa oppositifolia , Stereocaulon spp ., Cetraria cucullata, waver lapponicum ssp . occidentale , Blindia spp . and Polyblastia spp .
Four Rivers Association
The Four Rivers Association is the group of soils of which the parent material is the weakly to moderately calcareous glacial-fluvial and ice- contact coarse texture deposits on Precambrian bedrock . The soils found in this association belong to subgroups of Brunisolic Turbic Cryosol and Regosolic Turbic Cryosol . Regosolic Static Cryosol may also be found in relic deltas and terraces . The topography of these areas are dominated by steep small hills and ridges with intervening ravines . A Brunisolic
Turbic Cryosol soil at the foot of an esker is described as follows :
Site : W52A Location : 73° 20'N 95° 30'W
Ahy - 0 to 7 cm, dark yellowish brown (l0YR 2/2 moist) sandy loam, single-
grained, slightyly plastic, friable when moist, loose when dry ;
clear, abrupt boundary .
Bmy 7 to 34 cm, light olive brown (2 .5YR 5/4 moist) sandy loam, vesicular,
slightly plastic, firm when moist, firm when dry ; gradual, broken
boundary .
Cgy 34 to 55 cm, light olive brown (2 .5YR 5/4 moist) sandy loam, massive,
slightly plastic, firm when moist, hard when dry, distinct mottles ;
clear, abrupt boundary .
55
Cz - 55 cm plus, light olive brown (2 .5YR 5/4) sandy loam, well-bonded
ice inclusions .
Table 11 in the Appendix gives the physical and chemical properties
of this soil .
The active layer thickness of this association is 50 to 60 cm .
Drainage is well to imperfect . Vegetation cover ranges from 30 to 70
percent and includes species such as Dryas integrifolia , Cassiope tetragona ,
Luzula confusa and Polygonum viviparum.
Fury Association
The Fury Association refers to the Gleysolic Turbic Cryosols and
Brunisolic Turbic Cryosols of Creswell and Stanwell Fletcher Basin . The
parent material of these soils originated from calcareous marine silts and
clays deposited in the area . Soils of the Fury Association form complexes
with the Stanwell Fletcher till or the Fearnall Bay till in Ecodistricts
Ml and 236 on Somerset Is . Such occurrences are most common when the marine
deposits are thin and discontinuous . The relief change is low and the
topography is gently sloping and undulating . Drainage is imperfect to
poor . The active layer is between 20 to 40 cm thick in Gleysolic Turbic
Cryosol soils and 40 to 50 cm thick in Brunisolic Turbic Cryosol soils .
Except on tidal lacustrine flats, vegetation cover is as high as 70 to 100
percent . Sedge meadows and communities of Salix arctica and Dryas integrifolia
are most common .
Garnier Bay Association
The Garnier Bay Association includes soils of Gleysolic Turbic Cryosol,
Brunisolic Turbic Cryosol, Regosolic Turbic Cryosol and Saline Regosolic
Static Cryosol soils developed on marine fine texture deposits in the High
5 6
the frost Figure 10 . Brunisoiic Turbic Cryosol on marine silt . The top of table is shown in the lower left corner .
~r B9y Omy i
O- ~- 1 C ~ yZ Frost Table ~. Omyz 3340t40yrs(BG-S- 3J -----Permafrost
525180yrs C2yz (BGS - 330) W'Z2 samples . Figure 11 . Profile and 14C age determinations of
5 7
Arctic zone of Somerset Is . The layer of marine sediment is 1 to 2 m thick
and is often mixed in with the parent material of the Scarpbrook Association
through cryoturbation . The topography in these marine modified areas is gently
sloping and undulating, with a large scattering of small lakes 5 to 10
hectares in size . This association is seldom found above an elevation of
150 m a .s .l . Earch hummocks are the characteristic patterned ground of this
association . An example profile of a Brunisolic Turbic Cryosol is described
below and illustrated in Figures 10 and 11 .
Site : WZ2 Location : 73 ° 37'N 94° 50'W
Bmy - 0 to 25 cm, discontinuous, olive brown (2 .5Y 4/4 moist) silt loam,
massive, plastic, firm when moist, firm when dry ; clear, smooth
boundary .
Bgy - 25 to 45 cm, discontinuous, olive brown (2 .5Y 4/4 moist) silty clay,
massive, plastic, firm when moist, hard when dry, distinct mottles ;
clear, smooth boundary .
Cy - 22 to 50 cm, discontinuous, olive yellow (2 .5Y 6/4 moist) silty
clay loam, massive, plastic, firm when moist, hard when dry ; clear,
abrupt boundary .
C 1yz- 45 to 68 cm, olive yellow (2 .5Y 6/4) silty clay loam, some organic
intrusions, well-bonded ice crystals ; clear, smooth - boundary .
C 2yz- 68 cm plus, olive yellow (2 .5Y 6/4) silty clay loam, well-bonded
ice with soil inclusions .
The physical and chemical analyses of this soil is presented in Tables 12, 13 & 14 in the Appendix . Drainage in this parent material is imperfect to poor .
The permafrost table is 60 to 70 cm below the surface . Vegetation cover
is generally higher than that of the Scarpbrook Association . Salix arctica ,
graminoid and moss communites are quite common and may cover 50 to 70
percent of the surface . However, most areas only have 30 to 50 percent
5 8
cover of Saxifraga oppositifolia , Salix arctica and Dryas integrifolia .
Gifford Point Association
The Gifford Point Association refers to soils of Lithic Regosol
and Lithic Regosolic Cryosol of a Tertiary formation consisting of
sandstone, shale and lignite at Cunningham Inlet . Netterville, et al .
(1976) consider this formation is identical to the Eureka Sound Formation
known on Axel Heiberg Is . The outcrop is limited to an area of about 10
hectares and is deeply eroded by gullies and ravines . This formation is
fossil-rich (Tuke, et al ., 1966) and is extremely poorly consolidated
(Veillette, 1976) ; a control section exceeding a meter in depth can easily
be dug through the bedrock . There is hardly any indication of soil develop-
ment on the unconsolidated material . The only vegetation cover of the
gullies consists of very scattered individuals of Papaver lapponicum ssp .
occidentale and Draba spp ; the total cover does not exceed 1 percent .
However, the surfaces which are not subject to erosion have 10 to 30
percent vegetation cover .
Howe Harbour Association
The Howe Harbour Association consists of Brunisolic Turbic Cryosol
soils, and to a lesser degree, Regosolic Turbic Cryosol soils of strongly
to very strongly calcareous loam . This association occurs on Somerset
Is . and is found along the margins of a band of sedimentary rock sandwiched
between the Precambrian Ridge to the west and the limestone upland in the
east (Read Bay Formation) . The parent material originates from a mixture of
weathered Paleozoic dolomite and a small amount of till . The topography is
gently rolling and most of the slopes are heavily colluviated . Mass wasting
5 9
is very active in these areas . An example profile of a Brunisolic Turbic
Cryosol is given below :
Site : W31 Location : 73° 30'N 94 ° 00'W
Ahy - 0 to 25 cm, discontinuous, brownish yellow (l0YR 6/2 moist) loam,
single grained, plastic, friable when moist, hard when dry ; clear,
abrupt boundary .
Bmy - 0 to 54 cm, discontinuous, dark yellowish brown (l0YR 4/4 moist)
loam, single grained, plastic, friable when moist, firm when dry ;
clear, smooth boundary .
Cy - 10 to 54 cm, discontinuous, dark yellowish brown (l0YR 3/4 moist)
loam, massive, plastic, friable when moist, firm when dry, some organic
inclusions ; clear, smooth boundary .
Cz - 54 cm plus, dark yellowish brown (10YR 3/4) loam, well-bonded
randomly oriented ice .
Table 15 in the Appendix presents the chemical and physical analyses of
the sample . Drainage in these soils is imperfect to poor, with the frost
table resting 50 to 60 cm below the surface . Polyblastia spp . and Blindia
acuta are the dominant species, forming surface cover of 50 to 70 percent .
Hunting Association
The Hunting Association consists of soils of Gleysolic Turbic
Cryosol and .Brunisolic Turbic Cryosol developed on colluvium of extremely
calcareous medium texture material originated from weathered Paleozoic
bedrock calcareous till . This association is generally less stony than
the Scarp Brook Association but the silt content is higher . An example of
a profile of this type is given as follows :
Site : WZ4 Location : 73° 38'N 95° 12'W
Bm - 0 to 15 cm, strong brown (7 .5YR 5/6 moist) silt loam, massive,
plastic, firm when moist, hard when dry ; clear, smooth boundary .
Bgy - 0 to 26 cm, yellowish brown (l0YR 5/6 moist) silt loam, extremely
rheotropic, massive, plastic, firm when moist, hard when dry,
60
distinct mottles ; clear, smooth boundary .
Cgy - 26 to 60 cm, strong brown (7 .5YR 5/4 moist) silt loam, massive,
plastic, firm when moist, hard when dry, faint mottling, some organic
intrusions ; clear, smooth boundary .
Cgz - 60 to 68 cm, reddish brown (7 .5YR 6/8) silt loam, faint mottling,
ice not visible ; clear, abrupt boundary .
IICZ- 68 cm plus, reddish brown (7 .5YR 6/8) silt loam, very stony, ice not
visible .
The internal drainage of this soil is poor even though it associates
with slopes that may reach 30 percent . This is due to the permafrost
acting as an impervious layer . Salix arctica , mosses and graminoids
grow on these soils forming a 70 to 100 percent cover . The chemical and
physical properties as well as a soil temperature profile is presented in
Tables 17 and 18 in the Appendix .
Internal drainage is imperfect in the active layer, the thickness of
which varies from 50 cm to 70 cm . Overall vegetation cover is generally
in the 70 to 80 percent range . The speices that associate with this
association is quite characteristic and are dominated by Saxifraga
oppositi folia and Polyblastia spp ; other species include Saxifraga
caespitosa , P apaver lapponicum ssp . occidentale , Cerastium alpinum and Draba
spp .
The physical and chemical properties of the soil parent material are
listed in Table 16, Appendix 1 .
Leopold Association
The Leopold Association includes all the erosional products of
Paleozoic bedrock . Thus, the unconsolidated materials of screes and
61
talus fall into this association which is quite abundant on the sides of the deep
canyons in northeastern Somerset . Soil development, if any, is negligible
on these slopes . This is also the only association in which a frozen
layer may not be found in the first meter of the control section . The
soils found here belong to Lithic Regosolic Turbic Cryosol and Orthic and
Lithic Regosol . Rock glaciers are not uncommon on the northern half of
the study area . These steep slopes are barren of any vegetation .
Lyons Point Association
The Lyons Point Association comprises Brunisolic Turbic Cryosol
soils and a certain amount of Regosolic Turbic Cryosol soils ; the latter
occupy mostly the well drained areas . The parent material of these soils
is a moderately stony, loamy till which is derived from a mixture of
sandstone and dolostone bedrock . The soils are strongly calcareous with a
moderately high dolomite content but a low calcite content . Patterned ground
types such as sorted and non-sorted nets and circles are common . The
active layer thaws to 50 to 60 cm deep in August, and internal drainage is
well drained to imperfect . Vegetation cover of 20 percent, consisting of
Saxifraga oppositifolia , Draba corymbosa and Salix spp . occupy the mesic
sites . On seepage slopes Polyblastia- Cephaloziella communities may cover
up to 100 percent of the area . A Brunisolic Turbic Cryosol is described
below and laboratory analyses results are in Table 19 in the Appendix .
Bmy - 0 to 5 cm, dark yellowish brown (l0YR 4/2 moist) clay loam, granular,
plastic, firm when moist, hard when dry ; clear, wavy boundary .
Cy - 5 to 58 cm, dark yellowish brown (l0YR 4/1 moist) clay loam, massive,
plastic, firm when dry, hard when dry ; clear, abrupt boundary .
62
Cz - 58 cm plus, dark yellowish brown (l0YR 4/1) clay loam, well-bonded
segregated ice veins and crystals .
Mount Clarendon Association
This association comprises frost shattered calcareous bedrock on
which there are no indications of soil development . The material is extremely
calcareous and is-high in dolomite content . Frost heaving is shown by the
frequent occurrence of flat stones standing on edge, and a diffuse polygonal
pattern on the boulder fields . The vegetation is very sparse, less than
1 percent cover, consisting of Draba corymbosa , Papaver lapponicum ssp .
occidentale and some foliose lichens .
Mount Matthias Association
The dominant soils in the Mount Matthias Association are Regosolic
Turbic Cryosol on the uplands and Brunisolic Turbic Cryosol at lower
elevations of Prince of Wales Island . In wet depressions and seepage
slopes fed by permanent snowbanks Gleysolic Turbic Cryosol develops . The
parent material which is originally derived from calcareous sandstones
and conglomerates, and deposited as till, is modified by cryoturbation .
Colluviation on moderately steep, actively wasting slopes further modifies
the parent material . Based on 13 samples the parent material has a fairly
high stone content of 14 percent . On the average, the calcite content is
high (26 percent), but the dolomite content is low (9 percent) . Permafrost
induced microrelief such as sorted and non-sorted circles, nets, and stripes
are common . The active layer was 45 to 60 cm thick in early August . The
vegetation cover varies from 10 to 30 percent with Salix arctica , Saxifraga
oppositifolia and Poa arctica as the main vascular species . Up to 100
percent of the ground may be covered with Polyblastia-Poa or Polyblastia-
Cephaloziella communities .
63
A Regosolic Turbic Cryosol, developed on an imperfectly drained
6 percent N slope, with imperfectly sorted stripes, is described below .
Site : W85 Location : 73 ° 42'N 99 ° 12'W
Bmjy- 0 to 5 cm, gray brown (2 .5Y 5/2 moist) loam, vesicular, plastic,
firm when moist, hard when dry ; diffuse boundary .
Cy - 5 to 46 cm, gray brown (2 .5Y 5/2 moist) clay loam, massive, plastic,
firm when moist, hard when dry ; clear, smooth boundary .
Cz - 46 cm plus, gray brown (2 .5Y 5/2) clay loam, well-bonded with random
ice veinlets and crystals .
The chemical and physical characteristics of this soil are presented
in Table 20 in the Appendix . The vegetation cover is about 20 percent
consisting mainly of Polyblastia spp ., Blindia acuta , Saxifraga oppositifolia ,
Draba corymbosa and Luzula nivalis . Otrick Island Association
The Otrick Island Association includes soils of Regosolic Turbic
Cryosol and Brunisolic Turbic Cryosol forming on the alluvium of Mid-
Arctic Precambrian areas . The parent material consists of stratified acidic sand, silt and gravel, and the degree of soil development is more advanced than river terraces of calcareous bedrock . These soils are well drained internally and the active layer is 80 to 90 cm thick . Vegetation cover ranges from 50 to 70 percent ; these are mostly communities of
Saxifraga oppositif olia , Cetraria cucullata , Cetraria nivalis and
Stereocaulon spp .
Palmerston Point Association
Palmerston Point Association includes the frost-shattered layer of acidic - rubbles and shingles occurring as the uncoAsolidated-material covering Precambrian gneiss, schists and granite . These soils are confined to Precambrian rock outcrop areas . Frost shattering accounts for most of the weathering that has taken place .
Prince Regent Association
The Prince Regent Association is the group of Brunisolic Turbic
Cryosol, Regosolic Turbic Cryosol and Regosolic Static Cryosol soils of which the parent material is an extremely calcareous, medium to coarse
texture till which has been marine modified . While the main body of this material lies along the tributaries of the Central and East Creswell River,
it may extend above the late Pleistocene marine limit of 150 m a .s .l . It
can be distinguished from the Fearnall Bay Association by virtue of its higher clay and silt content and distinct color . The physiography is
characterized by low hills and ridges dissected by small rivers . The
descriptions of a Brunisolic Turbic Cryosol soils is given as follows :
65
Site : W72 Location : 73° 04'N 92 ° 22'W
Bmg - 0 to 10 cm, dark yellowish brown (l0YR 4/3 moist) loam, vesicular,
plastic, firm when moist, firm when dry ; clear, wavy boundary .
Cy - 10 to 56 cm, dark yellowish brown (l0YR 4/3 moist) loam, massive,
plastic, firm when moist, firm when dry ; clear, abrupt boundary .
Cz - 56 cm plus, dark yellowish brown (l0YR 4/3 moist) loam, well-bonded
randomly oriented ice .
Physical and chemical characteristics of the soil are presented in
Table 21 in the Appendix .
The active layer in these areas is 50 to 60 cm thick. Drainage is
between well drained and imperfect . The extreme calcareousness is at least
partly responsible for the scanty vegetation cover which is below 5 percent .
The recurring species are Papaver lapponicum ssp . occidentale , Draba eorymbosa
and Cerastium arcticum .
Scarp Brook Association
The dominant soils of the Scarp Brook Association are Regosolic
Turbic Cryosol, but some weakly developed Brunisolic Turbic Cryosol
soils are also found . The poorly drained members develop Gleysolic Turbic
Cryosol soils . The soils of this association developed on an exceedingly
stony (33 percent stones by weight) carbonate-rich loam textured parent
material . The calcite content and dolomite content are high (Section 5 .6) .
The parent material is a till, enriched by bedrock materials due to frost
heaving . Permafrost related microrelief, such as sorted circles, nets and
stripes are common . The active layer was 50 to 85 cm deep in early August .
Vegetation cover is characteristically less than 10 percent, often less than
1 percent on the well and imperfectly drained members, but may be as high
as 30 percent on poorly drained members . Salix arctica , Draba corymbosa
and Dryas integrifo lia are characteristic plants .
A Regosolic Turbic Cryosol, developed on a well drained 5 percent
SW slope, with poorly sorted nets, is described below .
Site : W100 Location : 73° 35'N 100 ° 05'W
Bmjy- 0 to 6 cm, pale brown (l0YR 6/3 moist) loam, vesicular, plastic,
firm when moist, hard when dry ; gradual, wavy boundary .
Cy - 6 to 71 cm, gray brown (l0YR 5/2 moist) loam, single grained, plastic,
firm when moist, hard when dry ; clear, smooth boundary .
Cz - 71 cm plus, frozen gray brown (l0YR 5/2 moist) loam, stony with
well-bonded randomly oriented ice crystals and veinlets .
The chemical and physical characteristics of this soil are presented in
Table 22 in the Appendix . The vegetation cover is about 5 percent, occurring
mainly in the cracks of sorted nets . Dominant species are Thamnolia
vermicularis, Arenaria sajanensis , A. rubella , Papaver lapponicum ssp .
occidentale and Saxifraga îoppositifolia .
6 7
Stanwell Fletcher Association
The Stanwell Fletcher Association consists of soils of Brunisolic
Turbic Cryosol and Regosolic Turbic Cryosol derived from very strongly
calcareous till over Tertiary sandstone and shale . This bedrock formation
is also poorly consolidated . A layer of till about 1 .5 m in thickness
covers this bedrock, and both Precambrian and Paleozoic erratics are
present on the gently sloping and undulating surface . An example profile
of a Brunisolic Turbic Cryosol is described as follows :
Site WZ19 Location: 72 ° 58'N 94° 57'W
Bm - 0 to 6 cm, dark yellowish brown (l0YR 3/4) single grained, plastic,
friable when moist, firm when dry ; clear, abrupt boundary .
Cy - 6 to 55 cm, olive brown (5Y 5/3 moist) clay loam, massive, plastic,
firm when moist, hard when dry ; clear, abrupt boundary .
Cz - 55 to 60 cm, olive (5Y 5/3) clay loam, well-bonded ice crystals and veinlets ;
clear, abrupt boundary .
IICZ- 60 cm plus, olive (5Y 5/1) sand, well-bonded segregated ice crystals .
The active layer of these soils is about 60 to 70 cm thick and
internal drainage is good . Vegetation such as Cassiope tetragona , Salix
arctica , Cladonia spp ., - Alectoria spp . cover 30 to 50 percent of the
surface . Chemical and physical properties of this soil are listed in
Tables 23, 24 and 25 of the Appendix .
68
Transition Bay Association
The Transition Bay Association is comprised of Brunisolic Turbic
Cryosol and Brunisolic Static Cryosol soils developed on marine sands and
sandy loams . The drainage is imperfect to well drained, but poorly drained
sands are also found . The parent material is usually stone-free to slightly
stony . The material is moderately calcareous, containing both calcite and
dolomite . Ice wedge polygons are frequent, often with non-sorted circles
in the central part of the polygons . The active layer was 50 to 80 cm
thick in early August . Vegetation cover varies from about 20 percent
in Salix-Dryas communities on well drained sites to 70 to 100 percent cover
in Cetraria-Saxifraga communities on well drained sites .
A Brunisolic Turbic Cryosol, developed on a level plain with no
microrelief, is described below .
Site : W91 Location : 73 ° 45'N 97° 36'W
Bmy - 0 to 45 cm, dark gray brown (l0YR 4/2 moist) sandy loam, many organic
intrusions, single grained, non-plastic, friable when moist, loose
when dry ; clear, smooth boundary .
Cz - 45 cm plus, dark yellowish brown (l0YR 2/2 moist) sandy loam,
well bonded, ice not visible .
The chemical and physical characteristics of this soil are presented
in Table 26 in the Appendix . Vegetation cover is continuous with Stereocaulon
paschale, Polyblastia sp ., Luzula nivalis, Saxifraga oppositifolia,
Thamnolia vermicularis being the recurring species .
69
Two Rivers Association
The Two Rivers Association includes soils of Brunisolic Turbic
Cryosol and Regosolic Turbic Cryosol developing on extremely calcareous
coarse texture till and weathered bedrock of the Peel Sound Formation on
Somerset Is . The parent material is characterized by a high dolomite
but low calcite content . The topography is severely dissected by drainage
systems resulting in hilly ridges and hills with fairly steep slopes . An
example is given below of a Brunisolic Turbic Cryosol .
Site : W21 Location : 73 ° 07'N 93 ° 36'W
Ahy - 0 to 10 cm, discontinuous, olive brown (l0YR 3/2 moist) sandy loam,
single grained, slightly plastic, friable when moist, loose when dry ;
clear, irregular boundary .
Bmy - 0 to 20 cm, olive brown (l0YR 4/4 moist) sandy loam, single grained,
slightly plastic, friable when moist, loose when dry ; clear, abrupt
boundary .
Cy - 20 to 57 cm, light olive brown (l0YR 5/4 moist) sandy loam, single
grained, non-plastic, friable when moist, loose when dry ; clear,
abrupt boundary .
Cz - 57 cm plus, light olive brown (l0YR 5/4) sandy loam, well-bonded
randomly oriented ice .
Table 27 in the Appendix gives the chemical and physical properties
of the parent material .
The depth of the permafrost table is between 60 to 70 cm . Internal
drainage is between well drained and imperfect . Vegetation cover ranges
from 30 to 80 percent consisting of communities of Saxifraga oppositifolia ,
Dryas integrifolia and Salix arctica in areas of dense cover . 7 0
Wadworth Island Association
This is an association of soils of Orthic Regosol, Lithic Regosol and Lithic Regosolic Turbic Cryosol of which the parent material is the unconsolidated material of Precambrian talus and screes . There are no indications of soil development . These canyons are not as deep as those found in northeastern Somerset Is . The surfaces are generally devoid of any vegetation .
Scott Bay Association
The Scott Bay Association comprises soils of Regosolic Turbic
Cryosol and Brunisolic Turbic Cryosol which develop on glaciofluvial and ice-contact deposits on sedimentary bedrock in the High Arctic . The parent material is an extremely calcareous sandy loam to coarse sand . In terms of distribution it occurs mostly on Prince of Wales Island ; on Somerset
Island this association is represented only by an esker south of Aston
Bay . These sites are generally well-drained with a very sparse (under 5%) vegetation cover which consists of mostly Papaver lapponicum ssp . occidentale
and Draba spp . The thickness of the active layer in August is 60 to 70 cm.
A summary of the characteristics of soil associations and those named for Peninsula can be found in Table 28 in the Appendix and Table 5 . Table 5 . Soil Associations Occurring in Boothia Peninsula (after Tarnocai, in press) .
Map Association Ecodistrict Parent Material Descriptions Subgroup Name and Drainage Class Symbol Name
Am2 Amituryouak 2 M3 Less than 1 .5 meters of 50% Brun . T . Cryosol (w-i) extremely calcareous sandy 40% Lithic Brun . T . Cryosol (w) loam to sandy clay loam 10% Gley . T . Cryosol (p) glacial till over limestone bedrock .
Nd2 Nudlukta 2 M3 Less than 1 meter of moder- 40% Brun . S . Cryosol (w-i) ately to strongly calcareous 30% Rego . S . Cryosol (w-i) marine sand and gravel . 30% Lithic Brun . S . Cryosol (w-i)
Pb3 Pasley Bay 3 M5, M6 Less than 1 .5 meters of very 40% Rego . T . Cryosol (w-i) strongly to extremely cal- 40% Lithic Rego . T . Cryosol (w-i) careous sandy clay loam 20% Gley . T . Cryosol (p) glacial till over limestone bedrock .
Pb4 Pasley Bay 3 M4, M5, M6 Less than 1 .5 meters of very 50% Lithic Rego T . Cryosol (w-i) strongly to extremely cal- 30% Brun . T . Cryosol (w-i) careous sandy loam to sandy 20% Gley . T . Cryosol (p) clay loam glacial till over limestone bedrock .
S12 Stilwell M4, M6 Less than 1 .5 meters of 50%Rego . S . Cryosol (w-i) Bay 2 strongly to extremely cal- 50% Lithic Rego . T . Cryosol (w-i) careous marine gravel over limestone bedrock .
7 2
5 .6 Chemical Properties of Some Major Soil Associations
The present study takes advantage of the chemical and physical
differences between soil parent materials in the grouping of soil
associations . The accuracy of this method is apparent in statistical
analyses of the laboratory results . The equivalent and calcite and CaCO3 dolomite contents were found to be very efficient variables in separating
associations . Table 6 gives the means and standard deviations of some of
these variables .
Table 6 . Means and Standard Deviations of Carbonate Content .
Parent Materials % Equivalent % Calcite % Dolomite No . of Samples CaCO3
Batty Bay 60 .94 ± 8 .27 53 .13 ± 12 .74 7 .20 ± 5 .01 5 Fearnall Bay 41 .67 ± 9 .24 14 .30 ± 5 .57 25 .21 ± 4 .69 11 Fiona Lake 34 .69 ± 15 .94 12 .50 ± 2 .87 20 .44 ± 13 .46 4 Fitz Roy 35 .19 ± 5 .12 13 .37 ± 1 .21 20 .16 ± 7 .40 5 Howe Harbour 27 .61 ± 13 .20 1 .36 ± 1 .28 24 .24 ± 12 .48 7 Lyons Point 36 .53 ± 7 .36 9 .88 ± 7 .36 26 .62 ± 5 .50 4 Mount Matthias 29 .39 ± 10 .96 15 .34 ± 11 .03 13 .18 ± 9 .39 15 Scarp Brook 58 .92 ± 15 .47 26 .02 ± 18 .48 36 .03 ± 17 .50 39
It can be seen immediately that , equivalent is higher in certain CaCO3 parent materials than in others . The extremely calcareous ones are :Batty
Bay and Scarp Brook Associations . It is also interesting to note that both
a sandstone till (Mount Mathias) and a dolomite-dominated till (Howe
Harbour) turned out to be less calcareous than till on Precambrian bedrock
(Fitz Roy and Fiona Lake loams) . These materials have very similar values
in their total equivalents . Yet, they are kept separate for it was CaCO3 of equivalent was not due to the realized that the high variability CaCO3 small number of samples collected but was due to the discontinuous distribution
of the Fiona Lake till .
73
The calcite and dolomite contents are also informative variables in
distinguishing associations . Figure 12 shows that while the CaCO3
equivalent of the Scarp Brook silt loam is generally higher, this
calcareousness may be attributable to either a high calcite or high dolomite
content . Similarly, while the CaCO3 equivalent of MountMatthias till is
only moderate, there is a lack of domination by either dolomite or calcite .
This may be contrasted to the Howe Harbour loam or the Batty Bay silt loam
in which one fraction completely dominates the parent material . The Batty
Bay silt loam is extremely calcareous and is almost exclusively calcite,
whereas the Howe Harbour loam is only moderately calcareous, consisting of
mainly dolomite . Table 7 shows the linear regression and correlation
coefficients of CaCO3 equivalent on calcite and dolomite respectively for
Scarp Brook silt loam . The correlations appear to be equally strong in
either case . However, when the analysis was applied to the Howe Harbour
till the dependence of CaCO3 equivalent on dolomite content is clearly
demonstrated (Figures 13 and 14) .
Table 7 . Linear Regression and Correlation Analysis .
Parent Material No . of Regression Equation St . error t* Correlation Samples of .b Coefficient R*
Scarp Brook 39 EQ = 3 .03 + .32 (CAL) .13 2 .61 .39 39 EQ = 45 .59 + .37 (DOL) .13 2 .80 .42
Howe Harbour 7 EQ = 3 .03 + .20 (CAL) .45 .04 - .19 EQ = 2 .10 + 1 .05 (DOL) .05 2 .24 1 .00
EQ = CaC03 equivalent * all R & t values significant at P = 0 .01 CAL = % calcite DOL = % dolomite
80.
70J
1 Calcite 60J 1 1 . Dolomite
50~
u
30.
20
30 40 ' 50 60 . 90 100 %COC03 Equiv.
Figure ï2 . Tn_e Scarp Lrcox silt !__W is extreme -_ ;
caïcareo-ls . either calcite or dolomite
cortert is rig_^. .
75 70
0 1 O Scarp Brook 60 O Oo e Mount Motth ;as 1 Howe Harbour 50 O O
40
O O O U O O 1 O 1 O O 20 11 O O
0 O 0 O O O 11 A000 O 0 -1 r be O O 0 10 20 30 40 50 60 70 80
°/, Dolomite
Figure 14 . The calcite and dolomite composition of three parent materials .
40
30
1 Cacite c Dolom . m 0 20 U
10
0 0 10 20 30 40
COC03 Equiv. Figure 13 . The Howe Harbour sandy loam is dominated by dolomite .
7 6
5 .7 Vegetation Communities
5 .71 Polar Desert Type
Papaver-Draba Community (Map Symbol 1 .1)
This is a community that is most extensive on Somerset Is . and
covers a significant portion of Prince of Wales Island . The total
vegetation is usually under 1%, consisting of scattered individuals of
Papaver lapponicum ssp . occidentale , Draba spp ., Cerastium arcticum and
Saxifraga oppositif olia . The exceptions are sites enriched by wastes of owls
and lemmings ; these locations have 80-100% coverage of Festuca baffinensis ,
Poa arctica, Poa _glauca and Papaver lapponicum ssp . occidentale . The
barreness of the limestone desert is primarily due to cold temperatures,
aridity and excessive calcium carbonate coAtent in the._sub-strate .
Rhizocarpon-Umbellicaria Community (Map Symbol 1 .2)
This is the community type that inhabits the felsenmeer and bedrock
outcrops of the Precambrian uplands . Crustose lichens such as Umbellicaria spp .5
Lecidea spp ., Rhizocarpon geographicum , Rhizocarpon disporum , and mosses
such as Andraeae rupestris and Polytrichum triste are the main species .
The cover of crustose lichen on rock surfaces may be as high as 30% ;
otherwise, the surface is barren except for occasional mosses, fruticose
lichens and Cassiope tetragona growing in crevices .
5 .72 Moss-Grass Vegetation Type
Polyb lastia-Poa Community (Map Symbol 1 .3)
Vegetation cover of the moss-grass type is as low as the polar desert
type, but the scarcity is not due to aridity . The community type of
Polyblastia-Poa are limited in distribution . They are mostly found on the 7 7
fines of non-calcareous to weakly calcareous substrates . Species of
Polyblastia in conjunction with mosses such as Blindia acuta form black crusts on the surface . Poa abbreviata and Cephaloziella spp . are the other common species (Fig . 15) . While=the=black crusts may- cover 30-50% of these imperfectly drained areas, there is a lack of vascular and especially dicotyledonous species ; for this reason, the appearance of this vegetation type resembles the polar desert more than the arctic dwarf shrub .
Polyblastia-Cephaloziella Community (Map Symbol 1 .4)
This is a community that closely resembles Community 1 .3 . The main difference is that there are more bryophyte species such as Bryum cr ophilum and Philonotis fontana due to active surface drainage . Crusts of Polyblastia are also better developed, Like the Polyblastia-
Poa Community, it is limited in distribution .
Heirochloe-Pleuropogon Community (Map Symbol 1 .5)
This community type is found most often in deltaic areas along the coasts . The main species are Heirochloe alpina , Pleuropogon sabinei and
Arctagrostis latifolia . They scatter along the banks of streams that cut through the deltas . The area of coverage of this community type is limited .
The typical % cover is under 1% .
5 .73 Dwarf Shrub Vegetation Type
Saxifragaa-Draba Community (Map Symbol 2 .1)
Arctic dwarf shrub vegetation has a higher % cover than the polar desert and moss-grass types . The basic pattern is the co-occurrence of vascular and non-vascular species with dwarf shrub* components such as
* The term "shrub" is used loosely here to include plants with rosette and cushion growth forms . 7 8
Fi.virrp 15 . The Pol blastia-Poa community type growing on the surface of gneissic fines . Polyblastia spp ., Poa abbreviata , Pol trichum triste and Blindia acuta are the species present .
Figure 16 . The Saxifraga- Polyblastia community type growing on moderately calcareous till on Precambrian gneiss . Lichens such as Cetraria and Polyblastia cover much of the surface . 79
Salix spp ., Saxifraga ooppositifolia , Dryas integrifolia and Cassiope
tetragona . In the Saxifraga-Draba Community, the vegetation cover is
5-10% consisting of Saxifraga oppositifolia , species of Draba , Papaver lapponicum var . occidentale , Cerastium spp . and Poa lauca . This community inhabits the xeric extremely calcareous portions of the Paleozoic uplands in the study area .
Saxifraga-Papaver Community (Map Symbol 2 .2)
This community type is dominated by Saxifraga oppositifolia ,
S . caespitosa , Papaver lapponicum ssp . occidentale , Stereocaulon spp .,
Cetraria cucullata, Cetraria nivalis and Polyblastia spp . It forms a
5-10% cover, but unlike the Saxifraga-Draba Community, it is not found on
excessively calcareous areas . The substrate that is favored by this
community is only moderately to very strongly calcareous . Moderate to well-drained sandstone till is the most favored habitat .
Saxifraga -Dryas Community (Map Symbol 2 .3)
This community usually covers 10-30% of the surface and is dominated bv Saxifraga oppositifolia , Dryas integrifolia , Alopecurus alpinus , Papaver
lapponicum ssp . occidentale and at low elevations Pedicularis spp . This
community is best developed on extremely calcareous mesic sites .
S axifraga-Salix Community (Map Symbol 2 .4)
This community is dominated by Saxifraga oppositifolia and other
common species listed for Community 2 .2 . However, the better moisture
content in the substrate promotes the growth of Salix spp ., mosses and
hepatics . The over-all vegetation cover is 10-30% . Drainage conditions are well to imperfectly drained . Table in the Appendix lists an example
of this type of--community .
80
Salix-Dryas Community (Map Symbol 2 .5)
This community covers 30-70% of the surface . The common species are
Salix spp ., Dryas integrifolia , Polygonum viviparum , Pedicularis spp .,
Distichium capillaceum , Polyblastia spp . Moderately to strongly calcareous
sites which are moderately to imperfectly drained are the best habitats
for this community .
Salix-Àlopecurus Community (Map Symbol 2 .6)
This is a community that is similar to Community 2 .5 in % cover
and species composition . However, a low carbonate content in the substrate
introduces lichens such as Cetraria cucullata, Cetraria nivalis, Cetraria
deliesi and Cladonia spp . Grasses such as Alopecurus alpinus, Poa spp .
and sedges are also favored by these imperfect drainage conditions .
Cetraria-Saxifraga Community (Map Symbol 2 .7)
This is an extensive and very distinctive community that inhabits
weakly to moderately calcareous areas of the Mid-Arctic . The average
vegetation cover is 30-70% consisting of Saxifraga oppos itifolia , Dryas
integrifolia , Cetraria spp ., Alectoria spp ., Stereocaulon spp ., Cladonia
spp ., Luzula spp ., Rhacomitrium lanuginosum and Tortula ruralis . This
community occupies mesic sites .
Cetraria-Cassiope Community (Map Symbol 2 .8)
This type of vegetation is limited in distribution but is very
distinctive . It is dominated by Cassiope tetragona, Dryas integrifolia ,
Cetraria spp ., Stereocaulon spp ., Cladoni a spp . and Luzula confusa .
As a fule this community can only be found in areas underlain by Precambrian
bedrock, forming cover ranging from 70 to 100% . Locations where snowbanks 81
linger late into the growing season are most favored, indicating moist but well-drained conditions are preferred by the vegetation . Table 30 in the
Appendix lists an example of this community .
Salix-Dicranum Community (Map Symbol 2 .9)
The dominant species of this community are species of Salix ,
Carex, Drepanocl adus , Pedicularis and Arctagrostis latifolia . This community never occurs too far from the coasts and is found below an elevation of 150 m . It forms a cover of 70 to 1001 on imperfect to poorly drained soils which range from moderate to extreme in carbonate content .
Saxifraga -Polyblastia Community (Map Symbol 2 .10)
This is a community that grows on imperfectly drained conditions on moderately calcareous soils . It is similar to Community 2 .7, but there is a marked domination by Polyblastia spp . and the associated mosses
(Figure 13) . Typical species are Saxifraga oppositifolia , Papaver lapponicum ssp . occidentale, S . caespitosa, Cetrar ia cucullata, Thamnolia spp .,
Stereocau lon spp . An example of this community is given in Table 31 in the
Appendix . 8 2
5 .74 Sedge Meadow Vegetation Type
Carex-Arctagnos tis Community (Map Symbol 3 .1)
The characteristics of sedge meadows are the continuous vegetation cover and the poor drainage conditions . Carex-Heirochloe communities are dominated by species of Carex , Heirochloe , Salix , Dicranum, Drepanocladus,
Luzula and Arctagnostis latifolia. The vegetation cover is seldom less than
80% and the drainage conditions are inevitably poor . The distribution of this community is wide . An example of relative species abundance in this community is given in Table 32 in the Appendix .
Carex-Drepanocladus Community (Map Symbol 3 .2)
This community is similar to community 3 .1 in site conditions and vegetation cover . However, in this community there is more of a domination by mosses such as Drepanocladus revolens , Distichium capillaceum and
Calliergon giganteum and species of Eriophorum and Juncus . Drainage conditions are too poor for the growth of Salix spp . Water bodies are often found among this community . Table 3 in the Appendix gives an example of the relative species abundance of this community . The characteristics of communities are also summarized in Table 8 . Table 8 . Summary of Vegetation Community Types in the Study Area .
Ecological Vegetation Map Community Type Typical Species Typical x Cover Substrate Drainage Soil Texture Region Type Symbol Carbonate Content
High Polar 1 .1 Papaver-Drabs Papaver lapponicum asp . 0-5% extremely well drained medium to Arctic Desert occidentale , Draba app ., calcareous to imperfect coarse Cerastium spp ., Saxif raga oppositifolia High Polar 1 .2 Rhizocarpon- Rhizocarpon geographicum , 0-57. non-calcareous Well drained medium to Arctic Desert Umbellicaria Lecidea spp ., (excluding to weakly to imperfect coarse Umbellicaria spp ., crustose calcareous Andraeae rupestris lichens) High Moss- 1.3 Polyblastia- Polyblastia spp ., Poa 30-507. non-calcareous well drained medium to Arctic grass " Poa abbreviata , Blindia (including to moderately to imperfect coarse acute , Cephaloziella Polyblastia calcareous app ., Papaver lapponicum spp .) ssp . occidentale High Moss- 1 .4 Polyblastia- Polyblastia app ., Poa 30-50% non-calcareous imperfect to medium Arctic grass Cephaloziella abbreviata , Blindia (including to weakly poor acute, Cephaloziella Polyblastia calcareous spp ., Polytrichum esp .) triste High Moss- 1 .5 Heirochloe- Heirochloe app ., 0-5X non-calcareous imperfect to medium to 6 grass Pleuropogon Pleuropogon sabinei , to moderately poor coarse Mid Arctagroetis latifolia calcareous Arctic High Arctic 2 .1 Saxifraga- Saxifraga oppositifolia , 5-10% Strongly to well drained medium to Arctic dwarf Draba Draba app ., Polyblastia extremely to imperfect coarse shrub spp ., Alopecurus alpinus , calcareous Papaver lapponicum sep . " occidentale Table 8 (cont'd)
Ecological Vegetation Map Community Type Typical Species Typical % Cover Substrate Drainage Soil Texture Region Type Symbol Carbonate Content
High Arctic 2 .2 Saxifraga- Saxifrage oppositifoliu , 5-10% moderately well drained medium t0 Arctic dwarf Papaver Papaver lapponicum sap . to strongly to imperfect coarse shrub occidentals , Cetraria calcareous spp ., Polyblaetia ep . High Arctic 2 .3 Saxifraga- Saxifraga oppositifolia , 10-309 strongly to well drained medium to & dwarf Dryao Drvas integrifolia , extremely to imperfect coarse Mid shrub Alopecurue alpinus , calcareous Arctic Papaver lapponicum app . occidentals High Arctic 2 .4 Saxifraga- Saxifraga oppositifolia , 10-30% moderately well drained medium to & dwarf Salix _S . caespitoer. .. Papaver to strongly to imperfect coarse Mid shrub lapponicum app . calcareous Arctic occidentals , Cetraria ' app . High Arctic 2 .5 Salix-Dryao Salix app ., Dryao 30-70% moderately to imperfect medium to & dwarf integrifolia , strongly to poor fine Mid shrub Polyblaetia sap ., calcareous Arctic Polyponum viviparum , Distichium capillacaum co Mid Arctic 2,6 Salix- Salix app ., Dryryas 30-709 weakly to imperfect medium to Arctic dwarf Alopecurue integrifolia , Alopecurue moderately to poor fine shrub alpinue , Cetraria app,, calcareous Qladonia app, mid Arctic 3,7 Oetraria- 6axifraga opposiclfolia , 30-709 weakly tQ imperfect to medium to Arctir, dwarf baxifra0a Dryas integrifolia , moderately well drained fine ahrO Cetraria app,, Aleptgrig Qal@areou® app ., Rhacomlfrlum ... lanuainoaum Mid Arctic 1,d Cetraria- Caosiope tatragana , 70100% weakly to woll , drainod medium to Arctic dwarf Oessiope Cetraria cucullata, non-oaloareoue ooorae shrub --CT4- ;,~TrKa6epp grifoliainte,~, ,- Table 8 (conta)
Ecological Vegetation Map Community Type Typical Species Typical % Cover Substrate Drainage Soil Texture Region Type Symbol Carbonate Content
High Arctic 2 .9 Salix- Salix app ., Dicranum 70-100% moderately imperfect medium to & dwarf Dicranum app ., Drep anocladue to extremely to poor fine Mid shrub app ., Arctagroatis calcareous Arctic latifolia, Carex spp . Mid Arctic 2 .10 Saxifraga- Saxifraga oppositifolia , 70-100% moderately imperfect fine to Arctic dwarf Polyblastia Polyblastia spp ., to strongly medium shrub Cetraria app ., calcareous _Alectoria sap ., Cladonia app . High Arctic . 3 .1 Carex- & sedge Heirochloe Carex app ., Arctagroatis 70-100% moderately imperfect fine to Mid meadow latifolia , Salix app ., to extremely to poor medium Arctic Dicranum spp ., calcareous Drepanocladue spp ., Luzula app . High Arctic 3 .2 Carex- Carex app ., Arctagrostis 70-100% moderate to imperfect fine to & sedge Drepanocladus latifolia , Heirochloe extremely to poor medium Mid meadow app ., Drepanocladus calcareous 00 Arctic revolens , Distichium capillaceum , Luzula app ., Eriophorum app .
5 .8 Species List of Vegetation
Of the 75 vascular species enumerated, eight are first reports for
Somerset Island and seven are first reports for Prince of Wales Island .
These are annotated in the species list in Table 10 . Samples collected
were deposited at Northern Forest Research Centre Herbarium, Environment
Canada, Edmonton : and the Central Experimental Farm Herbarium, Agriculture
Canada, Ottawa . In addition, 41 mosses, 3 liverworts and 24 lichens were
collected . These samples were deposited at the Northern Forest Research
Centre Herbarium and the University of Alberta Herbarium. Dr . D .H . Vitt
remarked (personal communication) that the occurrence of Lyellia aspera
and Psilopilum cavifolium represents a significant southward extension of
their range .
87
Table l0 .List of Vascular Plants for Somerset and Cornwallis Islands
Nomenclature follows those of Porsild (1964) and Dr . W .J . Cody, Agriculture Canada, who also made the identifications . This is an expansion of the original list provided by Savile (1959) .
* Indicates species not previously reported for Somerset Is . o Indicates species not previously reported for Prince of Wales Is .
1 . Alopecurus alpinus J .E . Smith 2 . Arnica alpina L . Olin ssp . angustifolia (Vahl) Maguire 3 . Arenaria Rossii R.Br . 4 . Arenaria rubella (Wahlenb .) Sm . *5 . Aranaria sajanensis Willd (Mill .) Willd . 6 . Arctagrostis latifolia (R.Br .) Griseb . *7 . Armeria maritima ssp . labradorica (Wallr .) Hult . 8 . Braya purpurascens (R .Br .) Bunge 9 . Campanula uniflora L . 10 . Cardamine bellidifolia L . Wahlenb . 11 . Cardamine pratensis L . var . angustifolia Hook . 12 . Carex amblyorhyncha Krecz . o13 . Carex aquatilis var . stans (Dej .) Bott . 14 . Carex membranacea Hook . o15 . Carex misandra R .Br . 16 . Carex rupestris All . o17 . Carex ursina Dew . 18 . Cassiope tetragona (L .) D . Don 19 . Cerastium alpinum L . 20 . Cerastium beeringianum cham . X Schlecht 21 . Cerastium regelii Ostf . 22 . Chrysosplenium tetrandrum (Lund) Fries 23 . Chrysosplenium iowense anctt . 24 . Chrysanthemum integrifolium Richards . L . 25 . Cochlearia officinalis var . groenlandica (L .) Porsild 26 . Cystopteris fragilis (L .) Bernh . 27 . Deschampsia brevifolia R .Br . 28 . Draba Bellii Holm . 29 . Draba cinerea Adams 30 . Draba crymbosa R . Br . ex DC . 31 . Draba lactea Adams . 32 . Draba nivalis Liljebl . 33 . Draba oblongata R. Br . 34 . Draba subcapitata Simm . 35 . Draba groenlandica F1 . Ekman . 36 . Dryas integrifolia M. Vahl . o37 . Dupontia Fisheri R. Br . 38 . Empetrum nigrum L . 39 . Epilobium latifolium L . 40 . Eqvisetum arvense L . o 4l . Equisetum variegatum Schleich . 42 . Eriophorum angustifolium Honck . *43 . Eriophorum callitrix Cham . 44 . Eriophorum scheuchzeri Hoppe . 45 . Eriophorum triste (Th . Fr .) Hadac & Love 46 . Eutrema edwardsii R . Br . 47 . estuca brachyphylla Schultes . 48 . Testuca baffinensis Polunin * 49 . Hierochloe alpina (Sw .) R . & S . 50 . Hierochloe pauciflora R . Br . 51 . Juncus biglumis L . 52 . Kobresia myosuroides (Vill .) Fiori & Paol . 53 . Luzula confusa Lindeb . 54 . Luzula nivalis (Laest .) Beurl . 55 . Lycopodium selago L . Fenzl . 56 . Melandrium apetalum var . artica (Fr .) Hult . 57 . Melandrium triflorum (R .Br .) J . Vahl . 58 . Oxyria digyna (L .) Hill 59 . Papaver lapponicum (Tolm .) Nordh . ssp . occidentale (Lundstr .) 60 . Parrya arctica R.Br .
89
61 . Podicularis artica R .Br . 62 . Podicularis capitata Adams . 63 . Podicularis hirsuta L . 64 . Podicularis Lanata Cham. & Schlecht . 65 . Podicularis sudetica Willd . 66 . Phippsia algida (Sol .) R.Br . 67 . Plouropogon sabinei R.Br . 68 . Poa abbreviata R.Br . *069 . Poa alpigena (Fr .) Lindm. var . colpodoa (Fr .) Sol . *70 . Poa alpina L . 71 . Poa arctica R.Br . 72 . Poa artica R . Br . var . vivipara *73 . Poa glauca Vahl . 74 . Polygonum viviparum L . 75 . Potontilla hyparctica Malte . 76 . Potontilla pulchella R .Br . 77 . Potontilla rubricaulis Lehm . 78 . Potontilla Vahliana Lehm . 79 . Puccinollia angustata (R .Br .) Rand & Redf . 80 . Puccinollia Bruggemannii Th . Spr . 81 . Puccinellia phryganodes (Trin .) Scribn . & Merr . 82 . Ranunculus hyperboreus Rottb . 83 . Ranunculus nivalis L . 84 . Ranunculus pygmaeus Wahlenb . 85 . Ranunculus sulphurous Sol . 86 . Salix arctica Pallas . 87 . Salix reticulata L . 88 . Salix Richardsonii Hook . 89 . Saxifraga caespitosa L . 90 .' Saxifraga cernua L . 91 . Saxifraga flagellaris Willd . ssp . platysepalia 92 . Saxifraga foliolosa R.Br . 93 . Saxifraga hieracifolia Waldsi . & Kit . o94 . Saxifraga hirculus L . , 9 0
95 . Saxifraga nivalis L . 96 . Saxifraga oppositifolia L . 97 . Saxifraga rivularis *98 . Saxifraga tenuis Sm . 99 . Saxifraga tricuspidata Rottb . 100 . Silene acaulis L . var . exscapa (All .) DC . 101 . Stellaria humifusa Rottb . 102 . Stellaris crassipes Hult . *103 . Stellaria laeta Richards . 104 . Stellaria monantha Hult . 105 . Taraxacum hyparcticum Dahlst . 106 . Taraxacum phymatocarpum J . Vahl . 107 . Taraxacum pumilum Dahlst . 108 . Trisetum spicatum (L .) Richt . 109 . Woodsia glabella R .Br .
91
Table ll .List of Mosses Collected on Somerset Island
Identifications were made by Dr . D .H . Vitt, University of Alberta .
1 . Andraea rupestris Hedw . 2 . Aulacomnium turgidum (Wahlenb .) Schwaegr . 3 . Blindia acuta (Hedw .) B .S .G . 4 . Bryum cryophilum Mart . 5 . Bryum pseudotriquetrum (Hedw .) Schwaegr . 6 . Calliergon giganteum (Schimp .) Kindb . 7 . Calliergon sarmentosum (Wahlenb .) Kindb . 8 . Campylium arcticum (Williams) Broth . 9 . Catoscopium nigritum (Hedw .) Brid . 10 . Cinclidium arcticum (B .S .G .) Schimp . 11 . Cirriphyllum cirrosum (Schwaegr . ex Schulres) Grout 12 . Cratoneuron filicinum (Hedw .) Spruce 13 . Dicranoweisia crispula (Hedw .) Milde . 14 . Dicranum elongatum Schwaegr . 15 . Didimodon asperifolius (Mitt .) Crum, Steere & Anderson 16 . Distichium cf . capillaceum (Hedw .) B .S .G . 17 . Ditrichum flexicaule Schwaegr . 18 . Drepanocladus brevifolius (Lindb .) Moenk 19 . Drepanocladus revolvens (Sw .) Warnst . 20 . Encalypta rhaptocarpa Schwaegr . 21 . Encalypta alpina Sm . 22 . Gymnostomum recurvirostrum Hedw . 23 . Hylocomium splendens (Hedw .) B .S .G . 24 . Hygrohypnum polare (Lindb .) Loeske 25 . Hypnum bambergeri Schimp . 26 . Hypnum vaucheri Lesq . 27 . Lyella aspera (Hag . & C . Jens .) Frye 28 . Myurella julacea (Schwaegr .) B .S .G . 29 . Orthothecium chryseum (Schulres) B .S .G . 30 . Philonotis fontana var . pumila (Turn .) Brid . 31 . Pogonatum alpinum (Hedw .) Roehl . 9 2
32 . Pseudoleskeela nervosa (Leskeela nervosa) (Brid .) Loeske 33 . Psilopilum cavifolium (Wils .) Hag . 34 . Rhacomitrium languinosum (Hedw .) Brid . 35 . Rhacomitrium sudeticum (Funck) Bauer 36 . Scapania simmonsii 37 . Scorpidium turgescens (T . Jens .) Loeske 38 . Tomenthypnum nitens (Hedw .) Loeske 39 . Tortella arctica (Arnell) Grundw. & Nyh . 40 . Tortula mucronifolia Schwaegr . 41 . Tortula ruralis (Hedw .) Gaertn ., Myer & Scherb .
Table 12 . List of Liverworts Collected on Somerset Island
Identifications were made by Dr . D .H . Vitt, University of Àlberta .
1 . Anastrophyllum minutum 2 . Blepharostoma trichophyllum (L .) Dum. 3 . Gymnomitrion eorallioides Leberm.
9 3
Table 13 . List of Lichens Collected on Somerset Island
Identifications were made by Dr . D .H . Vitt, University of Alberta .
1 . Alectoria ochroleuca (Hoffm .) Mass . 2 . Alectoria pubescens (L .) R .H . Howe 3 . Cetraria cucullata (Bell) Ach . 4 . Cetraria delisei (Bory ex Schaer .) Th . Fr . 5 . Cetraria nivalis (L .) Ach . 6 . Cetraria tilesii Ach . 7 . Cladina mitis (Sandst .) Hale & W . Culb . 8 . Cladonia multiformis Merr . 9 . Cladonia pyxidata (L .) Hoffm . 10 . Dactylina arctica (Hook .) Nyl . 11 . Lecanora epibryon (Ach .) Ach . 12 . Lecanora verrucosa Ach . 13 . Lecidea decipiens (Hedw .) Ach . 14 . Lecidea dicksonii (Gmel .) Ach . 15 . Lecidea milinodes (Korb .) Magn . 16 . Parmelia centrifuga (L .) Ach . 17 . Peltigera aphtosa (L .) Willd . 18 . Peltigera canina (L .) Willd . 19 . Polyblastia spp . 20 . Rhizocarpon disporum (naeg . ex Hepp .) Mull . Arg . 21 . Rhizocarpon geographicum (L .) DC . 22 . Sarcogyne simplex (Dav .) Nyl . 23 . Solorina crocea (L .) Ach . 24 . Stereocaulon paschale (L .) Hoffm . 25 . Thamnolia vermicularis (Sw .) Ach . ex Schaer .
9 4
6 . DISCUSSIONS AND ADDITIONAL RESULTS
6 .1 Soil Forming Processes
Since the mid-sixties much of the controversy over the nature of
soil formation in the Arctic has subsided . However, it is less certain
whether the issue has actually been resolved . In North America the
system of classification developed by Tedrow (1966) enjoys the most
following but it is still at odds with the Soviet classification developed
by Ivanova (1963) and her colleagues . A brief review is perhaps warranted
here so that the problem may be understood .
The opinions of Tedrow and colleagues may be found in their many
publications (Tedrow and Douglas, 1964 ; Tedrow, 1964 ; Hill and Tedrow, 1961 ;
Tedrow and Cantlon, 1958 ; Tedrow and Brown, 1962) . According to this view
the Alaskan Arctic Brown soil is the zonal soil of the tundra and the
Polar Desert Soil is the zonal soil of the High Arctic . Pedogenic processes
in both cases are identical except the latter is the result of a "weakening
of soil-forming potential" (Tedrow, 1966) . Arctic Brown is formed on well
drained sites, and by processes which are equivalent to weak podzolization ;
in other words, there is no qualitative difference in soil formation
between temperate and arctic environments . Since a criterion in the estab-
lishment of zonality is the maturity of the soil in question, gleyed soils
which were previously thought to be zonal were rejected as being arrested
in their development . Tedrow (1962) also considers the influence of frost
processes to be strictly mechanical in nature . Cryoturbation is largely
responsible for the erasure of soil horizons and therefore has no benefits
to pedogenesis .
Soviet workers (Ivanova, 1963 ; Fedorova and Yarilova, 1972), on the
95
other hand, recognize the uniqueness of the Arctic environment in soil
classification . It is realized that the poor drainage conditions of
tundra is due to the presence of the permafrost acting as an impervious
layer ; therefore, permafrost can no longer be considered as inactive in
soil development . Zonality can therefore be based on the occurrence of
permafrost ; in fact, in the discontinuous permafrost zone it is acceptable
to have two zonal soils in the same area . Frost processes, including
cryoturbation, are considered to be important pedogenic processes, and
the term cryopedogenesis is generally accepted .
The Canadian viewpoint on the subject has been presented by Pettapiece
(1974) and Tarnocai, et al . (1973) . It supports the contention that
pedogenesis in the permafrost regions is unique in character and the Order
Cryosol was adopted in the classification of arctic soils . That the
Canadian position is essentially correct may be supported by the following
lines of reasoning .
Firstly there are sufficient experimental work to prove that freeze-
thaw action in the soil is not only a physical process but a chemical one
as well . Hinman (1970) found that freeze-thaw cycles increased exchangeable
NH4-N but decreased exchangeable K in three Saskatchewan soils . Graham
and Lopez (1969) on the other hand, found that freeze-thawing releases
potassium in various Missouri soil parent materials . Whatever the exact
mechanism may be, it appears that freeze-thaw cycles cause changes in soil
chemistry in addition to modifying soil structure . Moreover, the potentcy
of this treatment is indicated by the small number of cycles required to
produce detectable results (in the order of 20 to 30 cycles) .
If arctic soil formation is characterized by intense frost actions, 9 6
one would expect the number of freeze-thaw cycles in the soil to increase with latitude . Frazer (1959) presented what seemed to be contradictory data for the number of freeze-thaw cycles in the Mid-Arctic is 20 to 30 annually, whereas central Manitoba records 40 to 60 cycles . However, these figures were extrapolations from air temperature measurements and the thermal regime in the soil does not necessarily follow such trends . Unpublished data of Mills, et al . (1974) indicate that central Manitoba soils (at a depth of 50 cm) experience only one cycle of freeze-thawing annually ; on the other hand, the data of Cook and Raiche (1962) show that in the High
Arctic the active layer freezes and thaws with air temperature changes and the number of such cycles in the soil is much higher than in southern latitudes . Thus it seems plausible that freeze-thawing accounts for much of the chemical weathering in arctic soil development .
Secondly, the role of permafrost in pedogenesis must not be down- graded . Tedrow (1966) apparently considers permafrost and frost processes to influence soil development in largely a negative way ; frost processes disrupt horizon development and permafrost impedes soil drainage (Fig : 17 6 18) .Howeve: if one examines the profile of an arctic soil, one would immediately realize that the most striking feature is the occurrence of the permafrost layer ; it is, therefore, not a mere chance occurrence but is the expression in the soil of a particular type of environment,much like the occurrence of the Bt horizon in the northern temperate forests and the Ah horizon in grasslands . The adoption of the frozen layer as the diagnostic horizon in the Order Cryosol is thus more than just a choice of convenience . Moreover, it has been shown that the permafrost not only impedes internal downward drainage, but the peculiar thermal conditions that associate with it influences the movement of nutrients and water in the active layer (Tarnocai,
9 7
Figure 17 . OrFanic intrusions in a Brunisolic Turbic Cryosol on marine till .
` T - Ah= Orny Frost Table Cz
Figure 18 . Profile o ¬ a Brunisolic Turbic Cryosol on marine till .
9 8
1972 ; Hoekstra, 1969) . The permafrost also causes more gradual thawing of
the active layer during the summer, thus keeping a high water content in
the soil throughout the summer . The behavior of permafrost is thus
more complex than acting merely as an inert impervious layer .
6 .2 Rheotropic Soils
Rheotropy is a phenomenon known among plastic soils and its occurrence
is quite widespread . It may be defined as a reversible isothermal strength
weakening of clay-water systems from high to lower yield values on dis-
turbance (Yong and Warkentin, 1975) . It is sometimes referred to as
thixotropy but the authors feel the latter term should be restricted to
sol-gel transformations and not gel-gel transformations (a sol is by
definition a liquid and has no yield value) .
While Yong and Warkentin (1976) describe rheotropy mostly among
clays this phenomenon has been observed in silts as well in the study area .
Liverovskaya-Kosheleva (1965) also report 'thixotropism' in silts of the
Soviet tundra . The Soviet authors also think that chemical changes are
involved in the process . However, the opinions of Drs . J .A . McKeagure and
G .C . Topp of the Soil Research Institute, Agriculture Canada, are that
rheotropy in the Canadian Arctic is strictly a physical phenomenon (personal
communication) . The key to the transformation hinges on the water content
of the soil ; rheotropy occurs when the water content is .above the liquid
limit but within the plastic range . Stirring or disturbance causes the
structure of absorbed water on clay particles to break up ; the particles
and fabric units are at the same time rearranged so that the bonds between
them are broken, the clay mass then flows under self weight for the water
saturated fabric structure has collapsed . Recovery or 'rest-hardening' 9 9
Figure 19 The rectangular high-centered ice wedge polygons of S . Somerset Island is associated with the Fitz Roy Association . Non- sorted nets have developed inside the polygons .
Figure 20 . The vesicular structure in the surface 20 cm of many silty soils is probably caused by formation of ice crystals . Note also the surface shrinkage crack caused by freezing and/or dessication . 100
occurs when the system regains a state of minimum energy or maximum attraction between fabric units . Whether the original full strength will be regained depends on the properties of the clay minerals, the original fabric structure and the degree of disturbance (Yong and Warkentin, 1975) .
If water content is the essential factor in rheotropic behavior, then one would not expect it to be a strictly arctic phenomenon . Indeed, this property is known in soils of the boreal forest as well . However, when permafrost is present, it maintains a nearly water-saturated active layer during the summer and high water content are ideal conditions for plastic changes to occur ; thus, rheotropy is more common in the Arctic .
On Somerset and Prince of Wales Islands rheotropic properties are often associated with a vesicular structure in the soil . This structure makes the soil appear to be perforated by small holes (Figure 20) . It is believed that this structure is caused by the slow freezing of saturated soils which results in minute ice crystals forming in the surface 20 cm . The thawing of the active layer in summer then leaves small holes in the soil ; since both rheotropy and vesicular structure are aided by high water and silt content the two phenomena are often associated, though not related .
However, vesicular structure does indicate lesser strength of the soil due to stable particle arrangement as the tendency is for the holes to become filled in . This type of structure is most often observed in Regosolic
Turbic Cryosol and Regosolic Static Cryosol with a high silt but low clay fraction .
6 .3 Earth Hummocks
Earth hummocks are common in Arctic Canada but they occur in areas of discontinuous permafrost as well . The term 'earth hummocks' is sometimes applied to relief forms created by the growth habits of some vegetation ;
strictly speaking, it should only be used to describe features that are
created by frost heaving and sorting alone (Washburn, 1958) . Part of the
confusion may be attributable to the concept that in some instances vegetation
plays an essential part in the inception of hummocks (Raup, 1965) . It is
believed that mosses growing on wet surfaces insulate the ground beneath
against solar heat ; this leads to uneven thermal conditions and ground frost
processes are affected, and non-uniform frost heaving is believed to account
for the doming of earth hummocks .
While the development of earth hummocks clearly relies on the action
of ground frost, it is doubtful whether vegetation cover is such an
indispensible part of the initiation stage . The freezing of materials of
non-uniform particle size alone will create the thermal heterogeniety
necessary for hummock inception . Mehuys, et al . (1975) showed that stones
in the soil can alter thermal conditions around them, thus creating
thermal gradients in the soil . Washburn (1969) also pointed out frost
heaving and sorting is in part due to the difference in thermal properties
between stones and finer materials . Well developed hummocks as high as
50 cm and having diameters of about 1 m have also been found on Somerset Is .
in an area that is totally barren . It appears that the occurrence of hummocks,
as opposed to other types of patterned ground, related more to the moisture
regime and the texture of the soil . Earth hummocks occur most often in
areas that are poorly drained as enough moisture must be available for
accumulation of a large amount of ice . Fine texture parent materials,
particularly marine silts and clays, are most suitable for hummock development .
The structure of earth hummocks have been sufficiently described
for the Mackenzie Valley area (Tarnocai, 1973 ; Zoltai and Tarnocai, 1973) .
10 2
In the study area, the morphology of earth hummocks are similar but the
tendency is for more gleying to occur in the lower horizons . An earth
hummock is described as follows (Fig . 21 & 22) :
Site : WZ21, 72° 58'N, 94° 57'W
L-H - 0 to 5 cm, discontinuous, black (lOYR 2/1, moist) litter of
partially decomposed mosses and grasses ; clear, irregular
boundary .
Omy - 5 to 10 cm, discontinuous, black (l0YR 2/1, moist) partially
decomposed organic matter ; clear, irregular boundary .
Bmy - 0 to 15 cm, discontinuous, dark brown (l0YR 4/3, moist) silt
loam, single grained, friable when moist, hard when dry ; clear,
smooth boundary .
BCgy - 15 to 40 cm, discontinuous, yellowish brown (l0YR 5/8, moist)
clay loam ; massive, firm when moist, hard when dry, distinct
mottles ; organic inclusions present ; clear, wavy boundary .
BCgyz - 40 to 53 cm, dark gray (l0YR 4/3) clay loam ; well-bonded
randomly oriented ice ; distinct mottles ; clear, wavy boundary .
Cz - 53 to 58 cm, black (l0YR 2/1) clay, well-bonded random oriented
ice ; clear, smooth boundary .
Omyz - 58 to 65 cm, black (l0YR 2/1) partly decomposed organic matter of
mostly mosses ; vein ice ; clear, smooth boundary .
IICZ - 65 cm plus, black (l0YR 2/1) clay ; well-bonded randomly oriented
ice .
The temperature profile of the hummock is presented in the Appendix,
Table 34 . Chemical and physical properties of the soil are comparable to those
of Site WZ2 listed in Table i2 of the Appendix .
Vegetation cover on this site is 100 percent . The species present are :
10 3
Figure 21 . Brunisolic Turbic Cryosol on marine-modified till (Site WZ21) . The lower right corner of the picture shows the top surface of the frost table .
' BCti,il ;
I ~. Omy I i ._ BCgy
BCgyz ~- Frost Table yf']-`Iyz Permofrost
2710 *ii0yrs. (BGS-336) ~~ 3000* 40yrs . (BGS - 335)
Figure 22 . Profile and 14C age determinations o£ WZ21 samples . 104
Carex spp .
Tomenthypnum nitens
Salix arcitca
Stereocaulon spp .
ErioQhorum triste
Aulacomnium turgidum
Hylocomium splendens
Cladonia spp .
Polyticum strictum
Arctogrostis latifolia
Poa arctica
6 .4 Organo Cryosols
Frozen organic soils occur throughout the Queen Elizabeth Islands
(Blake, 1974) . On Somerset and Prince of Wales Is . peat polygons occur in isolated pockets that are about 1 to 5 hectares in area . Organic soils mostly associate with river terraces but may also accumulate on marine deposits and fine texture colluvium . In all cases the external drainage conditions are poor due to feeding from streams or permanent snow banks .
Peat composed of mostly mosses accumulate to a depth of 1 .5 m in the Mid-
Arctic . However few, if any, of the remnants of these high-centered polygons (Zoltai, et al ., 1973) are actively accumulating peat any longer
(see Section 6 .6) ; in fact, all of them show signs of wind or stream erosion
(Fig .23 ) and in certain cases, the ice wedge in the polygon trough has completely melted . An example of a Glacic Mesic Organo Cryosol on glacio- marine fine sand is described as follows : 10 5
Figure 23 . Peat polygons eroded by the streams running among them . The snowbank in the background persists throughout the entire summer .
Figure 24 . Cryoturbation buries the Ahy horizon formed at the boundary of two small ice-wedge polygons . The dense vegetation cover along the boundary results from the better moisture supply of the depression .
106
Site : WZ10, 74 ° O1'N, 93 ° 27'W
Oh - 0 to 5 cm, dark yellowish brown (l0YR 3/4, moist) decomposed
peat ; loose ; clear, smooth boundary .
Om - 5 to 25 cm, dark yellowish brown (l0YR 2/2, moist) moderately
decomposed moss peat ; clear, smooth boundary .
Omz - 25 to 55 cm, dark yellowish brown (l0YR 2/2) moss peat, vein
ice ; clear, abrupt boundary .
Wz - 55 to 100 cm, ice with soil inclusions ; discontinuous ; clear,
abrupt boundary .
Cz - 100 cm plus, yellowish brown (l0YR 5/2) sand ; well-bonded ice
not visible .
Peat polygons in the study area are on the average 1 .5 m high and
3 to 4 m in diameter . In the above example, the height is 1 m and the
diameter is 3 .8 m . Laboratory analyses results of the peat are presented
in Table 35, Appendix . Moisture and temperature data are shown in Tables 36 & 37 .
Vegetation on peat polygons is quite distinctive . An example is given
here in which the total vegetation cover is 60 percent . On the polygon
itself the species present are :
Papaver lapponicum ssp . occidentale
Oxyria digyna
Juncus biglumus
Salix arctica
Cerastium alpinum
Draba corymbosa
Alopecurus alpinus
Pedicularis hirsuta
Melandrium apetalum
Saxifraga caespitosa
10 7
The species present in the trough areas are :
Alopecurus alpinus
Salix arctica
Melandrium apetalum
Ranunculus sulphureus
Polygonum viviparum
Hylocomium splendens
Practically all the peat deposits visited on Somerset Is . are in the
declining phase . Their occurrence in the High Arctic, therefore, indicate
warmer climatic conditions in the past . Surface and frozen peat samples
were collected for the purpose of 14C age determinations . The results
are discussed in Section 6 .6 .
6 .5 Soil Development and Chronology
As mentioned in Section 3 .4, the Pleistocene chronology of the northern
part of the study area is still unclear . Netterville, et al . (1976)
raised the possibility that this area was not ice covered during late or
even mid-Wisconsin times . With a few exceptions, soil studies in northern
Somerset do not yield results that elucidate Pleistocene chronology . On
the Paleozoic areas it is clear that weathered bedrock constituted
much of the unconsolidated material . It is equally obvious that at least
part of the parent material is till originated as erratics could be found
throughout the area . As bedrock is frost-shattered, it is brought to the
surface by frost heaving ; at the same time cryoturbation constantly buries
any till that is left on the surface . The result is a moderate to large
amount of angular stones in a fine texture matrix . Such a parent material
could have been deposited by glaciers during -late Wisconsin.:-or-it 108
could have been deposited earlier .
As far as the southern portion of the study area is concerned, chemical analyses of soil parent materials yield results which are consistent with the chronology described by Netterville, et al . (1976) . Ice movements from the southeast or the southwest would have covered the Precambrian areas with calcareous till such as found on SW Somerset . Netterville, et al . (1976) put a minimum date on an ice advance that began 30,000 yrs .
B .P . This ice is not considered to have covered northern Somerset Is .
The most illuminating piece of pedological information regarding
Pleistocene chronology lies in a detailed site in a Precambrian field of tors . The site is numbered W75R and its soil has been described in detail as an example of the Birmingham Bay Association . The pit was dug on the fines of non-sorted stone nets about 10 m from the center of a group of tors . The location is at the top of a 1 percent slope that extends 3 to 4 km to the northwest . Igneous and sedimentary erratics, generally of coarse gravel size, are found on the surface of the fines as well as among felsenmeer boulders . At 75 cm below the surface, a layer is encountered in which the material changes from non-calcareous to calcareous ; the clay content decreases while the silt content increases ; the color changes from yellowish brown to dark olive ; and the stone content decreases with depth .
The finding of a weakly to moderately calcareous layer beneath a non-calcareous layer is of considerable importance . The most plausible explanation is that the underlying layer is a calcareous till buried under the non-calcareous fines derived from the gneiss of the tors through prolonged weathering . Thus, the age of the buried till is relevant to the hypothesis of Netterville, et al . (1976) ; it should predate mid or late
109
Wisconsin times . If this hypothesis is true then the for fields can best
be explained as nunataks,which Washburn (1969) also invoked for shale tors
in eastern Greenland . The surface erratics could be frost-heaved from the
buried till . A difficulty in this explanation lies in the lack of any
signs of soil development in the non-calcareous layer . Despite the very
active mass wasting and cryoturbation, there should be some indications of
soil development in the profile .
An alternative explanation is that the entire profile represents
a well-developed soil on a very old till . The non-calcareous surface
75 cm could be considered as a very deep Bmy horizon from which all the
carbonates have been eluviated . Other differences in chemical and physical
properties are pedogenic . Despite the fact that high clay and stone contents
in the upper horizons is inconsistent with recognized trends the uniqueness
of cryogenesis must also be taken into account . If there is indeed only
one type of parent material, this profile would represent a mature soil
of the High Arctic environment . This explanation would also support the
hypothesis of an ice-free area during the Wisconsin Ice Age . Currently
mineralogical studies are being carried out on samples from this site for
comparison between upper and lower horizons .
6 .6 Radiocarbon Age Determinations
Samples obtained for radiocarbon dating on Somerset Island may be
divided into two groups, frozen organic materials buried by cryoturbation
collected at earth hummock sites and peat samples (frozen or otherwise)
collected at peat polygons . The samples were all canned in the field to
avoid the possibility of contaminations . Age determinations were done by
the Department of Geological Sciences of Brock University .
From the earth hummock samples it was learned that : (1) organic
materials were deposited, implying a favorable environment for growth
between 8,000 and 9,000 yrs . B .P ., (2) there is an indication of warmer
climatic conditions between 3,000 to 4,000 yrs . B .P . when the active layer
was deeper than at present, (3) cryoturbation is active today and has been
so for the past 3 ;000 years .
Evidence for the first conclusion is presented in Figure 22 .
This earth hummock occurs on marine-modified till at about 55 m a .s .l . Veins
of organic matter were frozen in the permafrost and samples were collected
along its length . The age determination for three samples were 9020 ± 120
yrs . (BGS-332), 8070 ± 110 yrs . (BGS-334) and 9480 ± 190 yrs . (BGS-333) .
These were the oldest of all the dates obtained and their closeness to the
accepted time of periglacial rebound shows that vegetation colonization of
new land was rapid at the time .
Other radiocarbon dates indicate that warmer climatic conditions
prevailed between 3,000 and 4,000 years ago than at present . Earth
hummocks, developed on fine textured marine deposits were excavated at
about 40 m a .s .l . in the Mid-Arctic Region . Cryoturbated organic materials
were taken from 5 to 20 cm below the well marked permafrost table,
yielding dates of 2710 ± 110 years (BGS-336) and 3,000 ± 90 years (BGS-335)
(Fig . 22) . At another hummock site, samples were obtained from cryoturbated
organic layers occurring within the seasonal frost, but above the assumed
permafrost table from beneath the central part and the edge of the hummock
A date of 3340 ± 140 years (BGS-331) was obtained from the
central part of the hummock, but the age under the edge was 525 ± 80 years
(BGS-330) . This indicates that cryoturbation occurred not only 3300 years
ago, but also in recent times . Surficial peat samples were collected from high centre polygons at two locations . The Cunningham Inlet location (74 ° O1'N and 93 ° 27'W) is an area of active peat accumulation ; although the'- polygon was raised some 1 m above the Drepanocladus fen it lacked peat forming vegetation .
A sample from 0 to 10 cm of the surface yielded a date of 1170 ± 80 years
(BGS-338) showing that peat was accumulating until recently . The second sample was taken from the top 30 cm of a high centre polygon in the Stanwell-
Fletcher basin above the apparent Holocene marine limit, at approximately
130 m a .s .l . (72° 58'N and 94° 57'W) . The age of surface peat from this highly eroded polygon was 6070 ± 100 years (BGS-337), indicating an early cessation of peat accumulation in this high centre polygon . Basal peat samples were also collected at these locations for radiocarbon date analysis by the GSC Radiocarbon Lab .
A final note must be made regarding the low elevation of site WZ8
(Fig . 25) and the unexpected old dates obtained there . Of several possible explanations, the most satisfactory one appears to .b e that the organic matter did not grow on the marine sedtment . However, the conclusion drawn on that determination still stands even if stratigraphic control is unclear . It should also be noted that the age determinations of this study are in general agreement with the studies of Blake (1964, 1970,
1974) who obtained dates of around 9,000 yrs . for buried organic matter in late Wisconsin stratigraphy .
6 .7 Vegetation Survival in the Arctic Environment
The survival of vegetation in arctic and alpine environments has been reviewed to some detail by Bliss (1971) . Plants that survive in the High and Mid-Arctic generally possess one or several of some typical morphological and physiological adaptations . Many arctic species have a high incidence 0 50cm
Bmy Bmy Of
Frost Table Cz
9020t 120 yrs. (BGS-332)
94803190 yrs. (BGS-333)
8070±110yrs. (BGS-334)
Figure 25 . Profile and 14C age determinations for Site WZ8 . of polyploidy (Packer, 1969 ; Johnson and Packer, 1965) . But it is still unresolved whether this is due to the wider genetical range favored by plants in the face of a harsh uncertain climate (Love and Love, 1957) or whether this is the result of the uniformity of the arctic environment propagating a few favored genotypes (Mosquin, 1966) . The compact growth forms of many species are also efficient means to reduce heat and water loss (Dennis and Johnson, 1970 ; Bliss, 1971) .
Opportunistic reproductive cycles and the ability to metabolize under low temperatures are also characteristics of arctic plants (Mosquin,
1966) . In general, the growth and reproductive strategies of arctic species emphasize the ability to survive rather than the ability to compete with other species .
A number of environmental factors have been named as limiting factors for arctic plant survival . Porsild (1951) considers that the major limiting factor in the polar desert is moisture and not low temperature . Bliss
(1971) mentioned nutrients as another factor that is deficient . Observations in the study area indicate all the known factors are indeed limiting ; yet, it is not possible to single out one or two factors as most limiting as it would lead to over-simplification . It appears that several limiting factors operate in High and Mid-Arctic ecosystems ; the release of one but not all of these factors will result in the establishment of a characteristic type of community (e .g . nitriphiles such as Xanthoria elegans and Festuca baffinensis ) . The release of one or several of the limiting factors brings about qualitative and quantitative improvements in the plant communities . But, the effect of each limiting factor is quite specific ; the release of a certain limiting factor under certain site conditions will
lead to predictable qualitative changes in the vegetation . Some of these
limiting factors are low temperature, lack of moisture, nitrogen deficiency
and excessive carbonate content of the soil .
6 .8 Vegetation and Cryoturbation
Since the early fiftyJs .studies have shown that the distribution
and perhaps survival of vegetation are affected by the frost processes in
the Arctic . Benninghoff (1952) and Hanson (1950) noted the instability of
the surface in Alaska affects the growth of vegetation . Recently Zoltai
(1975) demonstrated that periods of active soil movement may be discovered
in stress symptoms discovered in the annual rings of trees in the
Mackenzie Valley .
It is less certain, however, that the survival of short-lived
herbaceous species is threatened by cryoturbation (Fig 24) . Part of the problem
is the scarcity of quantitative information on the amount of movement taking
place . Perhaps the most relevant comments came from Hopkins and
Sigafoos (1950) who stated in their study in Alaska that"the concept
of a 'climax' vegetation must be modified when applied to tundra vegetation .
Disturbance of the substratum (due to cryoturbation) recurs repeatedly,
and all stages in the plant succession exist on unstable surfaces . The
vegetation in areas of patterned ground represents an equilibrium assemblege
adjusted to the climate in which it exists, but differs from a 'climax'
assemblage in that bare areas and areas covered by pioneer plants are
intimately mixed among areas covered by assemblages representing the highest
stable in plant succession" . In other words, vegetation-soils systems on
patterned ground are in equilibrium already ; thus, the artificial introduction
Figure 26 , Continuous carpet of mosses on a seepage slope in the High Arctic with an abundance of Ranunculus sulphureus .
Figure 27 . The vegetation cover on the darker Paleozoic sandstone surface is about 50%, whereas the limestone surface has less than 1% cover .
of vegetation to barren areas will not add an extra measure of stability
to the terrain ; but the outcome of such an endeavor would be contrary
to expectations .
6 .9 Vegetation Distribution and Petrology
In general, the occurrence of vegetation can be related to the
petrology of the substrate . On the whole the excessive carbonate content
of the Paleozoic and Proterozoic uplands have much poorer cover than the
Precambrian Shield and Tertiary sandstone areas . However, it must be
pointed out that the Precambrian surface is not always acidic, as all the
tills found were calcareous in reaction. Nevertheless, the dilution by
underlying Precambrian bedrock inevitably promotes better growth of
crustose and foliose lichens (Stereocaulon spp ., Cetraria cucullâta ,
Rhizocarpon geographicum) . A more striking example of this phenomenon
was seen in a site of Paleozoic sandstone surrounded by limestone (Fig . 27) .
This contrast may be detected in the analyses=of soil-parent materials as
seen in the following table .
Table 14 . Comparison between vegetation grown on Paleozoic sandstone and limestone .
Site Location 39A (73 ° 10'N, 92°12'W) 39B (73°10'N, 92°12'W) Bedrock Type limestone sandstone Soil Parent Material Textural Class loam loam Drainage Class well drained well drained Parent Material % CaCO3 Equiv . 54 .24 52 .32 % Calcite 47 .68 22 .38 Dolomite 6 .04 27 .58 % Plant Cover Estimate 1 50
Table 14 . (cont'd)
Species List Papaver lapponicum Saxifraga caespitosa ssp occidentale Thamnolia vermicularis Draba spp . Saxifraga oppositifolia Cerastium alpinum Papaver lapponicum Tharmnolia vermicularis . spp . occidentale Polyblastia spp . Poa arctica Cetraria cucullata Stereocaulon spp .
6 .10 Wildlife
There are observations on the wildlife of the study area that are
worth reporting . The most productive areas on Somerset Is . correspond to
the biologically sensitive environments identified in Section 7 , namely
these are Stanwell-Fletcher Basin, Creswell Basin, Cunningham Inlet and the
Union River area . The entire Prince of Wales Is . i s quite productive except
for the northeastern uplands . Somerset Is . has been devoid of muskoxen
for nearly a century following indiscriminate slaughter by whalers
(Richard Russel, personal communication) . However, a herd of twelve
muskoxen (Ovibus moschatus) including calves, was sighted first in July
west of Stanwell-Fletcher Lake and then again in August in the Union River
area . It is safe to say this herd is the only one on Somerset, in contrast
to the fairly large population on Prince of Wales Is .
On Somerset, the most frequent sightings of barren ground caribou
(Rangifer groelandicus ) occurred in the valley north of Stanwell-Fletcher
Lake and in West Creswell River Basin ; perhaps this is where they congre
gate in July after moving off the known calving grounds along the west coast .
Caribou were also sighted throughout Prince of Wales Is . ; the animals
seem to favor upland locations during August . A herd of up to 100 animals,
possibly Peary's caribou (Rangifer ep aryi) sighted east of Allen Lake was
the largest herd encountered.
7 . RECOMMENDATIONS
7 .1 Sensitive Environments
Sensitive environments exist where a disturbance would induce an
environmental reaction of such magnitude that it is out of proportion to
the initial disturbance . In a highly sensitive environment a relatively
minor disturbance could cause a severe reaction, but in a less sensitive
environment the same disturbance would cause only a mild reaction . The
sensitivity of the terrestrial environment examined in this report may be
due to the characteristics of the terrain, the vegetation covering the
terrain, or a combination of these . Reactions primarily attributable to
the characteristics of the terrain are referred to as terrain sensitivity
(Van Eyk and Zoltai, 1975) . Terrain sensitivity is dependent on character-
istics inherent in the ecosystem, for example, ice content either near the
surface or at depth, slope angle, the properties of surficial material,
and vegetation insulating cover are all relevant factors . Other sensitive
environments may be unique habitats for vegetation and wildlife, or habitats
which. are keys to the perpetuation of these populations .
During this study, certain processes were noted which may contribute
to the sensitivity of the environment to disturbance . These are listed
below with actions recommended to minimize their impact .
7 .11 Tabular ground ice was found in certain areas on both islands
in association with retrogressive thaw flow-slides (Figure 28) . In these
features about 1 m of active layer or permafrost low in ice-content rested
on large masses of ground ice . The thickness of exposed ground ice was
about 1 m; this ice was melting at a fairly fast rate and releasing large
quantities of water (Figure 29) . Much of this sediment-rich water reached
nearby streams causing much sedimentation . The occurrence of tabular ice
C.Anne
C Clarence
wc
Brenlford Boy oc
C.Swinburne
20 40 Figure 28. Sensitive terrain the study area . Kilom o ires 0 _r0 i,n 9 20 stotute Mllos 44 Active or stabilized thaw flow-slides . ® Mass wasting caused by disturbance in active layer . Figure 29 . Tabular ground ice exposed in a retrogressive thaw flow- slide in marine sediments (73 ° 37'N, 94° 0$'W) .
Figure 30 . Winter road constructed in the spring of 1975 . Note soil exposed by scalping on the left side, and vegetation debris in the middle . Active layer was 10 percent deeper under scalped area by early August, 1975 .
12 2
exposures were associated with fine texture marine sediments or till which
was modified by marine inundation . It is not known whether tabular ground
ice can exist in a stable state naturally . The only known occurrences are
those exposed by thermal erosion .
Recommendation 1 :
Disturbance of the surface over tabular ice bodies should be avoided
to prevent-the development of retrogressive thaw flow-slides and
attendant sedimentation of water bodies .
7 .12 Moss vegetation cover, however thin, serves an an insulation
of the frost table . Similarly, an active layer low in moisture content also
insulates the underlying permafrost . The combined insulating effects of
vegetation cover and active layer determine the depth of thaw during the
summer period . If the vegetation cover or the active layer are disturbed
by stripping, compaction, churning by wheels or by other means, their
insulating qualities will be reduced and deeper thawing will result
(Fig . 30) . This will lead to the melting of near-surface permafrost,
causing subsidence or thermokarst development . If the shape of the impact
is linear (e .g . vehicle tracks, seismic lines, winter roads, etc .) the
channel created by newly depressed permafrost table will carry subsurface
drainage water, and the subsided ground surface will channel the surface
runoff . Depending on the nature of surficial materials and the slope
angle, gullying can become the end result . This can be a serious problem
on ice-rich and erosion prone materials such as fine texture marine
sediments or till which is low in stone content .
Recommendation 2 :
Disturbance of the surface vegetation and active layer should be
avoided as much as possible on fine texture soil parent materials .
123
7 .13 Uplifting of rocks by frost heaving was noted on crystalline
bedrock areas . In one instance a 2 m x 2 m bedrock block was lifted 1 m
above the glacially smoothed bare bedrock surface . Examination showed that
cracks had developed in the bedrock along natural jointing, and water
seeping into the cracks eventually lifted the bedrock boulder upon freezing .
Should blasting create or enlarge cracks in solid bedrock, the process
described above could be artificially induced, causing disruptive actions
on roads, pipelines or buildings . The possibility of rock heaving after
blasting should be tested under field conditions .
Recommendation 3 :
Blasting of solid crystalline bedrock may induce frost heaving .
This effect should be investigated and construction design should
accommodate the findings of these studies .
7 .14 Mass wasting of the active layer is very common even on gentle
slopes . The development of sorted and non-sorted stripes mark such locations
as circular forms of patterned ground are elongated by downslope movement .
Flow rates of 1 cm to 2 cm per year were measured on Banks Island in
relatively coarse texture material on dry sites ('French, 1974, 1976) .
This implies a volumetric downslope movement of 30 cm3 /cm/yr . Actual rates
of movement depend on the nature of soil materials and the active layer
moisture regime during the summer ; the rate of movement is higher on wet
to moist fine texture materials .
It is probable that linear structures running parallel to the contour
will interfere with the downslope movement of mass wasting . Structures
built on roadbeds or foundations (berms, roads, etc .) may be moved
differentially by the downslope flow . Structures built on piles or stilts 12 4
may be subjected to increasing pressures . Permafrost table raised artificially
(i .e . under roadbeds, over chilled pipelines) may impede the mass wasting of the active layer, and the pressures which build up against structures may lead to their eventual destruction ; moreover, the ensuing repair operations can cause further terrain damages . This aspect of the active
layer solifluction should be the subject of further studies .
Recommendation 4 :
Natural mass movements occurring as active layer downslope flow may
be impeded by artificial structures and the resultant pressures are
potentially disruptive . The effects of mass movements on structures
should be studied and construction methods should be based on the
results of such studies .
7 .15 Many soils with high silt and moisture contens show rheotropic
characteristics . Mechanical vibrations such as those which may be produced
by vehicle traffic, compressor stations, and the vibration of the pipeline
may be sufficient to cause the active layer to turn into a fluid state .
This will lead to damage to structures, and the permafrost may also thaw
out because of the change in thermal regime . Moreover, some of the soil
materials under plastic flow may reach water bodies, thereby causing
sedimentation and damaging the aquatic environment . The rheotropic
phenomenon, common on the two islands investigated, should be studied from
soil mechanics point of view . Data on the rheotropic properties of these
soils will be reported by the staff of Geological Survey of Canada .
Recommendation 5 :
Rheotropic soils may turn into a fluid state as a -.result of
mechanical vibrations . Construction methods to overcome this
phenomenon should be developed based on field tests . 125
7 .16 Extensive well vegetated areas suitable to sustain musk oxen populations are limited . Such areas are in Ecological Districts H3, M6 and M5 on Somerset Island, and Districts H5 and 145 on Prince of Wales Island .
These are generally areas of marine sediments or areas underlain by
Tertiary bedrock . Other unique habitats which have been identified by wildlife biologists are Prince Leopold Island (seabird habitat) and the rugged Precambrian areas of Somerset Is . (barren-ground caribou habitat) .
Disturbance to these areas may lead to the displacement of these animals which may threaten their survival .
Recommendation 6 :
Interference with unique areas which are vital for the survival
of wildlife should be avoided . 8 . CONCLUSIONS
A reconnaissance of Somerset and Prince of Wales Islands have revealed aspects of the environment of these islands which are unique and deserve deeper investigations . The richness of wildlife resource both in the High and Mid-Arctic is a cause for much concern . Protection and management of these animals are essential to the preservation of the character of these islands . Certain factors and processes which affect terrain sensitivity have already been identified as relevant to pipeline construction . The function of vegetation and the active layer as insulation layers for the permafrost must not be interferred with to any great extent .
Natural processes of frost heaving, rheotropism, thermokarst and mass- wasting are also critical factors ; extreme caution must be exercised in
constructing where these processes are known to be active .
From another viewpoint, the study, area is - also unique in that it stores
for the inquiring mind a number of scientific problems . Geologically,
the intriquing question of the glacial history of Somerset Is . remains unresolved . Related to this problem is a pedological one of achieving a better understanding of the process of cryogenesis . There are some
indications that these two questions may be resolved by some common key .
If it can be shown that soil development has not been interrupted by
glaciation for a long period then those soils would represent fully mature soils developed in a High Arctic environment . It is hoped that further studies in geology and: pedelogy -wiilï-enrich the knowledge of either discipline .
12 7
9 . REFERENCES
1 . Andrews, J .T . 1970 . Present and postglacial rates of uplift for glaciated northern and eastern North America derived from postglacial uplift curves . Can . J . Earth Sc . 7 :703-715 . 2 . Anonymous . 1963 . A report of the physical environment of northern Baffin Island and adjacent areas, Northwest Territories, Canada . Geog . Dept ., McGill Univ . Rand Corporation Memorandum BM-2706-1-PR, 302 p ., Santa Monica, Calif . 3 . Atkinson, H .J ., G .R . Giles, A.J . MacLean and J .R. Wright . 1958 . Chemical methods of soil analysis . Contrib . No . 169 (rev .) . Chem. Div ., Sci . Serv ., C .D .A., Ottawa. 90 p . 4 . Barnett, D .M ., L .A . Dredge and S .A. Edlund. 1976 . Terrain inventory : Bathurst, Cornwallis and adjacent islands, Northwest Territories . Geol . Surv . Can . Paper 76-1 . 5 . Benninghoff, W .S . 1952 . Interaction of vegetation and soil frost phenomena . Arctic 5 (1) :34-44 . 6 . Blackadar, R .G . 1967 . Precambrian geology of Boothia Peninsula, Somerset Is . and Prince of Wales Is ., District of Frankon . Geo . Surv . Can . Bull . 151 . 7 . Blake ; Jr ., W . 1964 . Preliminary account of glacial history of Bathurst Is ., Arctic Archipelago . Geo . Surv. Can . Paper 64-30 . 80 p . 8 . Blake, Jr ., W . 1970 . Studies of glacial history in Arctic Canada . I . Pumice, radiocarbon dates, and differential postglacial uplift in eastern Queen Elizabeth Is . Can . J . Earth Sci . 7 :634-664 . 9 . Blake, Jr ., W . 1974 . Studies of glacial history in Arctic Canada . II . Interglacial peat deposits on Bathurst Is . Can . J . Earth Sci . 11(8) :1025-1042 . 10 . Bliss, L .C . 1971 . Arctic and alpine plant life cycles . Ann . Rev . of Ecol . and Syst . 2 :405-38 . 11 . Bliss, L .C ., G .M. Courtin, D .C . Pattie, R .R . Pieive, D .W .A . Whitfield, P . Widden . 1973 . Arctic tundra ecosystems . Ann . Rev . Ecol . and Syst . 4 :339-399 . 12 . Brassard, G .R . 1967 . A contribution to the bryology of Melville Is ., N .W .T . Bryologist 70 :347-51 .
12 8
13 . Brassard, G .R . and W .C . Steere . 1968 . The mosses of Bathurst Is ., N .W .T ., Canada . Can . J . Bot . 46 :367-83 . 14 . Chesnin, L . and C .H . Yieu . 1950 . Turbidimetri c determination of available sulphates . Soil Sci . Soc . Am . Proc . 15 :149-151 . 15 . Cook, F .A . and V .G . Raiche . 1962 . Freeze-thaw cycles at Resolute, N .W .T . Geog . Bull . 18 :64-78 . 16 . Craig, B .G . 1963 . Surficial geology of Boothia Peninsula and Somerset, King William and Prince of Wales Is ., District of Franklin . Geo . Surv . Can . Paper 63-44 . 17 . Cruickshank, J .G . 1971 . Soils and terrain units around Resolute, Cornwallis Island . Arctic 24 :195-209 . 18 . Danks, H .V . and J .R. Byers . 1972 . Insects and Arachnids of Bathurst Is ., Canadian Arctic Archipelago . Can . Ent . 104 :81-88 . 19 . Day, P .R . 1965 . Particle fractionation and particle-size analysis . In : Methods of soil Analysis . C .A . Black, et al . (eds .) . Am. Soc . Agron . Monog . No . 9, p . 545-467, Madison, Wisc . 20 . Dennis, J .G . and P .L . Johnson . 1970 . Shoo t and rhizome-root standing crops of tundra vegetation at Barrow, Alaska . Arctic and Alpine Res . 2(4) :253-66 . 21 . Downes, J .A . 1964 . Arctic Insects and their environment . Can . Ento- mologist 96 :279-307 . 22 . Fadorova, N .N . and E .A. Yarilova . 1972 . Morphology and genesis of prolonged seasonally frozen soils of western Siberia . Geoderma 7 :1-13 . 23 . Fraser, J .K . 1959 . Freeze=thaw frequencies and mechanical weathering in Canada . Arctic 12(1) :40-53 . 24 . French, H .M . 1974 . Mass-wasting at Sochs Harbour, Banks Island, N .W .T ., Canada . Arctic and Alpine Res . 6 :71-78 . 25 . French, H .M . 1976 . Geomorphological process and terrain disturbance studies, Banks Island, District of Franklin . Geo . Surv . Can . Paper 76-lA:289-292 . 26 . Frontier, Y .O ., et al . 1963 . Geology of the north-central part of the Arctic Archipelago, Northwest Territories (Operation Franklin) . Geo . Surv . Can . Memoir 320 .
129
27 . Graham, E .R . and P .L . Lopez . 1969 . Freezing and thawing as a factor in the release and fixation of soil potassium as demonstrated by isotopic exchange and calcium exchange equilibria . Soil Sc . 108 (2) :143-147 . 28 . Greweling, T . and M . Peech . 1965 . Chemical Soil Tests . Cornell Univ . Agr . Exp . Sta. Bull . 960(rev .) 47 p . 29 . Hanson, H .C . 1950 . Vegetation and soil profiles in some solifluction and mound areas in Alaska . Ecol . 31(4) :606-630 . 30 . Hill, D .E . and J .C .F . Tedrow. 1961 . Weathering and soil formation in the Arctic environment . Am . J . Sc . 259 :84-101 . 31 . Hills, G .A . 1960 . Regional site research . Forestry Chron . 36 :401-23 . 32 . Hindle, W . 1975 . Piping arctic gas south via Hudson Bay . Can . Geog . J . 90 :14-17 . 33 . Hinman, W .C . 1970 . Effects of freezing and thawing on some chemical properties of three soils . Can . J . Soil Sc . 50 :179-182 . 34 . Hoekstra, P . 1969 . Water movement and freezing pressures . Soil Sci . Soc . Am . Proc . 33 :512-518 . 35 . Hopkins, D .M . and R .S . Sigafoos . 1950 . Fros t action and vegetation patterns on Seward Peninsula, Alaska . U .S . Geo . Surv . Bull . 974-C :51-101 . 36 . Ivanova, E .N . 1963 (ed .) . Soils of Eastern Siberia . Translated from Russian . 223 p . Israel Program for Scientific Translation, Jerusalem . 1969 . 37 . Jackson, M .L . 1958 . Soil chemical analysis . Prentice-Hall, N .J . 498 p . 38 . Johnson, A .W . and J .K . Packer . 1965 . Polyploidy and environment in Arctic Canada . Science 148 :237-39 . 39 . Kerr, J .W . and R .L . Christie . 1965 . Tectonic history of Boothia Uplift and Cornwallis Fold Belt, Arctic Canada. Am . Assoc . of Precamb . Geo . Bull . 49(7) :905-26 . 40 . Kersaw, K .A . 1973 . Quantitative and dynamic plant ecology . 308 p . 2nd edit . Edward Arnold, London . 41 . Kiger, R .W . 1975 . Papaver in North America north of Mexico . Rhodora 77 :410-422 .
13 0
42 . Lacate, D .S . 1969 . Guidelines for biophysical land classification . Can . Forest . Serv . Publ . No . 1264, 61 p . 43 . Liverovskaya-Kosheleva, I .T . 1965 . The problem of thixotropy of soils in the tundra zone . Translated from Russian . Problems of the North 8 :241-255 . 44 . Love, A . and D . Love . 1957 . Arctic polyploidy . Proc . Genet . Soc . Can . 2 :23-27 . 45 . McMillan, N.S . 1960 . Soils of the Queen Elizabeth Islands . J . Soil Sci . 11 :131-9 . 46 . Mehuys, G .R ., L .H . Stolzy and J . Letey . 1975 . Temperature distributions under stones submitted to a diurnal heat wave . Soil Sc . 120(6) : 437-159 . 47 . Mills, G .F ., C . Tarnocai and C .F . Shaykewich . 1974 . Soil temperature studies in Manitoba . In : Papers presented at the 8th Manitoba Soil Science Meeting (not published) . 48 . Mitchell, R.H . 1975 . Geology, magnetic expression and structure control of the Central Somerset Is . kimberlites . Can . J . Earth Sc . 12 : 757-764 . 49 . Mosquin, T . 1966 . In : The evolution of Canada's flora . Ed . R.L . Taylo r and R.A. Ludwig . U of T Press, Toronto, 137 p . 50 . Netterville, J .A ., A .S .-Dyke, R .D . Thomas and K .A . Drabinsky . 1976 . Terrain inventory and Quaternary geology, Somerset, Prince of Wales and adjacent islands . Geo . Surv . Can . Paper 76-lA :145-154 . 51 . Pack;;~.r, J .G . 1969 . Polyploidy in the Canadian Arctic Archipelago . Arctic and Alpine Res . 1 :15-28 . 52 . Pawluk, S . and R . Brewer . 1975 . Micromorphological and analytical characteristics of some soils from Devon and King Christian Islands, N .W .T . Can . J . Soil Sci . 55 :349-361 . 53 . Peech, M . 1965 . Hydrogen-ion activity . In : Methods of soil analysis . C .A . Black, et al . (eds .) . Am . Soc . Agro . Monog . No . 9, p . 914-926, Madison, Wisc . 54 . Pettapiece, W .W . 1974 . A hummocky permafrost from Sub-Arctic of north- western Canada and some influences on fire . Can . J . Soil Sc . 54 :343-355 . 55 . Polunin, N . 1948 . Botany of the eastern Canadian Arctic . II . vegetation and ecology . Nat . Mus . Can . Bull . 104 . 56 . Poole, R .W . 1974 . An introduction to quantitative ecology . 532 p . McGraw-Hill . 57 . Porsild, A .E . 1951 . Plant life in the Arctic . Can . Geog . J . 42(3) : 121-145 . 58 . Porsild, A .E . 1964 . Illustrated flora of the Canadian Arctic Archipelago . 2nd edit . Nat . Mus . Can . Bull . 146 . 21 8 p . 59 . Raup, H .M. 1965 . The structure and development of turf hummocks in the Mesters Vig District, Northeast Greenland . Meddelelser Om Gronland 166(3) :122 p . Reitzels Forlag, Copenhagen . 60 . Rae, R .W . 1951 . Climate of the Canadian Arctic Archipelago . Can . Dept . of Transport, Toronto . 61 . Richards, L .A . (ed .) . 1954 . Diagnosis and improvement of saline and alkali soils . U .S .D .A . Agr . Handbook 60, 160 p . Washington, D .C . 62 . Riewe, R .R . 1972 . Preliminary data on mammalion carnivores including man in the Jones Sound Region, N .W .T . In : Devon Island I .B .P . Project Rept . 1970 & 1971 . ed . L .C . Bliss, U . of Alberta, Edmonton, 413 p . 63 . Rohmer . 1973 . The arctic imperative . 224 p . McClelland & Stewart, Toronto . 64 . Savile, D .B .O . 1959 . The botany of Somerset Island, District of Franklin . Can . J . Bot . 37 :959-1002 . 65 . Savile, D .B .O . 1961 . The botany of the Northwestern Queen Elizabeth Islands . Can . J . Bot . 39 :904-942 . 66 . Schofield, W .B . and Cody, W .J . 1955 . Botanical investigations on coastal southern Cornwallis Island, Franklin District, N .W .T . Can . Field Nat . 69 :116-128 . 67 . Skinner, S .I .M ., R .L . Halstead and J .E . Brydon . 1959 . Quantitative manometric determination of calcite and dolomite in soils and lime- stones . Can . J . Soil Sc . 39 :197-204 . 68 . Smith, D .I . 1972 . The solution of limestone in an Arctic environment . In : Polar geomorphology . eds . R .J . Price & D .E . Sugden . Inst . Brit . Geog . Special Publ . #4, 215 p . 69 . Sutton, G .M . 1971 . High Arctic - an expedition to the unspoiled north . Eriksson, N .Y . 116 p .
13 2
70 . Tarnocai, C . 1972 . Some characteristics of cryic organic soils in northern Manitoba. Can . J . Soil Sc . 52 :485-496 . 71 . Tarnocai, C . and A .N . Boydell . 1975 . Biophysical study on the Boothia Peninsula and Northern Keewatin . Geol . Surv . Can . Paper 75-1, Part A. p . 423-424 . 72 . Tarnocai, C ., W .W . Pettapiece and S .C . Zoltai . 1973 . Repor t on Cryoturbed Soils in Northern Canada . In : Proc . Ninth Meeting Can . Soil Surv . Comm. p . 96 . ed . J .H . Day, P .G . Lajoie, Univ . of Sask ., Saskatoon . 73 . Tedrow, J .C .F. 1962 . Morphologica l evidence of frost action in arctic soils . Biuletyn Peryglacjalny 11 :343-391 . 74 . Tedrow, J .C .F . 1966 . Polar desert soils . Soil Sci . Soc . Am. Proc . 30 :381-387 . 75 . Tedrow, J .C .F . 1964 . Soils of the High Arctic landscape . In : Polar Deserts and Modern Man . ed . T .L . Smiley & Z .H . Zumberge . Univ . of Arizona Press, Tuscon . 76 . Tedrow, J .C .F . and J . Brown . 1962 . Soils of the Northern Brooks Range, Alaska : weakening of the soil-forming potential at High Arctic altitudes . Soil Sc . 93 :254-261 . 77 . Tedrow, J .C .F . and J .E . Cantlon . 1958 . Concept s of soil formation and classification in arctic regions . Arctic 11 :166-79 . 78 . Tedrow, J .C .F . and L .A . Douglas . 1964 . Soi l investigations on Banks Is . Soil Sc . 98 :53-65 . 79 . Tener, J .S . 1963 . Queen Elizabeth Is . game survey, 1961 . Can . Wildl . Serv . Occasional Paper 414 . 80 . Thannheiser, D . 1972 . New plant records from Boothia,Isthmus and King
William Is ., N .W .T ., Canada . Polarforschung 42(1) :50-55 .
81 . Thomson, J .W . 1972 . Distribution patterns of American Arctic lichens .
Can . J . Bot . 50 :1135-1156 .
82 . Tuke, M .F ., D .L . Dineley and B .R . Rust . 1966 . The basal sedimentary rocks
in Somerset Is ., N .W .T . Can . J . Earth Sc . 3(5) :697-711 .
83 . Van Eyk, D .W . and S .C . Zoltai . 1974 . Terrain sensitivity, Mackenzie
Valley and northern Yukon . Environmental-Social Program, Task
Force on Northern Oil Development Rept . 74-44, Queen's Printer .
Maps .
13 3
84 . Veillette, J .J . 1976 . Assessment of terrain performance, Somerset and
Prince of Wales Is . Geo . Surv . Can . Paper 76-lA :281-282 .
85 . Washburn, A .L . 1958 . Classification of patterned ground and review of
suggested origin . Geo . Soc . Am . Bull . 67 :823-66 .
86 . Washburn, A .L . 1969 . Weathering, frost action, and patterned ground in
the Mesters Vig District, Northeast Greenland . Meddelelser om
Gronland 176(4) :303 p . Reitzels Forlag, Copenhagen .
87 . Yong, R .N . and B .P . Warkentin . 1975 . Soil properties and behavior .
Elsevier, N .Y .
88 . Zoltai, S .C . 1975 . Tree ring records of soil movement on permafrost .
Arc . & Alp . Res . 7(4) :331-340 .
89 . Zoltai, S .C . and W .W . Pettapiece . 1973 . Terrain, vegetation and permafrost
relationships, northern Mackenzie Valley and Yukon . Task Force on
Northern Oil Development Rept . 73-4, 105 p . Info . Can . Cat . No .
R72-7973 .
90 . Zoltai, S .C ., F .C . Pollett, J .K . Jeglum and G .D . Adams . 1973 . Developing
a wetland classification for Canada . 4th North Am . For .. Soils Conf .
1973, Quebec, 20 p . A P P E N D I X Table 1 . A Modified Domin Scale .
Domin No .
Cover about 100% 10
Cover >75% 9
Cover 50-75% 8
Cover 33-50% 7
Cover 25-33% 6
Abundant, cover 10-25% 5
Abundant, cover 5-10% 4
Scattered, cover small 3
Isolated, cover small 2
Barren 1
Table 2 . Chemical and physical analyses ;, Batty Bay Association
Site : W-37 Location : 73 ° 05'N & 91°30'W Chemical Characteristics
Exchangeable Cations Conduc- % % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C P N03-N m .e .j ppm ppm Hor . cm pH mhos/cm equiv . cite mite C N ratio Cat+ Mg 2+ K+ Na+ 100 g
Cy 0-49 8 .2 0 .37 56 .63 42 .0 13 .5 0 .3 0 .02 15 .0 4 .7 22 .8 2 .8 0 .5 0 .1 2 .2 0 .5
Cz 49+
Chemical Characteristics Particle Size Characteristics
o Soluble Salts Sand Fraction ' ppm in saturation extract Depth % Total/ % % Textural Hor . Cm I Stone Ca Mg Na K C1 S04-S .C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Cy. 0-49 37 .8 17 .5 12 .7 6 .1 4 .6 23 .3 0 .0 0 .2 0 .1 0 .1 0 .2 0 .4 1 .0 58 .9 40 .1 SiClay
Cz
Table 3 . Chemical and physical analyses, Birmingham Bay Association
Stte : W-75R Location : 72 ° 51'N & 92°33'W Chemical Characteristics
Exchangeable Cations % Conduc- % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e ./ 2+ 2+ + Na+ ppm ppm 100 g Ca Mg K
Cy 0-50 6 .7 0 .3 ------
ICz 50-75 7 .2 1 .1 Tr . -- --
IICz 75-10 7 .8 2 .0 5 .5 2 .3 2 .9
IIC z 05-11 7 .6 . 2 .4 3 .0 2 .5 0 .5
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction ppm in saturation extract Z Depth Total % % Textural Hor . Stone Ca Mg Na K C1 S04-SI V .C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Cy' 0-50 110 19 .1 13 .6 14 .4 14 .4 10 .3 71 .8 14 .6 13 .6 SLoam
ICz 50-75 29 13 .4 15 .1 15 .6 15 .3 11 .5 70 .9 19 .0 10 .1 SLoam
IICz 75-10 5 5 .9 5 .1 10 .9 21 .7 18 .8 62 .4 29 .3 8 .3 SLoam IIC z 105-11~ L7 8 .5 7 .1 10 .2 16 .4 18 .4 60 .6 30 .6 8 .8 SLoam
Table 4 . Chemical and physical analyses, Cape Garry Association
Site : W-119B Location : 72°54'N & 93°29'W Chemical Characteristics
Exchangeable Conduc- % % % % % Cations Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P 1103-N m Ca 2+ ppm ppm Hor . cm pH nmhos/cm equiv . cite mite C N ratio .e ./ fig 2+ K+ Na+ 100 g
Cly 0-15
C2y 15-51 8 .2 0 .69 58 .36 14 .5 40 .4 0 .3 0 .04 7 .5 3 .6 23 .9 1 .6 0 .1 0 .1 1 .1 6 .0
Cz 51+
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction 7 ppm in saturation extract Depth o Total % Textural Hor . Stone On Ca Mg Na K Cl S04-S V .C .S . C . S . M.S . F .S . V .F .S. Sand Silt Clay Class
C -y 0-15
C y 15-51 86 .8 22 .4 18 .4 4 .8 91 .1 25 .5 0 .0 0 .0 0 .2 1 .7 16 .7 18 .8 37 .4 49 .8 12 .8 Loam
Cz 51+ Association Table 5 . Chemical and physical analyses, Cape Granite
Site : W-77a Location : 73° 40'N & 95°30'W Chemical Characteristics
Exchangeable Cations Avail . % / / / / m .e ./100 gm Conduc- P N03-N Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . K+ Na+ ppm ppm Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e / Ca t+ Mg 2+ 100 g 0 .5 0 .06 10 .0 10 .0 7 .2 4 .6 0 .1 0 .04 3 .4 Cy 0-52 6 .7 0 .11 ------0 .6
Cgy 52-64
Cz 64+
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction ppm in saturation extract % Depth % Total Textural Hor . cm Stone Sand Silt Clay Class Ca Mg Na K C1 S04-S V .C .S . C . S . M .S . F .S . V .F .S.
Cy 0-52 7 .8 5 .4 5 .3 0 .9 3 .2 7 .0 117 .7 7 .1 14 .3 13 .4 18 .0 12 .5 65 .3 15 .3 19 .4 SLoam
Cgy 52-64
Cz 64+
Table 6 . Chemical and physical analyses, Creewell Association
Site : W-23 Location : 72 ° 47'N & 92°58'W Chemical Characteristics
o Exchangeable Cations Conduc- % % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- -Org . Total C/N C .E .C . P N03-N Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e ./ Ca2+ 2.+ K+ Na+ ppm PPM 100 g fig
Ahy 0-15
Bmy 0-35
Omy 10-25
Cy 0-35 8 .0 0 .31 48 .99 17 .8 28 .7 1 .3 0 .09 14 .4 6 .0 21 .5 1 .7 0 .1 0 .01 1 .0 0 .0
Cz 35±
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction . ppm in saturation extract : Depth % Total % % Textural Stone Hor . cm Ca Mg Na K C1 S04-S .CA . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Ahy 0-15
Bmy 0-35
Omy 10-25
Cy 0-35 59 .5 10 .6 5 .1 0 .7 4 .6 14 .0 0 .0 0 .1 0 .2 0 .6 4 .7 25 .3 30 .9 52 .0 17 .1 SiLoam
Cz 35+
Table 7 . Chemical and physical analyses, Elwin River Association
Site : W-32 Location : 73 ° 23'N & 92°55'W Chemical Characteristics
e Exchangeable Cations Conduc- % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Hor . cm pH hos/cm equiv . cite mite C N ratio m .e ./ C12+ Mg t+ K+ ppm PPM 100 g Na+
Bmj 0-22 7 .8 0 .48 24 .27 5 .5 17 .3 1 .5 0 .1 15 .0 11 .7 19 .9 3 .2 0 .3 0 .02 2 .0 8 .0
Cy 22-37 7 .0 0 .34 27 .82 6 .6 19 .5 1 .3 0 .1 13 .0 11 .2 23 .3 3 .0 0 .3 0 .02 2 .5 0 .3
CZ 37+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction ppm in saturation extract % Depth Total % % Textural Hor . Stone cm Ca Mg Na K C1 S04-S .C .S . C .S . M .S . F .S . V.F .S.Sand Silt Clay Class
Bmj 0-22 82 .5 13 .9 3 .0 2 .8 3 .6 10 .6 8 .5 2 .7 3 .4 4 .5 9 .5 16 .3 36 .4 40 .4 23 .2 Loam
Cy 22-37 57 .5 11 .3 3 .1 4 .0 3 .6 9 .9 4 .2 1 .4 2 .3 3 .5 9 .3 19 .0 35 .5 42 .5 22 .0 Loam
Cz 37+
Table 8 . Chemical and physical analyses, Fearnall Bay Association
Site : W-73 Location : 72°51'N & 92°33'W Chemical Characteristics
e Exchangeable Cations Conduc- % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N mite C N ratio m . e ./ Ca 2+ K+ Na+ ppm Hor . cm pH nmhos/cm equiv . cite tig 2+ PPM 100 g
Bmj 0-12 7 .9 1 .3 45 .59 12 .2 30 .7 0 .9 0 .09 10 .0 5 .7 21 .6 1 .7 0 .1 0 .04 1 .2 8 .5
Cy 12-55 8 .1 0 .6 47 .63 17 .9 27 .4 0 .7 0 .06 12 .0 5 .4 22 .5 1 .8 0 .1 0 .03 1 .3 1 .0
Cz 55+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fractionaction % ppm in saturation extract Depth % t Total / Textural Hor . cm Stone Ca Mg Na K C1 S04-S V .C .S . C . S . M . S . F .S . V .F .S.Sand Silt Clay Class
Bmj 0-12 448 .8 37 .1 11 .5 2 .1 270 .5 120 .0 3 .4 2 .2 1 .9 3 .9 15 .0 19 .3 42 .3 38 .1 19 .6 Loam
Cy 12-55 89 .8 19 .3 7 .6 2 .6 86 .9 33 .0 1 .5 1 .0 2 .1 4 .1 15 .0 21 .1 43 .3 37 .61 19 .1 Loam
Cz 55+
Table 9 . Chemical and physical analyses, Fiona Lake Association
Site : W-60 Location : 73 ° 32'N & 95°24'W Chemical Characteristics
Exchangeable Cations ° ° Conduc- ° m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e ./ Ca 2+ K+ Na+ ppm ppm . 100 g F1g 2+
Ahy 0-9
Bmy 9-19
ICY 19-83 8 .0 0 .29 17 .29 10 .3 6 .4 0 .9 0 .03 30 .0 11 .9 27 .9 2 .5 0 .2 0 .03 1 .1 0 .5
IICy 83-89 7 .6 0 .14 0 .00 0 .0 0 .0 0 .3 0 .02 15 .0 6 .9 5 .7 2 .5 0 .2 0 .03 1 .6 0 .5
IICyz 89+.
Chemical Characteristics Particle Size Characteristics Soluble Salts ° Sand Fr action ppm in saturation extract Depth Total % % Textural Hor . cm Stone Ca' Mg Na K Cl S04-S V .C .S . C . S . M .S . F .S . V .F .S.Sand Silt Clay Class
Ahy 0-9
Bmy 9-19
ICY 19-83 50 .8 7 .7 3 .9 2 .6 5 .0 12 .3 67 .4 15 .6 10 .9 6 .6 12 .5 11 .1 56 .7 27 .5 15 .8 SLoam
IICy 83-89 13 .3 6 .0 6 .0 2 .3 3 .6 12 .0 59 .8 10 .9 11 .4 9 .6 15 .7 12 .8 60 .4 23 .3 16 .3 SLoam
IICyz 89+
Table 10 . Chemical and physical analyses, Fitz Roy Association - Stte : W-117 Location : 72 ° 38'N & 95°00'W Chemical Characteristics
Exchangeable Cations % o o Conduc- % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P 1103-N Hor . cm pH mhos/cm equiv . cite mite C N ratio m . e ./ Cat+ 2+ K+ Na+ ppm ppm 100 g Mg
Cy 0-70 8 .4 0 .28 29 .34 13 .4 14 .7 0 .3 0 .03 10 .0 4 .5 23 .1 2 .3 0 .2 0 .03 1 .0 0 .8
Cz 70+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction % ppm in saturation extract o % Depth o Total % % Textural Hor, On Stone Ca Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Cy 0-70 38 .5 12 .8 3 .4 3 .5 3 .2 15 .6 17 .5 3 .9 5 .6 5 .5 19 .1 12 .6 46 .7 31 .0 22 .3 Loam
Cz 70+
Table'11 .Chemical and physical analyses, Four Rivers Association
Sate : W-52A Location : 73 ° 20'N & 95°30'W Chemical Characteristics
Q o Exchangeable Cations Conduc- q, m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N 2+ K+ Na+ ppm ppm Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e ./ Ca Mg 2+ 100 g
Ahy 0-7
Bmy 7-34 7 .9 0 .23 0 .57 0 .4 0 .2 0 .3 0 .02 15 .0 5 .3 4 .2 2 .3 0 .1 0 .1 0 .5 0 .3
Cgy 34-55 8 .5 0 .28 0 .97 0 .3 0 .6 0 .2 0 .02 10 .0 5 .2 4 .3 2 .4 0 .1 0 .1 4 .1 0 .5
Cz 55+ '
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction ppm in saturation extract Depth % t Total / Textural Hor, cm Stone V .C .S . Ca Mg Na K Cl Soy-S C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Ahy 0-7
Bmy 7-34 17 .5 9 .2 21 .4 3 .3 5 .3 14 .7 0 .8 0 .5 0 .7 3 .3 20 .2 30 .6 55 .3 33 .2 11 .5 SLoam
Cgy 34-55 13 .5 6 .0 51 .5 4 .3 9 .9 14 .4 9 .1 1 .2 2 .1 1 .9 13 .2 40 .1 58 .5 31 .5 10 .0 SLoam
Cz 55+
Table 12 .Chemical and physical analyses, Garnier Bay Association
Site : WZ-2 Location : 73 ° 37'N & 94°50'W Chemical Characteristics
Exchangeable Cations o Avail . Conduc- % . % % ~ m .e ./100 gm Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N ppm Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e / Ca2+ 2+ Na+ ppm 100 g fig K+
Om 0-9 8 .0 0 .91 22 .3 0 .0 20 .5 24 .0 1 .5 16 .0 56 .0 33 .9 26 .0 1 .02 .28 35 .5 8 .8
Bmy 0-25 8 .0 0 .28 47 .1 3 .4 40 .3 0 .4 0 .1 4 .0 10 .4 8 .3 4 .1 0 .09 0 .02 2 .1 0 .0
Bgy 25-45 8 .0 0 .28 44 .8 5 .8 36 .0 2 .7 0 .3 9 .0 18 .6 16 .4 10 .5 0 .24 0 .06 0 .5 0 .0
C 1yz 45-68 8 .0 0 .51 42 .2 3 . .2 36 .0 2 .9 0 .3 9 .7 19 .1 16 .8 4 .8 0 .35 0 .06 3 .9 0 .0
C 2yz 68+ . 8 .4 L 0 .30 I 86 .7 I13 .7 I67 .0 0 .2 I0 .02 l 10 .0 I 9 .0 113 .8 11 .7 10 .01I 0 .08 I 0 .2 l 0 .0 I
Chemical Characteristics Particle Size Characteristics
o Soluble Salts Sand Fraction ppm in saturation extract Depth % Total % % Textural Hor . Stone cm Ca Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S. Sand Silt Clay Class
Om 0-9 123 .8 80 .6 11 .3 2 .8 17 .0 243 .0 N .D . Organic
Bmy 0-25 39 .3 14 .7 5 .7 2 .1 53 .3 21 .6 35 .6 4 .0 5 .6 8 .0 17 .0 8 .2 43 .4 41 .2 15 .4 Loam
Bgy 25-45 32 .5 15 .4 8 .8 3 .9 88 .8 5 .3 N .D . 0 .0 0 .1 0 .4 0 .8 2 .6 3 .9 54 .8 41 .3 SiClay
C1yz 45-68 64 .3 24 .1 9 .8 2 .0 30 .8 23 .5 N .D . 0 .6 0 .2 0 .4 1 .1 3 .3 5 .6 56 .9 37 .5 SiLoam
C 2yz 68+ 23 .8 11 .8 28 .6 3 .9 44 .4 14 .4 58 .6 9 .4 10 .9 5 .5 8 .4 17 .3 51 .5 34 .2 14 .3 Loam Association Table 13 . Moisture characteristics, Garnier Bay
Site : WZ-2 Location : 73 °37'N & 94°50'W
Moist . x Moist . % by by Bulk Horizon Depth Vol . Weight Density cm g/cc
Om 5 75 .6 341 .3 0 .98
Bg 20 40 .0 24 .0 2 .09
Bm 35 30 .4 20 .7 1 .78
Bm 40 34 .3 19 .3 2 .12
Cz 60 94 .4 115 .4 1 .61 .69 Cz 65 92 .l 99 .8 1 Table 14 . Temperature profile of a hummock, Garnier Bay Association
Site : WZ-2 Location : 73°37'N & 94°50'W Date : July 3, 1975
Section at top of hummock
Horizon Depth Temperature cm °C
Bm 5 8
Bm 10 6
Bg 20 5
Bg 25 4
Bg 30 3
Bg 38 0
Section in trough between hummocks
Horizon Depth Temperature cm °C
Om 5 6
Om 10 4
Om 15 1
Table 15 . Chemical and physical analyses, Howe Harbour Asàociation
Site : W-31 Location : 73'30'N &94 ° 00' Chemical Characteristics
o Exchangeable Cations Conduc- % % m .e ./100 gm Avail . Depth tivity CaCO3 Cal- Dolo- Org . Total C/N C .E .C . P N03-N ppm ppm Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e ./ 2+ Fig e+ K+ Na+ 100 g C9
Ahy 0-25
Bmy 0-54 8 .0 0 .37 33 .67 0 .0 31 .0 1 .0 0 .1 10 .0 9 .1 10 .8 4 .4 .13 .03 0 .66 2 .25
Cy 10-54 8 .0 0 .32 30 .34 0 .9 27 .1 1 .1 0 .1 11 .0 10 .0 13 .9 4 .5 .14 .03 0 .66 0 .75
Cz 54+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction % ppm in saturation extract Depth % Total % %' Textural Hor . Stone cm Ca Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V.F .S.Sand Silt Clay Class
Ahy 0-25
Bmy 0-54 53 .3 16 .8 3 .7 0 .9 3 .6 9 .7 23 .2 4 .9 8 .3 8 .7 13 .3 15 .0 50 .2 34 .0 15 .8 Loam
Cy 10-54 46 .0 14 .4 3 .0 1 .6 4 .3 9 .1 126 .1 5 .6 9 .6 9 .4 13 .4 13 .5 51 .5 31 .5 17 .0 Loam
Cz 54+
Table 16 . Chemical and physical analyses, Hunting Association
Side : WZ-4 Location : 73 ° 38'N & 95°12'W Chemical Characteristics
Exchangeable Cations % o Conduc- % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e ./ 2+ Mg t+ + ppm ppm 100 g Ca K Na+
Bm 0-15 8 .2 0 .24 80 .2 4 .4 69 .7 0 .8 0 .1 8 .0 9 .5 7 .0 4 .3 0 .04 0 .01 0 .5 0 .4
Bgy 0-26 8 .2 0 .23 83 .2 7 .3 69 .9 0 .5 0 .1 5 .0 8 .6 7 .8 4 .6 0 .02 0 .01 0 .0 0 .1
Cgy 26-60 8 .3 0 .18 86 .8 7 .8 72 .8 0 .4 0 .1 4 .0 8 .9 12 .8 2 .1 0 .03 0 .01 0 .5 0 .1
Cgz 60-68 8 .2 1 .05 71 .5' 10 .2 56 .3 3 .1 0 .3 0 .3 18 .2 16 .9 6 .7 0 .21 0 .11 4 .7 0.0
IICZ 68+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction ppm in saturation extract Depth % Total % % Textural Hor, cm Stone Ca* Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Bm 0-15 30 .5 14 .2 5 .3 1 .9 71 .0 9 .2 N .D . 1 .2 2 .1 2 .4 3 .2 5 .8 14 .7 74x1 11 .2 SiLoam
Bgy 0-26 35 .0 10 .6 3 .3 0 .9 88 .8 6 .1 N .D . 2 .3 3 .3 2 .6 2 .9 4 .6 15 .7 73 .0 11 .3 SiLoam
Cgy 26-60 26 .3 9 .0 4 .0 2 .6 67 .4 3 .3 N .D . 0 .4 1 .1 1 .7 3 .3 5 .8 12 .3 78 .2 9 .5 SiLoam
Cgz 60-68 95 .5 31 .3 5 .7 6 .5 21 .3 99 .6 0 .0 1 .3 0 .5 0 .7 1 .7 6 .0 10 :2 73 .0 16 .8 SiLoam
IICZ 68+ Table 17 . Moisture characteristics, Hunting Association
Site : WZ-4 Location : 73 °38'N & 95°12'W
Moist . % Moist . by by Bulk Horizon Depth Vol . Weight Density cm g/cc
Bm 5 38 .5 20 .5 2 .27
Bg 5 37 .2 18 .8 2 .35
Cg 40 32 .0 18 .0 2 .09
Cg 55 34 .6 14 .7 2 .47
Cz 60 44 .5 26 .6 2 .12 Table 18 . Temperature profile of an unsorted circle, Hunting Association
Site : WZ-4 Location : 73 °38'N & 95°12'W Date : July 7, 1975
Section at mid-circle
Horizon Depth Temperature cm °C
Bg 5 8 .0
Bg 10 7 .0
Bg 20 5 .0
Cg 30 3 .0
Cg 40 2 .0
Cg 50 1 .5
Cg 60 1 .0
Cg 62 0 .5
Section between circles
Horizon Depth Temperature cm °C
Bm 5 6 .5
Bm 10 6 .0
Bg 20 4 .0
Bg 30 3 .5
Bg 40 2 .5
Bg 50 1 .5
Bg 60 1 .0
Table 19 .Chemical and physical analyses, Lyons Point Association
Site : W-90 Location : 74°01'N & 98°32'W Chemical Characteristics
Exchangeable Cations % % Conduc- % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Hor . cm pH mhos/cm . equiv cite mite C N ratio m .e ./ 2+ 2+ + .Ppm ppm 100 g Ca Mg K Na+
Bm 0-5
Cy 5-5&~ 8 .0 0 .39 27 .31 6 .7 27 .3 0 .9 0 .08 11 .3 6'.3 12 .7 4 .6 0 .3 0 .1 2 .3 0 .5 Cz 58+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction ppm in saturation extract Depth % Total Hor . cm Stone % % Textural Ca' Mg Na K C1 S04-S 7-C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Bm 0-5
Cy 5-58 37 .3 16 .2 21 .3 8 .2 19 .1 24 .3 29 .1 4 .6 4 .4 3 .4 7 .3 14 .5 34 .2 36 .6 29 .2 CLoam
Cz 58+
Table 20 .Chemical and physical analyses, Mount Matthias Association
Site : W-85 Location : 73 ° 42'N & 99°12'W Chemical Characteristics
Exchangeable Cations Conduc- % % % % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E,C . P N03-N Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e ./ 2+ 2+ K+ Na+ ppm ppm 100 g Ca figg
Bmj 0-5 8 .1 0 .47 29 .43 20 .0 8 .7 0 .6 0 .06 10 .0 6 .5 23 .5 1 .9 0 .2 .03 1 .1 4 .8
Cy 5-46 8 .1 0 .29 29 .80 20 .9 8 .2 0 .7 0 .06 11 .7 6 .3 26 .4 2 .2 0 .2 .03 0 .8 0 .0
Cz 46+
Chemical Characteristics Particle Size Characteristics Soluble Salts ppm in saturation extract I Sand Fraction Depth % Total Hor, cm Stone % % Textural Ca' . Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S. Sand Silt Clay Class
Bmj 0-5 73 .5 15 .0 5 .1 3 .3 7 .1 24 .8 i 8 .8 3 .4 3 .7 3 .2 4 .9 13 .8 29 .0 45 .1 25 .9 Loam
Cy 5-46 44 .3 10 .5 2 .6 3 .0 5 .3 15 .6 10 .2 2 .7 3 .6 3 .9 5 .2 14 .4 29 .8 42 .3 27 .9 CLoam
Cz 46+
Table 21 .Chemical and physical analyses, Prince Regent Association
Site : W-72 Location : 73°04'N & 9'2°22'W Chemical Characteristics
Exchangeable Cations q ° Conduc- m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e ./ 2+ 2+ + ppm ppm 100 g Ca Mg K Na+
Bmj 0=10 8 .1 0 .52 66 .8 37 .3 27 .1 0 .4 0 .05 8 .0 4 .2 21 .0 1 .7 0 .1 0 .02 0 .5 6 .5
Cy 10-56 8 .1 0 .32 57 .2 29 .0 25 .9 1 .1 0 .10 11 .0 7 .2 23 .5 2 .3 0 .2 0 .02 1 .6 0 .0
Cz 56+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction 7 ppm in saturation extract . ° I . Total % Î Textural Hor . Depthp Stone Ca Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Bmj 0-10 74 .5 17 .7 6 . 2 .0 8 .0 17 .5 30 .3 4 .0 4 .3 2 .9 6 .5 15 .4 33 .1 48 .2 18 .7 Loam
Cy 10-56 53 .8 12 .6 2 .3 1 .8 4 .6 ' 9 .1 11 .2 3 .0 4 .0 3 .1 6 .6 11 .7 28 .4 54 .0 17 .6 Loam
Cz 56+
Table 22 .Chemical and physical analyses, Scarp Brook Association
Site : W-100 Location : 73 ° 35'N & 100°05'W Chemical Characteristics
Exchangeable Cations Conduc- % % % % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N + ppm Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e ./ 2+ 2+ Na+ ppm . 100 g C8 g K
Bmj 0-6 8 .0 0 .67 71 .52 25 .3 42 .5 0 .5 0 .05 10 .0 2 .9 23 .3 1 .3 0 .1 0 .02 1 .3 14 .3
Cy 6-71 8 .4 0 .30 72 .47 30 .5 38 .6 0 .6 0 .04 15 .0 7 .6 23 .5 1 .7 0 .1 0 .03 1 .2 0 .0
Cz 71+
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction ppm in saturation extract . Depth Total % % Textural Hor . cm Stone Ca Mg Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S. Sand Silt Clay Class
Bmj 0-6 100 .5 20 .8 3 .9 2 .7 7 .4 10 .8 30 .8 7 .0 8 .5 6 .2 8 .2 10 .1 40 .0 42 .9 17 .1 Loam
Cy 6-71 38 .0 14 .0 7 .3 2 .5 8 .5 19 .3 5 .7 7 .4 5 .3 6 .7 8 .0 33 .0 50 .8 16 .2 Loam
Cz 71+
Table 23 .Chemical and physical analyses, Stanwell Fletcher Association
Site : WZ-19 Location : 72 ° 58'N & 94°59'W Chemical Characteristics
Exchangeable Cations e Avail Conduc- % % m .e ./100 gm . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N Ca 2+ Mg2 + + ppm Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e ./ K Na+ ppm 100 g
Bm 0-6 6 .2 0 .18 ------1 .1 0 .1 11 .0 11 .6 6 .4 4 .3 M 0 .04 1 .1 0 .0
Cy 6-55 6 .8 0 .09 ------0 .2 0 .02 10 .0 6 .2 3 .3 2 .9 0 .3 0 .02 4 .3 0 .5
ICz 55-60 7 .0 0 .08 ------0 .1 0 .02 5 .0 5 .4 2 .4 2 .3 0 .3 0 .02 4 .0 0 .5
IICz 60+ 7 .0 0 .40 ------0 .1 0 .02 5 .0 2 .0 0 .9 1 .1 0 .2 0 .01 0 .8 0 .8
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction % ppm in saturation extract I % o Depth ~ Tot al % % Textural Stone Hor . cm Ca* Pig Na K Cl S04-S .C .S .. C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Bm 0-6 2 .2 8 .4 11 .0 6 .6 4 .6 17 .0 0 .0 0 .4 0 .8 1 .7 28 .2 13 .6 44 .7 2 .3 53 .0 Clay
Cy 6-55 1 .1 3 .3 3 .5 5 .4 3 .6 19 .0 0 .0 0 .1 0 .4 1 .0 25 .3 27 .7 54 .5 18 .0 27 .5 SCLoam
ICz 55-60 1 .2 3 .2 2 .4 5 .2 3 .2 6 .0 0 .0 0 .2 0 .6 1 .0 38 .0 20 .9 60 .7 16 .8 22 .5 SCLoam
IICz 60+ 28 .8 21 .4 3 .9 44 .8 5 .0 52 .0 0 .0 0 .0 0 .1 0 .8 44 .8 29 .6 75 .3 10 .6 14 .1 SLoam , Table 24 . Moisture characteristics, Stanwell Fletcher Association
Site : WZ-19 Location : 72 ° 58'N & 94°57'W
Moist . % Moist . % by by Bulk Horizon Depth Vol . Weight Density cm g/cc
Bm 10 21 .1 13 .8 1 .74
Cy 30 22 .6 12 .2 2 .07
Cy 50 23 .5 12 .3 2 .14
ICz 54 38 .5 24 .6 1 .78
IICZ 68 64 .8 34 .3 2 .52 Table 25 . Temperature profile, Stanwell Fletcher Association
Site : WZ-19 Location : 72 ° 58'N & 94°57'W Date : July 26, 1975
Horizon Depth Temperature cm °C
Bm 5 3 .5
Cy 10 3 .5
Cy 20 3 .0
Cy 30 2 .5
Cy 40 2 .0
Cy 50 1 .0
Cy 55 0 .0
Table 26 .Chemical and physical analyses, Transition Bay Association
Site : W-91 Location : 73°45'N & 97°36'W Chemical Characteristics
Exchangeable Cations Conduc- % % % % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N ppm Hor . cm pH nmhos/cm equiv . cite mite C N ratio m .e ./ 2+ K+ Na+ ppm 100 g Ca tig e+
Bmy 0-45 7 .9 0 .27 12 .70 1 .5 10 .3 2 .9 0 .2 14 .5 13 .2 12 . 9 6 .5 0 .2 0 .1 1 .2 0 .3
CZ 45+
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction ppm in saturation extract Depth Total % % Textural Stone Hor . Cm Ca rig Na K Cl S04-S V .C .S . C .S . M .S . F .S . V .F .S. Sand Silt Clay Class
Bmy 0-45 26 .0 15 .9 9 .0 2 .1 14 .5 23 .3 3 .1 0 .7 3 .3 7 .8 28 .0 17 .2 57 .0 23 .5 19 .5 SLoam
Cz 45+
Table 27 . Chemical and physical analyses, Two Rivers Association
Site : W-21 Location 73 ° 07'N & 93°36'W Chemical Characteristics
Exchangeable Cations Conduc- % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N ratio m.e ./ + ppm ppm Hor . cm pH nmhos/cm equiv . cite mite C N 2+ 2+ K Na+ 100 g C2 fig
Ahy 0-10
Bmy 0-20
Cy 20-57 8 .2 0 .26 53 .4 9 .4 40 .5 0 .1 0 .01 : . 10 .0 3 .4 15 .3 1 .5 0 .1 0 .01 0 .2 0 .3
Cz 57+
Chemical Characteristics Particle Size Characteristics
Soluble Salts Sand Fraction % ppm in saturation extract I Depth % Total % % Textural Hor . cm Stone Ca Pig Na K C1 S04-S V .C .S . C .S . M .S . F .S . V .F .S.Sand Silt Clay Class
Ahy 0-10
Bmy 0-20
Cy 20-57 37 .0 13 .2 6 .4 2 .6 3 .9 10 .8 14 .8 5 .8 9 .1 7 .0 19 .8 23 .5 65 .2 25 .3 9 .5 SLoam
Cz 57+ '
Table 28 . Summary of the Characteristics of Soil Associations .
Map Association Ccoregion Parent Mat rial Soil Subgroups and Drainage Class Active Layer Symbol Name Thickness Depth to Calcareousness Textural Origin (cm) Bedrock Class (m)
As Aston High extremely loam to alluvium on sedimentary 707 Rego .T. Cryosol (w) 50-60 Arctic calcareous sand bedrock 207 Rego .S . Cryosol (w) 50-60 107.' Gleysolic T . Cryoeol (i-p) 30-40
Be Batty Bay High extremely silty clay marine modified till on 707 Rego.S . Cryosol (w-i) 40-60 Arctic calcareous to loam Paleozoic sedimentary rock 207 Rego.T . Cryosol (w-i) 40-60 57 Saline Rego .S . Cryosol (w-i) 40-60 5% Brun . T . Cryoeol (w-i) 40-60 Bc Baring High moderately to sand to marine beach deposits on 907 Rego .T. Cryosol (w) 40-50 Channel Arctic very strongly gravel Paleozoic sandstone bedrock 107 Lithic Rego . T . Cryosol (w) 40-50 calcareous 107 Brun . T. Cryoeol (w-i) 40-50 Bh Birthday High extremely sand to marine beach deposits on 807 Rego . T. Cryosol (w) 40-50 Bay Arctic calcareous gravel Paleozoic limestone bedrock 107 Lithic Rego . T . Cryoeol (w) 40-50 107 Brun . T . Cryosol (w-i) 40-50
Br Birmingham High 1-2 noncalcareous loam to fines from weathered 907 Rego . T . Cryosol (i-p) 40-50 Bay Arctic sandy Precambrian gneissic bedrock 57 Lithic Rego . T . Cryosol (w-i) 50-60 loam 57 Brun . T . Cryoeol (i-p) 40-50 Cg Cape Mid- very strongly loam to alluvium on sedimentary bedrock 707 Brun . T. Cryosol (w-i) 40-50 Carry Arctic to extremely sand 207 Gleysolic T . Cryosol (i-p) 40-50 calcareous 107 Rego . T . Cryosol (w-i) 50-60 Ch Cape High < 1 moderately to --- Paleozoic sandstone bedrock Hardy Arctic very strongly & calcareous Mid- Arctic Table 28(cont'd)
Map Association Ecoregion Parent Material Soil Subgroups and Drainage Class Active Layer Symbol Name Thickness Depth to Calcareousness Textural Origin (cm) Bedrock Class (m)
Cr Creswell Mid- - moderately to silt loam marine sand and beach 70% Brun . T . Cryosol (w-i) 40-50 ' Arctic very strongly to sandy deposits on sedimentary 30% Rego . T . Cryosol (w) 50-70 calcareous loam bedrock El F,lwin High - extremely clay loam lacustrine deposits and 50% Brun . T . Cryosol (w-i) 40-50 River Arctic calcareous to silt colluvium undifferentiated 40% Rego . S . Cryosol (w-i) 40-50 loam on Paleozoic bedrock 10% Rego . T . Cryosol (w-i) 40-50 Fbl Fearnall Mid- 1 .5 extremely loam to marine modified till on 80% Brun . T . Cryosol (w-i) 50-60 Bay 1 Arctic calcareous sandy sedimentary bedrock 20% Rego . T . Cryosol (w-i) 60-70 loam F62 Fearnall Mid- 1 .5 extremely loam to marine modified till on 60% Brun . T. Cryosol (w-i) ' 50-60 Bay 2 Arctic calcareous sandy sedimentary bedrock 40% Rego . T. Cryosol 60-70 loam Fol Fiona High 1 .5 moderately to clay loam mixture of calcareous till 70% Brun . T. Cryosol (w-i) 70-90 Lake 1 Arctic extremely to sandy and fines of weathered 20% Rego . T . Cryosol (w) 70-90 calcareous loam Precambrian bedrock 10% Gley . T . Cryosol (i-p) 60-70 Fog Fiona High 1.5 moderately to clay loam mixture of calcareous till 70% Brun . T . Cryosol (w-i) 70-90 Lake 2 Arctic extremely to sandy and fines of weathered 30% Rego . T. Cryosol (w) 70-90 calcareous loam Precambrian bedrock Fr Four High - weakly to loam to glaciofluvial and ice- 60% Brun . T . Cryosol (w-i) 50-60 Rivers Arctic moderately sandy contact materials on 20% Rego . T. Cryosol (w) 50-60 calcareous loam Precambrian bedrock 20% Rego . S . Cryosol (w) 50-60 Fu Fury Mid- - strongly to clay to marine sediments on 80% Gley . T. Cryosol (i-p) 30-40 Arctic extremely silt sedimentary rock 20% Brun . T. Cryosol (1) 40-50 calcareous loam Table 28 (eont'd)
Map Association Ecoregion Parent Material Soil Subgroups and Drainage Class Active Layer Symbol Name Thickness Depth to Calcareousness Textural Origin Bedrock Class ( (m)
Fzl Fitz Mid- 1 .5 strongly to loam to till over Precambrian 80% Brun . T . Cryosol (w-i) 60-70 Roy 1 Arctic very strongly sandy bedrock 15% Rego . T . Cryosol (w-i) 60-70 calcareous loam - 57 Gley . T . Cryosol (i-p) 50-60 Fz2 Fitz Mid- 1 .5 strongly to loam to till over Precambrian 80% Brun . T . Cryoeol (w-i) 60-70 Roy 2 Arctic very strongly sandy bedrock 20% Rego . T . Cryosol (w-i) 60-70 calcareous loam Ga Garnier High - extremely silty clay marine sediment on sedimentary 60% Brun . T . Cryosol (w-i) 60-70 Bay Arctic calcareous to silt bedrock 20% Gley . T . Cryosol (i-p) 50-60 loam 15% Rego . T . Cryosol (w-i) 60-70 5% Saline Rego . T . Cryosol (w-i) 60-70 Gf Gifford High 2 moderately to silty loam weathered Tertiary sandstone, 60% Lithic Rego . S . Cryosol (w) 80-90 Point Arctic strongly to sand lignite end shale (Eureka 40% Lithic Regosol (w) 100+ calcareous Sound Formation) Gr Cape High 1 .5 noncalcareous sandy weathered Precambrian granite 40% Brun . T. Cryoeol (w-i) 60-70 Granite Arctic loam to (gneiss), may be wave- 20% Lithic'Rego . S . Cryoeol (w) 70-80 sand washed 20% Rego . T . Cryosol (w) 70-80 20% Gley . T . Cryosol (w-i) 60-70 Hn Hunting High - extremely silty colluvium or colluviated till 50% Gley . T . Cryosol (i-p) 50-60 Arctic calcareous clay on Paleozoic bedrock 50% Brun . T. Cryosol (1) 60-70 loam to loam Hw Howe High - very strongly loam to till and weathered Paleozoic 70% Brun . T . Cryoeol (w-i) 50-60 Harbour Arctic to extremely sandy dolostone 30% Rego . T . Cryosol (w-i) 50-60 calcareous loam Lp Leopold High - very strongly sand to erosional products such as 40% Lithic Rego . S . Cryosol (w) 80-90 Arctic to extremely gravel screes and talluses on 30% Orthic Regoeol (w) 100+ calcareous sedimentary rock . 30% Lithic Regosol (w) 100+ Ly Lyons High - strongly to loam to till and weathered sandstones 607. Brun . T . Cryoeol (w-i) 50-60 Paint Arctic very strongly clay loam and dolostones 40% Rego . T . Cryosol (w) 50-60
Table 28 (conta)
Map Association Ecoregion Parent M terial Soil Subgroups and Drainage Class Active Layer Thickness Symbol Name Depth to Calcareousness Textural Origin (cm) Bedrock Class (m)
Mc Mt . High 1 very strongly -- Paleozoic bedrock of Claredon Arctic to extremely limestone, doloetone and calcareous sandstone Mml Mt . High 1 .5 moderately to loam to mixture of till and weathered 75% Rego . T . .Cryosol (w-i) 60-80 Matthias Arctic very strongly sandy Paleozoic sandstone bedrock 10% Brun . T . Cryoeol (w-i) 60-80 câlcareous loam 10% Gley . T . Cryoaol (i-p) 50-60 5% Rego . S . Cryoeol (w-i) 60-80
Mm2 Mt . High 1 .5 moderately to loam to mixture of till and weathered 75% Rego . T . Cryosol (w-i) 60-80 Matthias Arctic very strongly sandy Paleozoic sandstone bedrock 10% Brun . T . Cryosol (w-i) 60-80 calcareous loam 10% Gley . T . Cryosol (i-p) 50-60 5% Rego . S . Cryosol (w-i) 60-80 Ot Otrick Mid- noncalcareous loam to alluvium on Precambrian 50% Rego . T . Cryosol (w-i) 80-90 Island Arctic sand bedrock 50% Brun . T . Cryoeol (w-i) 80-90 Pr Palmerston High 1 noncalcareous -- Precambrian gneiss, schiste ------Point 6 and granite Mid- ' Arctic Pg Prince Mid- extremely loam to till and marine modified 60% Brun . T . Cryosol (w-i) 50-60 Regent Arctic calcareous silt till on sedimentary bedrock 30% Rego . T . Cryosol (w-i) 50-60 loam 10% Rego . S . Cryosol (w-i) 50-60 Sbl Scarp High 1.5 extremely loam to mixture of till and weathered 80% Rego . T . Cryoeol (w-i) 60-70 Brook 1 Arctic calcareous sandy Paleozoic limestone, doloetone 10% Brun . T . Cryosol (w-i) 60-70 loam and sandstone 5% Rego . S . Cryosol (w-i) 60-70 5% Gley . T . Cryosol (i-p) 30-40 Sb2 Scarp High 1.5 extremely loam to mixture of till and weathered 80% Rego . T . Cryosol (w-i) 60-70 Brook 2 Arctic calcareous sandy Paleozoic limestone, doloetone 10% Brun . T . Cryosol (w-i) 60-70 loam and sandstone 10% Rego . S, Cryoeol (w-i) 60-70
Table 28 (cont'd)
Map Association Ecoregion Parent M terial Soil Subgroups and Drainage Class Active Layer Symbol Name Depth to Calcareousness Textural Origin Thickness (cm) Bedrock Class (m)
Sf Stanwell- Mid- 1-2 strongly to clay mixture of till and uncon- 70% Brun . T . Cryosol (w-i) 60-70 Fletcher Arctic very strongly loam to solidated Tertiary sandstone 307. Rego . T. Cryosol (w-i) 60-70 calcareous sand and shale (Eureka Sound Formation) Tb Transition High moderately to sand to marine beach deposits on 90% Rego . T . Cryosol (w) 50-60 Bay Arctic very strongly gravel Paleozoic sandstone 10% Lithic Rego . T . Cryosol (w) 50-60 calcareous bedrock 10% Brun . T . Cryosol (w-i) 50-60 Tw Two Mid- extremely sandy till and weathered sandstone 609, Brun . T . Cryosol (w-i) 50-60 Rivers Arctic calcareous loam of the Peel Sound Formation 40% Rego . T . Cryosol (w-i) 60-70 Wa Wadworth Mid- noncalcareous sand to erosional products such as 407. Lithic Rego . S . Cryosol (w) 80-90 Island Arctic gravel screen and talluses on 30% Orthic Regosol (w) 100+ Precambrian bedrock 30% Lithic Regosol (w) 100+ St Scott High extremely loam to glaciofluvial and ice- 80% Rego . T . Cryosol (w) 60-70 Bay - calcareous sand contact deposits on 20% Rrun . T . Cryosol (w-i) 60-70 sedimentary rock Arctic
Table 29. An example of the Saxifraga-Salix community type (map symbol 2 .4)
Site : VW6 Location : 72° 58'N 94° 57'W Site Descriptions : 3% E slope, moderately calcareous, moderately well drained sand Vegetation Cover : 25%
Species Domin No . Dryas integrifolia 4 Rhacomitrium languginosum 2 Salix arctica 2 Saxifraga oppositifolia 2 Thamnolia spp . 2 Alectoria spp . 2 Stereocaulon spp . 4 Umbellicaria spp . 2 Rhizocarpon geogrphicum 2 Carex rupestris 4 Polyblastia spp . 2 Poa arctica 2
Table 30 . An example of the Cetraria-Cassiope community type (map symbol 2 .8) Site : VW5 Location : 72° 58'N 94° 57'W Site Descriptions : 6% E slope, moderately calcareous, moderately well drained sand Vegetation Cover : 1001 Species Domin No . Cassiope tetrajona 7 Salix arctica 4 Carex rupestris 3 Rhacomitrium languginosum 8 Cladonia spp . 5 Alectoria spp . 3 Stereocaulon spp . 5 Cetraria deliesi 3 Pedicularis arctica 3 Polyblastia spp . 5 Thamnolia spp . 4
Table 31. An example of the Saxifraga-Polyblastia community type (map symbol 2 .10) Site : VWll Location : 73 ° 03'N 94 ° 05'W Site Descriptions : 6% W . slope, imperfectly drained, moderately calc . sand Vegetation Cover : 80%
Species Domin No . Dryas integrifolia 7 Thamnolia 3 Cetraria cucullata 3 Saxifraga oppositifolia 2 Salix arctica 2 Stereocaulon 7 Alectoria spp . 2 Polyblastia spp . 3 Cetraria deliesi 2 Pedicularis arctica 2
Table 32 . An example of the Carex-Arctagrostis community type (map symbol 3 .1) Site : VW3 Location : 72° 58'N 94° 57'W Site Descriptions : 6% S . slope, imperfectly drained, weakly calc . sand Vegetation Cover : 90%
Species Domin No . Salix. arctica 5 Rhacomitrium languginosum 5 Carex spp . 5 Dryas integrifolia 2 Polygonum vibiparum 2 Thamnolia spp . 4 Stereocaulon spp . 4 Alectoria spp . 4 Polyblastia spp . 4 Hlirochloe alpina 2 Arctagrostis latifolia 2 Alopecurus alpina 2 Cassiope tetragona 2 Cladonia spp . 4
Dicranum spp . 4 Tortula spp . 2
Table 33 . An example of the Carex-Drepanocladus community type (map symbol 3 .2)
Site : VW4 Location : 72° 58'N 94° 57'W Site Descriptions : level, poorly drained moderately calcareous silt Vegetation Cover : 1001
Species Domin No .
Carex spp . 7 Polygonum vivipanum 2 Heirochloe alpina 2 Saxifraga hircules 2 Drepanocladus revolens 9 Thamnolia spp . 2 Cetraria spp . 2 Pedicularis arctica 2 Polyblastia 2 Dicranum spp . 6 Distichium capillaceum 7 Calliergon giganteum 7
Table 34 . Temperature profile -of-- Site-- WZ21
Site : WZ-21 Location : 73 °07'N & 93°36'W Date : July 27, 1975
Horizon Depth Temperature cm °C
Bmy 5 3 .5
Bmy 10 3 .5
Bmy 20 3 .0
Cy 30 2 .0
Cy 40 0 .5
Cy 42 0 .0
Table 35 . Chemical and physical characteristics of a Glacic Mesic Organo Cryosol . Site : WZ-10 Location : 74'01'N & 93°27'W Chemical Characteristics
Exchangeable Cations Conduc- % % % % m .e ./100 gm Avail . Depth tivity CaC03 Cal- Dolo- Org . Total C/N C .E .C . P N03-N K+ ppm Hor . cm pH mhos/cm equiv . cite mite C N ratio m .e / 2+ 2+ + ppm 100 g C8 Fig Na
Oh 0-5 7 .l 1 .26 5 .4 3 .8 l .5 24 .8 2 .5 9 .2 122 .5 111 .8 12 .5 0 .20 0 .84 15 .5 232 .5
Om 5-25 6 .l 0 .46 3 .2 0 .9 2 .2 35 .6 2 .9 12 .3 111 .0 81 .8 8 .4 0 .10 0 .20 7 .5 78 .8
Omz 25-55 6 .5 1 .35 2 .6 0 .7 1 .7 43 .6 3 .7 11 .8 90 .1 66 .8 5 .8 0 .05 0 .12 6 .3 0 .0
Wz 55-100--
Chemical Characteristics Particle Size Characteristics Soluble Salts Sand Fraction ppm in saturation extract Depth % e Total / Textural Hor . cm Stone Ca' Mg Na K Cl S04-S V .C .S . C . S . M .S . F .S . V .F .S.Sand Silt Clay Class
Oh 0-5 212 .5 34 .4 30 .7 2 .0 117 .2 55 .8 0 .0 Organic
Om 5-25 84 .3 11 .4 4 .7 1 .1 19 .2 24 .0 0 .0 Organic
Omz 25-55 28 .3 3 .4 3 .0 0 .6 7 .l 15 .6 0 .0 Organic
Wz 55-100 ' Table 36 . Moisture characteristics, Organic soil
Site : WZ-10 Location 74'01'N & 93°27'W
Moist . % Moist . by by Bulk Horizon Depth Vol . Weight Density cm g/cc
Oh 5 28 .9 86 .6 0 .62
Om 18 31 .3 102 .0 0 .62
Omz 23 58 .1 215 .6 0 .78
Omz 30 91 .7 255 .9 1 .17
Omz 50 91 .8 274 .1 1 .14
Omz 77 92 .2 204 .8 l .26
Wz 96 98 .7 3740 .7 0 .95 Table 37 . Temperature profile, organic soil
Site : WZ-10 Location : 74*01'N & 93°27'W Date : July 14, 1975
Horizon Depth Temperature cm °
Oh 5 3 .0
Om 10 3 .0
Om 20 2 .0
Om 25 0 .0