**BOREAS PROJECT** **TE-20**

**SOILS OF TOWER SITES AND SUPER SITE**

**NORTHERN STUDY AREA**

**THOMPSON, MANITOBA, CANADA**

**by**

**Hugo Veldhuis**

**AGRICULTURE AND AGRI-FOOD CANADA, RESEARCH BRANCH**

**CENTRE FOR LAND AND BIOLOGICAL RESOURCES RESEARCH**

**MANITOBA LAND RESOURCE UNIT**

**WINNIPEG, MANITOBA**

**CANADA**

**Winnipeg June, 1995**

Contact address for this report and accompanying data:

Mr. Hugo Veldhuis

Agriculture and Agri-Food Canada

CLBRR, Manitoba Land Resource Unit

Rm. 362A, ELLIS Building

University of Manitoba

Winnipeg, Manitoba

Canada R3T 2N2

Tel: (204) 474-6124

Fax: (204) 275-5817

**PREFACE**

Four tower sites, Old Jack Pine (OJP), Young Jack Pine (YJP), Old Black
Spruce (OBS) and Fen (FEN), were established in 1993 in the BOREAS
Northern Study Area located between Thompson and Nelson House in
North-central Manitoba. An ancillary site, Old Trembling Aspen (OTA) and
a large site called the Super Site (SST) were added in 1994. The Super
Site encompasses an area which includes all tower sites and OTA and the
area between and some distance around the tower sites. The soil and
landscape information from the sites is required by investigators of
varying disciplines to help correlate atmospheric data with soil and
landscape units, and to develop an understanding of the extent of
potential carbon sinks and carbon sources in this part of the Boreal.

Soil investigations of the four tower sites commenced in 1993, and were
continued during the 1994 field season. Also in 1994 the soils of the
Old Trembling Aspen site and of the Super Site were investigated,
described and sampled. In addition four soils along the Gillam road were
described and sampled in burns of varying ages.

The soils of the tower and ancillary site were investigated, described
and mapped at a scale of 1:5000. The area of the tower sites is circular
with a radius of 500 m with the tower, or a locartion near by as pivot
point. The OTA site is smaller and basically rectangular and borders on
the highway The tower sites were investigated in detail in the late
summer of 1993. Also some inital work was done on the FEN site during
that time. During the winter of 1993-94 the data was evaluated, and it
became apparent that the OJP and YJP sites required additional site data
to delineate soil units properly. This additional work was carried out
during the summer of 1994. During the same period the FEN tower site was
also surveyed as was the OTA site. However most of the 1994 field season
was spent on the mapping and soil and landscape data collection of the
Super Site, which is mapped at a scale of 1:100 000.

In the following report the soils of the five detailed sites and the
Super Site are described. Some information on geology and geomorphology
of the area is provided, as well as a section on soil development,
permafrost distribution and soil-landscape relationships. The
accompanying maps show the distribution of soil types or groups of soil
types in the tower sites and the super site.

**ACKNOWLEDGEMENTS**

I like to acknowledge firstly the financial support received from the
U.S. National Aeronautics and Space Administration (NASA) for the field
work and soil analyses for the project. Especially I like to thank Dr.
Elissa Levine for her support for the project. I also like to thank
Agriculture and Agri-Food Canada, and especially Drs. Richard Asselin,
Dr. Dick Coote and Mr. Robert Eilers for allowing me the time to carry
out the project and their interest shown throughout. I also thanked Ms.
Barbara Stupak, Agriculture and Agri-Food Canada for her administrative
help.

I also like to acknowledge the interest shown and the financial support
provided in 1993 by Dr. Jennifer Harden, U.S. Geological Survey. The
encouragement and cooperation in the field has made the project a
special experience. I also like to thank very much the support and
encouragement received from Dr. Susan Trumbore, University of
California, Dr. Patrick Crill, University of New Hampshire, Drs. Tim
Moore and Jill Bubier, McGill University.

Also acknowledged are Mr. Barry Goetz, University of Saskatchewan, Mrs.
Rehanna Mirza, Manitoba Department of Agriculture, and Mr. Don Swidinsky
for carrying out soil analyses.

Many thanks are due to Mrs. Sheri Grift, Agriculture and Agri-Food
Canada for her diligent data input, editing of files, legends and maps.
Mr. Arnie Waddell, Agriculture and Agri-Food Canada is also thanked very
much for all his hard work to get the GIS maps developed. Mr. Jim
Griffiths, Manitoba Agriculture, is thanked for helping to produce the
hard copy maps and Mr. Cris Aglugub, Manitoba Agriculture is thanked for
the development of the soil data storage software.

A special thanks goes to Messrs. Seth Henoch and Elie St.Jacques,
Agriculture and Agri-Food Canada for the hard work they put in during
the 1994 field season, and to Mr. Tom Black, U.S. Geological Survey for
his assistance in the field in 1993.

Many more people supported the project in some way or another,
facilitated the field portion of the project, or helped me with data
input and map development. It has been appreciated very much.

**TABLE OF CONTENTS**

**PREFACE** 3

**ACKNOWLEDGEMENTS** 4

**PART 1** 8

**1 GENERAL DESCRIPTION OF THE STUDY AREA** 8

1.1 Physiography and surficial deposits 8

1.2 Climate 9

1.3 Soil Climate 9

1.4 Soil Moisture 10

1.5 Permafrost 10

**PART 2** 12

**2 METHODOLOGY** 12

2.1 Map Polygon 12

2.2 Simple and Compound Map Polygons 13

2.2.1 Simple Map Polygon 13

2.2.2 Compound Map Polygon 13

2.3 Phases 13

2.4 Sampling 14

2.5 Mapping and Characterization of Soils and Landscapes 15

2.5.1 Soil Mapping of the Tower Sites 16

2.5.2 Soil Mapping of the Super Site 16

2.6 Maps and Legends 17

**PART 3** 18

**3 DEVELOPMENT, CLASSIFICATION AND DESCRIPTION OF SOILS** 18

3.1 Soil Classification and Development 18

3.1.1 Soils on Fine Textured Glacio-lacustrine Sediments 18

3.1.2 Soils on Coarse Textured Glacio-fluvial Deposits 19

3.1.3 Soils Developed on Organic Materials 19

3.2 Soil Series and Complexes 21

3.2.1 Soils Developed on Calcareous, Fine Textured, Glacio-lacustrine
Sediments 21

3.2.2 Soils Developed on Fine Textured Alluvial (fluvial) Deposits 22

3.2.3 Soils Developed on Sandy Glacio-fluvial and Glacio-lacustrine
Deposits 23

3.2.4 Non-frozen Organic Soils 25

3.2.5 Permanently Frozen Organic Soils 28

3.3 Soil Series, Phases, Variants and Complex Descriptions 29

ATK - ATIK complex 29

3.3.2 BDY - BALDY series 29

BDYp - BALDY peaty phase 30

BGCd - BOG COLLAPSE deep phase 30

BGCv - BOG COLLAPSE very deep phase 31

BRN - BRANNIGAN CREEK series 32

BRNp - BRANNIGAN CREEK peaty phase 32

BTT - BUTTON series 33

BTTp - BUTTON peaty phase 33

CLK - CLARKE series 33

CLK1 - CLARKE variant 1 34

CMK - CORMORANT LAKE complex 34

FCDd - FEN COLLAPSE deep phase 36

FCD1 - FEN COLLAPSE variant 1 36

FCDv - FEN COLLAPSE very deep phase 37

FCD2 - FEN COLLAPSE variant 2 37

FENs - FEN shallow phase 38

FENd - FEN deep phase 38

FENv - FEN very deep phase 39

GRS - GRASS RIVER complex 39

LPR - LA PEROUSE series 40

LPRp - La PEROUSE peaty phase 40

LWP - LOW PINE series 41

LWP1 - LOW PINE variant 1 41

MDR - MEDARD series 42

MDRp - MEDARD peaty phase 43

NIC - NICHOLS LAKE complex 43

NIC1 - NICHOLS LAKE variant 1 44

NIC2 - NICHOLS LAKE variant 2 44

PAA - PALSA complex 44

PAAd - PALSA deep phase 45

PAA2 - PALSA variant 2 46

PCB - PARTRIDGE BEAK series 47

PCH - PARTRIDGE HEAD series 47

PCP - PARTRIDGE CROP series 48

PCPh - PARTRIDGE CROP humus variant 48

PKW - PAKWA series 49

PLH - PALSA HUMMOCK complex 49

PLT - PLATEAU complex 50

PPU - PIPUN series 50

ROK - ROE LAKE series 51

ROK1 - ROE LAKE variant 1 52

SWK - SIPIWESK series 52

SWK - SIPIWESK cryic phase 53

SYBd - SANDY BOG deep phase 53

SYBs - SANDY BOG shallow phase 54

TBL - TURNBULL series 54

TFNs - THAW FEN shallow phase 55

TFNw - THAW FEN very shallow phase 56

TYL - TYRRELL series 56

WBW - WABOWDEN series 57

WBWz - WABOWDEN cryic phase 58

WRL - WARREN LANDING series 58

WTP - WET PINE series 59

WTP1 - WET PINE variant 1 59

YGP - YOUNG PINE series 60

YGP1 - YOUNG PINE variant 1 60

**BIBLIOGRAPHY** 62

**APPENDIX A** 63

GLOSSARY 63

**APPENDIX B** 74

SOIL HORIZON DESIGNATIONS 74

ORGANIC HORIZONS 74

MASTER MINERAL HORIZONS 74

LOWER-CASE SUFFIXES 75

**PART 1**

**1 GENERAL DESCRIPTION OF THE STUDY AREA**

In the following section a general description of the landscape in which
the sites are located is provided. Also a general physiographic
description of each tower site is given.

**1.1 Physiography and surficial deposits**

The area between Thompson and Nelson House is physiographically part of
the Kazan Upland, which is part of the Kazan Region, which in turn is
part of the Shield (Bostock 1968). Thus the area is underlain by fine
and coarse grained bedrock of Precambrian origin. The bedrock is for the
most part blanketed by thick surficial deposits. Although the bedrock
topography is masked by the unconsolidated surficial materials the
general subdued hummocky topography reflects, at least in part, the
configuration of the underlying bedrock.

During the Wisconsin glaciation all of the area was subject to the
scouring of bedrock, and the removal and deposition of unconsolidated
materials by land ice. The eastern part of the area was covered by the
Labradorean Ice Sheet, while the western part was covered by the
Keewatin Ice Sheet. Deposition of ground moraine (till) took place, but
the deposits are often thin or non existent. In the study area only
limited exposures of morainal till occur, and they are generally
associated with bedrock outcroppings.

Other materials laid down during the glacial period consist of
interlobate and end moraine deposits as well as glacio-fluvial materials
(Nielsen et al. 1981). These deposits are generally sandy and gravelly,
and in part silty and form some of the most pronounced topographic
elements in all of the study area.

During deglaciation glacial Lake Agassiz developed in front of the
receding ice sheets. Large amounts of sediments were deposited in the
deep water sections, while strand lines developed along the shores. The
lake level was not static, but fluctuated as outlets opened up or
closed. Glacial Lake Agassiz disappeared about 7500 years B.P. (Klassen.
1983) from all of northern Manitoba, and probably some what earlier from
the study area.

Because of the short time that has elapsed since the land fell dry
drainage is not well developed and the terrain is characterized by many
depressions that lack drainage or are linked by slow moving creeks.

Due to the imperfectly developed drainage system, the development of
organic deposits is wide spread throughout the area. Most low lying area
contain organic deposits of various thicknees and of varying origin.
Bordering gentle sloping uplands often are covered with thin peat as
well, although this peat is not as permanent in the landscape as the
deposits that developed in the depressions.

The Old Jack Pine (OJP and Young Jack Pine (YJP) sites are situated on
glacio-fluvial deposits, which may be part lateral moraine and part
kames. The deposits are stratified and apper to have been subject to
wave action during various stages of Glacial Lake Agassiz. Washed, very
stony and cobbly ridges and hummocks are present in both localities,
also subdued beaches occur in both area. In a number of areas very sandy
and gravelly materials, possibly glacio-fluvial materials rest on or
contain fine textured, calcareous materials, which probably are of
glacio-lacustrine origin. Sand washed out off the glacio-fluvial
materials has been redeposited as sandy lacustrine in areas bordering
the glacio-fluvial deposits.

The Old Black Spruce site is very representtative of a large part of the
Super Site. This tower site is a complex of subdued hummocky, clayey
glacio-lacustrine and peat filled depressions, with permafrost in many
localities. Thin discontinous peat cover a large part of the site due to
the gentle slopes and forest fire free period sufficiently long for
mature black spruce to develop and sphagnum mosses to accumulate.

The Old Trembling Aspen site is also located on hummocky, clayey,
glacio-lacustrine sediments, but the slopes are generally steeper and
the are is better drained. Peaty soils, and permafrost areas occur along
the lower slopes.

The Fen site is for the most part a depression occupied by deep fens and
high, permanently frozen palsas, which have high ice content. This peat
filled depression is bordered by hummocky, clayey, glacio-lacustrine
uplands, which are partially covered by shallow peat.

**1.2 Climate**

The closest meteorological station is the one located at Thompson
airport, where records have been kept for more than 30 years.

The study area is situated along the northern boundary of Subregion 1 of
the High Boreal subhumid Ecoclimatic Region (Manitoba Ecoclimatic
Regions Working Group. 1985). This region is characterized by long, cold
winters and short cool summers. The mean annual air temperature (MAAT)
is -1.9 oC and the mean annual precipitation is 485 mm. The mean
frost-free period is 93 days, but varies significantly, as does the
number of degree days which averages 1089.

**1.3 Soil Climate**

The soil climate of the area is classified as cold Cryoboreal with humid
and aquic soil moisture regimes (Clayton [et]{.underline}
[al]{.underline}. 1977). According to soil climate data collected by the
Canada-Manitoba Soil Survey in this area, mean annual soil temperature
(MAST) at 50 cm depth is between 2.1 and 3.7 oC on well drained clay,
approximately 2.8 oC on poorly drained clay and about 3.7 oC on well
drained loamy sand and sandy loam. The mean summer soil temperatures
(MSST) at 50 cm range from 5.7 to 8.9 oC for well drained clays, to
about 5.2 oC on poorly drained clay. MSST ranges between 9.2 and 10.5 oC
on well drained sandy loam and loamy sand. However these temperatures
are all very much influenced by vegatation characteristics of the sites.
Therefore an upland clay soil may well have a MAST and MSSYT several
degrees lower than indicated. Upland clay areas tend to have rather low
MAST and MSST when a well established closed black spruce forest cover
with feather moss ground cover is present.

Organic soils have colder thermal regimes than mineral soils in the same
area, and at 50 cm depth these soils have MAST of less than 2 oC and
MSST of less than 5 oC. Data for two sites from a long term soil climate
study a short distance north of Thompson are presented in Table 2, and
may be used as indicators of values that may be expected to be found on
similar sites in the study area.

**1.4 Soil Moisture**

The soil moisture regimes are dominantly humid and subhumid on clay and
subhumid on sandy loam, loamy sand and sand . Organic soils are aquic
and peraquic. Soil water deficits occur on freely drained clayey, loamy
and sandy soils. Deficits can be severe on coarse textured materials,
but in some years even clay soils may experience large deficits. Mineral
soils that are saturated for moderately long periods occur extensively
and consist largely of poorly drained clay soils, which are usually
overlain by thin peat. Organic soils remain saturated for very long
periods or throughout the year. Fens usually have a water table close to
or at the surface, but the water table may drop significantly in dry
years, depending of hydrological conditions. Bogs will have a water
table a short distance below the surface for a period during the growing
season, but the water table may drop considerably later in the year,
especiall if precipitation is less than average. Some frozen organic
deposits have better drainage due to concave nature of the permafrost
which aids drainage, and the upper part of the peat may become dry in
the latter part of the summer season.

**1.5 Permafrost**

The study area lies in the discontinuous permafrost zone. Permafrost is
locally extensive, especially in bogs, but very localized in shallow
organic deposits and upland locations. The formation and the stability
of permafrost in this regiona is very much dependent on local, sometimes
very local, conditions. In this region the permafrost is in an easily
disturbed equilibrium with the regional climate.

Although permafrost is degrading in many areas, it is, at the same time,
aggregating in other areas. It is known that drainage, depth of organic
overlays and type of vegetative cover all play an important role in the
maintenance and formation of the permafrost. This is very evident in
veneer bog areas, where permafrost is very localized and often confined
to singular or small groups of sphagnum hummocks with the right vertical
and lateral dimensions. If the hummocks are of sufficient height and
extent, or if smaller are well shaded by black spruce, and are situated
on terrain with enough slope to move excess water away permafrost may be
present. This frost does not extent very deep, and is best visualised as
a lens. However if left undisturbed for an extended period these area
could develop into more extensive permafrost bodies.

Permafrost is also present in clayey uplands, but only where the
feathermoss cover is thick and the black spruce stands are dense and
tall enough to provide shade throughout the swummer day. The permafrost
on upland sites, and also in veneer bogs, is so much dependent on the
insulating properties of the organic surface layer and/or density of the
forest stand, that small disturbances in the vegetative cover may cause
the permafrost to melt. On these sites permafrost develops after soil
development has been active for some time in a permafrost free
environment.

Evidence of permafrost on clayey upland sites is limited to a soil
temperature below 0 oC at some depth and the presence of ice (segregated
ice crystals, vein ice, ice lenses). Also thermokarsting expressed in
the form of irregular highs and lows may be present. Cryoturbation in
the profile is minimal and, if present, is usually confined to the
subsoil. Distorted varves are the most common morphological evidence.
However in some areas small low relic earth hummocks (a form of a
nonsorted net) have been found. These hummocks which are formed in a
permafrost environment are very persistent and remain long after the
permafrost has disappeared. The most clearly observed after forest fires
which expose the mineral soil. Earth hummock like features may also be
present under sphagnum hummocks.

The earth hummocks, both relict and active, have commonly cryoturbated
organic material like organic smears or inclusions to a depth of 60 to
80 cm from the surface. As a result of climatic change or disturbance
permafrost likely disappearde and although consequent soil devlopment
possibly obliterated most evidence of cryoturbation the organic smears
and inclusions and the hummocky surface configuration persisted.

The permafrost in peat plateaus and palsas has influenced soil
development more strongly than on uplands. The accumulation of organic
matter or peat is governed and modified by the developing permafrost
which causes the surface to rise above the surrounding terrain. As a
result drainage is altered, usually resulting in a change in vegetative
composition and a change in insulating properties of the peat material.
Permafrost in these landforms is generally well established, is several
meters thick, and is able to withstand minor disturbance. However in
this region the thermal balance is precareous and thermokarsting is a
common phenomenon. Therefore associated with these peatlands are both
active and inactive bog and fen collapses.

**PART 2**

**2 METHODOLOGY**

**2.1 Map Polygon**

A map represents mappable portions of the soil landscape that together
have characteristics and properties varying within more or less narrow
limits that are determined by the intensity of the survey. A map polygon
contains one or more than one soil or nonsoil individual plus a certain
proportion (varying within prescribed limits) of unnamed and undescribed
inclusions. They are delineated on the basis of the types and relative
proportions of their soils or nonsoils, as well as on the basis of
external criteria such as slope or stoniness.

Soil maps show the distribution of kinds of soils and, as such, serve as
a link so that the knowledge gained in one locality about the usefulness
or behaviour of a kind of soil can be extended to other bodies of the
same soil.

A map polygon represents a real portion of the landscape and is an
aggregate of all the soil types, landforms, slopes and other
characteristics within its boundary. The proportions of each of the
component soils and nonsoils and undescribed inclusions may vary
strongly from one delineation to another. But polygons containing
similar soil types in similar proportions will in general be very much
alike in most other aspects, although may vary to some degree in slope.
The soil units used are soil series, phases, variants and complexes.

The soil series is defined as a naturally occurring soil body such that
any profile within that body has a similar number and arrangement of
horizons whose colour, texture, structure, consistence, reaction and
composition are within a narrowly defined range. The phase usually
differs from the series concept in one characteristic. A variant may
vary in one or more characteristics, and would possibly be a series in
itself if the extent of its distribution was known more precisely, and
sufficient representative profiles were described and sampled. In many
parts of the study area soils that differ quite markedly from each other
occur in such close proximity or such complexity, that they are
difficult to map as separate entities. These soils have been mapped as
complexes. Organic soils often fall in this category, as do soils which
drainage and soil development is affected by forest fire or permafrost
development.

Map polygons will always contain small proportions of inclusions that
have not been identified. These inclusions may be soil or non-soil
mapping individuals that are named elsewhere in the survey, or soils or
nonsoils that are not recognized and named at all in the survey. They
may, however, be mentioned in the description of other soil types in the
report.

**2.2 Simple and Compound Map Polygons**

There are two major types of map polygons, simple and compound. The
difference between them is defined in terms of the proportion and
contrast of their components.

[2.2.1 Simple Map Polygon]{.underline}

A Simple Map Polygon contains predominantly one soil or nonsoil. The
proportion of its components vary according to their areal extent and
contrasting characteristics as they may affect soil management or use.

Its components vary as follows: the predominant component comprises at
least 65 percent with up to 35 percent of nonlimiting, similar
components (components are alike in most properties and behaviour), or
up to 25 percent of nonlimiting dissimilar components (components do not
affect management of the map unit but have a significant number of
properties that vary from the predominant component), or up to 15
percent of limiting, dissimilar components (components have many
contrasting properties and usually affect management differently).

[2.2.2 Compound Map Polygon]{.underline}

A Compound Map Polygon contains predominantly two or more soils or
nonsoils (or a combination of both). The proportions of the major
components may vary from one considerably exceeding the others to all
being approximately equal. Complementary to the definition of a single
map unit, the proportions of its components vary according to their
areal extent and contrasting characteristics. As they may affect soil
management or use its major components vary as follows: if other
components are similar and nonlimiting no single component represents
more than 65 percent: or if other components are dissimilar and
nonlimiting no single component represents 75 percent; or if other
components are dissimilar and limiting no single component represents 85
percent.

**2.3 Phases**

It is frequently desirable to indicate a condition or quality of soil
property or landscape feature that deviates significantly from the
normal definition of the soil units. These indicated variations or
phases of soil properties and landscape features, varying from
delineation to delineation, significantly affect soil behaviour and land
management or use.

It is not always easy to maintain a clear distinction between a soil
phase and a land phase. Soil properties that are frequently used as
phase criteria include depth, surface peat, salinity and physical
disruption. Properties of land that are used include slope, stoniness,
and rockiness.

**2.4 Sampling**

During the course of field investigations and mapping, selected surface
and subsurface soil samples were collected for laboratory analysis.
These samples were used as benchmark references for specific soil
attributes and to assist in general soil characterization. Detailed soil
sampling, description, and laboratory analysis was performed on selected
modal soil sites to provide examples of common soil physical and
chemical characteristics in the study area.

An intensive physical and chemical characterization was conducted at
these sites to an average depth of 1 to 1.5 m. Field evaluations
commonly included:

\- soil classification

\- soil colour

\- soil horizonation

\- soil structure

\- soil drainage/water table characteristics

\- clay films

\- concretions, nodules and cast descriptions

\- root description

\- landscape features and land use

\- stoniness and rockiness

\- soil erosion

The following analysis were carried out:

Particle size Percent weight. Pipette method, with pretreatment for
carbonates and organic carbon.

Total N Percent weight. Semi-micro kjehldahl.

Total organic C Percent weight. CR-12 Leco furnace (Tot C - inorganic C)

Total inorganic C Percent weight of CaCO3 equivalents (%C x 8.333). Acid
digestion and titration.

Organic pH H2O 1:10 soil:H2O (organic soil)

pH H2O 1:2 soil:H2O (mineral soil)

Organic pH CaCl2 1:10 soil:CaCl2 (organic soil)

pH CaCl2 1:2 soil:CaCl2 (mineral soil)

Extractable acidity Percent weight in meq/100 gm. 0.5 N BaCl2 buffered
(with triethanolamine and HCl) saturation with ammonium acetate for
measuring exchange capacity.

Exchange capacity Percent weight in meq/100 gm. 0.5 N BaCl2 buffered
(with triethanolamine and HCl) saturation with ammonium acetate for
measuring exchange capacity.

Exchangeable Ca, Percent weight in meq/100 gm. 0.5 N BaCl2 buffered
(with

Mg, Na, K triethanolamine and HCl) saturation with ammonium acetate for
measuring exchange capacity.

Field Moisture 10th .01 MPa moisture with units being % moisture.
Moisture retention plates.

Saturated moisture .033 MPa moisture with units being % moisture.
Moisture retention plates.

Wilting moisture 1.5 MPa moisture with units being % moisture. Moisture
retention plates.

Note:

1\. A few of the 15 atm moistures have a higher moisture value than the
.33 atm. The problem is very high organic content that prevents the
formation of a proper seal on the pressure plate. (personal
communication Mr. Barry Goetz, lab supervisor).

2\. Field texture determination is done on the soil as is with all the
carbonates present. For that reason the clayey soil samples were rerun
in the Winnipeg lab on samples from which only the organic matter was
removed. In a number of cases there is a dramatic shift in the
percentages silt and clay, resulting in different texture classes. These
results are provided in dBase file 2DTLLABO.dbf.

**2.5 Mapping and Characterization of Soils and Landscapes**

Information on soils and landscapes in the Boreas Northern Study Area
was limited in extent and detail prior to the soils project carried out
under BOREAS. The area was covered in 1972 by a biophysical land survey
(Beke [et]{.underline} [al]{.underline} 1973). A biophysical survey
covering the Sipiwesk (63P) and SE1/4 of Split Lake (64A) NTS sheets (
Veldhuis [et]{.underline} [al]{.underline} 1979) including terrain close
to the the super site area and ancillary sites along the road to Gillam,
provided information on similar soils and landscapes. Data from a soil
climate study on a veneer bog (Mills [et]{.underline} [al]{.underline}
1987) helped to understand the complexity of soils and their thermal
properties, especially as they relate to permafrost distribution.
Detailed soil mapping and sampling projects on a number of sites in the
Thompson area and along the road to Gillam (Veldhuis and Mills 1976;
Veldhuis and Dutchak 1978; Veldhuis and Burachynsky 1979) provided
additional background information.

The soils in the study area were described and mapped along transects,
roads, trails and power line. Information of the terrain between soil
investigation sites was recorded, and ancillary probes were carried out
to ascertain soil properties like permafrost, peat depth, and
stratification. Information on soils were recorded on field sheet and
the data were subsequently transferred to electronic (dBase) files. The
additional field notes augmented by selected information from the field
sheets were transferred to WP files, to provide a type of narrative for
the transects.

Soils described and sampled in detail to provide detailed information
for the most common soils in the study area were collected on the tower
sites, and in the surrounding area (Super Site).

After air drying the soil samples were sieved and the 2 mm fraction
ground to reduce the soil aggregates. Fragments coarser than 2 mm were
separated in classes and expressed as percent weight of the total
sample. The soil samples were subsequently shipped to the Soil Science
Department of The University of Saskatchewan in Saskatoon for analysis.

[2.5.1 Soil Mapping of the Tower Sites]{.underline}

The tower sites were mapped using 1971 and 1972, 1:15 840 scale, B&W
panchromatic aerial photographs. The Old Black Spruce (OBS), Old Jack
Pine (OJP) and Young Jack Pine Sites (YJP) were surveyed along compass
lines radiating from the tower or a location nearby. The transects were
500 m long providing coverage for an area in the form of a circle with 1
km diameter with the tower as centre point. The OJP and YJP were mapped
in that manner along four transects, while the eight transects were
carried out in the OBS site. Soils were investigated at 100 m intervals,
and notes were made about the terrain between soil sites, and a number
of additional soil probes were carried out were a change occurred, to
probe for permafrost or depth of peat.

Four soils were sampled and described in detail in the OJP and YJP sites
and six soils were collected from the OBS site. Four soils were sampled
on the Fen (FEN) tower site, but no transects were done on this site in
1973.

After the field season preliminary maps were produced for the four tower
sites, by interpreting stereoscopically the 1:15 840 scale photos and
transferring the information to 1:5000 scale photo enlargements. The
evaluation of the data and the photo interpretation showed that some
additional information would be needed to improve the mapping.

In 1994 additional transect work was carried out on the OJP, YJP and Fen
Sites. Also the Old Trembling Aspen site was mapped. The transects on
the Fen site were determined by photo pattern, while the transect in the
OTA site were located parallel to each other, starting from the edge of
the road allowance of PTH 392. Two additional soils were sampled of the
YJP site, three of the OJP site, one of the OBS site and five of the FEN
site. Two soil were sampled on the OTA site.

[2.5.2 Soil Mapping of the Super Site]{.underline}

In 1994 an area called the Super Site (SST), and which encompassed all
the tower sites, was selected to be mapped at a scale of 1:100 000 using
1:50 000 scale panchromatic B&W aerial photographs flown in 1978. A
preliminary photo interpretation was carried out prior to the field
work. Because of the difficulty of the terrain and its limited access
most of the soil investigations were carried out along PTH 392, the
Power Transmission Line, a number of trails and by means of foot
traverses starting at the road or transmission line. Three transects
were carried out by being dropped off by helicopter at one point and
picked up at the end of the day at a point at several kilometres
distance. The latter transects provided some information from areas
otherwise out of reach.

**2.6 Maps and Legends**

After the 1994 field work photo interpretation was carried out again and
the maps upgraded. Two types of maps were to be produced. The first map
is a \"hard copy map\" produced on a photomosaic base, the second map is
a GIS (PAMAP-ARC/INFO) based map.

The photo base maps are uncontrolled which results in a somewhat
distorted map. These maps are not geo-referenced and should not be used
to do any area measurements, but may be of use in the field.

The base map for GIS based maps was generated using 1:50 000 scale NTS
maps. The information on these maps is better geo-referenced but still
not ideal. However they can be used to aerial extent measurements, and
if a better (more accurate base) becomes available these maps can be
adjusted to fit the new base. The GIS maps are stored in the form of a
number of layers, which contain information on roads, streams and lakes,
the soil polygon lines and the location of the soil investigation sites.
These layers may be combined in various ways to produce maps most useful
to a particular project.

A dBase based legend for each site area is provided and is to be used
with both types of maps. The link between the maps and the legends is
through the polygon number on the map and the legend. The legend
contains information on segments of the landscape(s) that are delineated
by the map polygon. The type of landform, surficial materials, slopes,
drainage, depth of organic layer, soil development and soil types
associated with the landscape segments are listed.

Explanation of the codes and a description of the classes is provided in
the report. Soil descriptions are also provided in the report. Physical
and chemical data for selected soils can be found in the DTLABO.dbf and
2DTLLABO.dbf files (dBase).

By linking the legend to the GIS maps a variety of maps may be produced
at any scale. Maps showing drainage, depth of organic deposits,
permafrost distribution may be generated by selecting the relevant
fields.

For the tower sites also a narrative legend is provided describing
briefly what is contained in each polygon with respect to materials,
drainage and soils.

**PART 3**

**3 DEVELOPMENT, CLASSIFICATION AND DESCRIPTION OF SOILS**

**3.1 Soil Classification and Development**

The principal factors affecting soil formation are climate, vegetation,
parent material, relief and drainage. The interaction of these soil
forming factors is expressed in the morphological characteristics of
soil. Through observation of these characteristics, it is possible to
classify soils into natural units and to infer their genesis or the
processes involved in their formation.

After Glacial Lake Agassiz disappeared from this area the land became
vegetated and soil development commenced. Carbon dates suggest that peat
formation may have started as early as 6000 years B.P., and possibly
earlier. Because of the topography of the landscape and the infancy of a
drainage network, much of the landscape lacked, and still lacks,
adequate drainage. This condition was favourable to the development of
peat. Peat deposits accumulated in wet depressions, along streams and
margins of lakes, infilling of lakes also took place. All these types pf
peat accumulation continue to this day. Soil formation on the upland
sites commenced at about the same time or earlier. Due to the short time
elapsed since the area emerged from Glacial Lake Agassiz, and the
generally cold, subhumid climate, and the dominance of moderately to
strongly calcareous glacio-lacustrine deposits soil development on fine
to medium textured materials is generally shallow. On coarse textured
glacio-fluvial deposits, which are generally neutral to weakly acidic in
reaction, soil development is slightly deeper, but soils are still
shallow and weakly developed.

[3.1.1 Soils on Fine Textured Glacio-lacustrine Sediments]{.underline}

Most of the glacio-lacustrine deposits consist of clay to heavy clay
textured sediments, which are varved at depth. As the glacio-lacustrine
sediments are commonly stratified with siltier materials, the clay
mantle may be thin and may lie over silt loam to silty clay sediments.
The glacio-lacustrine deposits are calcareous, but the carbonates have
been leached from the upper 30 to 50 cm during soil development. The
parent materials within the control section range from weak to very
strongly calcareous.

The dominant soils developed on these materials are Orthic Gray
Luvisols, Gleyed Gray Luvisols, and various Gleysols. The Luvisolic
soils are characterized by a B horizon enriched with clay eluviated
(leached) from the horizon(s) above and illuviated (deposited) in the B
horizon. Or in other words the B horizon usually has a higher clay
content than the horizon above or below it. Less frequently encountered
are Dark Gray Luvisols and Gleyed Dark Gray Luvisols, which have an A
horizon high in organic matter.

Under the right conditions (stand density, thick duff layer) the
luvisolic soils may contain permafrost within the control section and
are classified as cryic phases of Luvisolic soil types or as Cryosols.
This classification discrepancy is due to the absence of taxonomic type
which recognizes permanently frozen soils with luvisolic properties. The
presence of permafrost in moderately well drained Luvisols will be
discussed in more detail in a later section.

[3.1.2 Soils on Coarse Textured Glacio-fluvial Deposits]{.underline}

The glacio-fluvial deposits in the study area are sandy and gravelly,
although silty deposits occur as well, especially in aprons or in
transition areas to glacio-lacustrine sediment dominated landscapes. The
coarse textured glacio-fluvial parent materials are neutral to weakly
acidic, and the soils that developed are generally weakly developed.
Leached horizons are generally thin (often less than 5 cm thick, and
often broken or mixed with B-horizon material).

The B horizon has some enrichment of amorphous iron and aluminum
compounds, some amorphous organic material, but very little or no
increase in clay content. Occasionally the B horizons are stronger
developed, but this is likely due to particular site conditions
(variation in parent material properties, drainage conditions and aspect
of the site, and possibly vegetation history of the site).

Most of the soils fall taxonomically within the Dystric Brunisol Great
Group of the Canadian Soil Classification System. In this area the
difference is very slight between the two groups and is solely based on
the pH of the upper 30 cm of the solum. Soils within a short distance
from and developed on basically the same material may belong to
different Great Groups. The critical value is a pH of 5.5 and some soils
are slightly more acid (Dystric) and some are more basic (Eutric).

The dominant soils on the glacio-fluvial materials are well drained
Eluviated Dystric Brunisols and Eluviated Eutric Brunisols. Imperfectly
drained areas have Gleyed Dystric or Eutric Brunisols. Poorly drained
lower slopes have usually a thin peat surface layer and the soils are
classified as Orthic or Rego Gleysol, peaty phase soils. Permafrost may
be associated with these materials or soils.

[3.1.3 Soils Developed on Organic Materials]{.underline}

Because of the fine texture of the glacio-lacustrine materials, and the
generally subdued topography of the terrain organic soils of various
types occupy a large proportion of the landscape.

Most of the deep to very deep organic soils appear to have developed in
a fen environment. The peat is dominated by sedge and brown moss
remains. The peat is slightly to moderately well decomposed, but bottom
peats are usually very well decomposed and may consist of aquatic peat.
The peat of frozen peatlands (palsas and peat plateaus) is also mostly
fen peat, but is often capped by a thin to moderately deep sphagnum or
feather moss peat. This surface peat accumulated under bog (ombrotrophic
conditions) since the time permafrost first developed in those
peatlands.

The soils on the fens are dominantly Typic Fibrisols, Mesic Fibrisols
and Fibric Mesisols on deep peat on shallow peat (40-160 cm) equivalent
Terric subgroups are found. The deep, frozen peatlands have Fibric
Organic Cryosols and Mesic Organic Cryosols. On frozen peatlands
shallower than 100 cm Terric Fibric, mesic and Humic Organic Cryosols
are present.

Veneer bogs are widespread throughout the study area and are
characterized by a their shallow peat deposits and hummocky surface.
These peatlands occur on gently sloping terrain that is subject to
frequent forest fires. The fires cause the complete or partial burning
of the peat. Peat development recommences eventually in most of the
area, and, if sufficient time is allowed to elapse and the peat
development becomes deep enough, localized permafrost may develop.

The veneer bogs may be reduced to mineral soil after fire, resulting in
an eutrophic environment, however soon after peat development reoccurs
the sites become increasingly ombrotrophic, causing a change in the
vegetation and in the type of peat being accumulated.

The soils ion the veneer bogs range from Terric Fibrisols to peaty
Gleysols of various kinds to Terric Fibric, Mesic or Humic Organic
Cryosols.

**3.2 Soil Series and Complexes**

[3.2.1 Soils Developed on Calcareous, Fine Textured, Glacio-lacustrine
Sediments]{.underline}

[Soils developed on HC to SIC sediments]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

OGL Sipiwesk SWK Generally finely structured. HC overlying varved HC-SIC

OGL,z Sipiwesk, cryic SWK z Similar to SWK, but has permafrost within
100 cm of the surface

OGL Wabowden WBW Generaly coarse, strong structure in AB and B horizons.
Parent materials similar to SWK.

OGL,z Wabowden, cryic WBW z Similar to SWK,z, but has WBW structure

GLGL Roe Lake ROK Soil similar to SWK, except it is imperfectly drained.

OLG La Perouse PRL Soil similar to SWK or WBW, but is poorly drained.

OLG,p La Perouse, peaty PRL p Similar to above, but has a peaty surface
15-40 cm thick

OG Medard MDR Poorly drained soil without B horizon development

OG,p Medard, peaty MDR p Similar to above, but has a peaty surface
between 15 and 40 cm thick

[Soils developed on HC-C overlying SIC-SICL materials within 50 cm from
the surface]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

OGL Pipun PPU Soil similar to SWK, but has SIC-SICL subsoil (more
calcareous)

GLGL Roe Lake, var1 ROK 1 Similar to above, but imperfectly drained

RG Button BTT Similar to PPU, but poorly drained

RG,p Button, peaty phase BTT p Similar to BTT, but has a peaty surface
between 15 and 40 cm deep

[Soils developed on HC-C overlaying bedrock]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

OGL,l Warren Landing WRL Soil similar to SWK or WBW, but has bedrock
contact witin 100 cm

GLGL,l Turnbull TBL Similar to above, but imperfectly drained

OG,l Tyrrell TYL Similar to above, but poorly drained

[3.2.2 Soils Developed on Fine Textured Alluvial (fluvial)
Deposits]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

GLCUR Grass River GRS Imperfectly to poorly drained cumulic sediments

[3.2.3 Soils Developed on Sandy Glacio-fluvial and Glacio-lacustrine
Deposits]{.underline} (including soils containing fine textured,
glacio-lacustrine layers)

[Soils developed on noncalcareous sand and loamy sand, including soils
with fine sandy layers in the control section]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

EDYB Clarke CLK Sand to loamy sand material.

EDYB Clarke, var1 CLK, 1 Similar to CLK, but contains significant FS
layers in control section

GLEDYB Pakwa PKW Similar to CLK, but imperfectly drained

RG Baldy BDY Poorly drained equivalent of CLK

RG,p Baldy, peaty BDY p Similar to above, but has peaty surface between
15 and 40 cm deep.

[Soils developed on noncalcareous, glacio-fluvial, coarse sand and
gravel deposits]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

EDYB Partridge Crop PCP Stratified CS and VGCS, VCS etc. Usually also
cobbly.

EDYB,h Partridge Crop, humus PCP h Similar to above soil, but has well
developed LF or LFH layer (\>10 cm)

GLEDYB Partridge Beak PCB Stratified CS and VGCS,VCS etc. Usually also
cobbly.

OG Partridge Head PCH Stratified CS and VGCS, VCS etc. Usually also
cobbly.

[Soils developed on noncalcareous, glacio-fluvial or glacio-lacustrine
sand, coarse sand and gravel deposits overlying or containing
significant layers of glacio-lacustrine clay.]{.underline}

[Class]{.underline} [Soil Series Name]{.underline} [Code]{.underline}
[Var]{.underline} [Characteristics/Description]{.underline}

EDYB Young Pine YGP Similar to PCP, but contains clay in the subsoil,
which results in a perched water table in the subsoil during part of the
year.

EDYB Young Pine, var1 YGP 1 Similar to CLK, but contains clay in the
subsoil, which results in a perched water table in the subsoil during
part of the year

GLEDYB Low Pine LWP Similar to YGP, but imperfectly drained, as a result
of a high perched water table.

GLEDYB Low Pine, var1 LWP 1 Similar to YGP1, but imperfectly drained

OG Wet Pine WTP Similar to YGP, but poorly drained, as a result of a
high perched water table.

OG Wet Pine, var1 WTP 1 Similar to YGP1, but poorly drained

[3.2.4 Non-frozen Organic Soils]{.underline}

[Soils developed on brown moss and sedge peat overlying calcareous, fine
textured, glaciolacustrine sediments.]{.underline}

[Class]{.underline} [Soil Series/Complex Name]{.underline}
[Code]{.underline} [Var]{.underline}
[Characteristics/Description]{.underline}

TF Fen, shallow FEN s Shallow (120-160 cm), very fibric fen peat

TYF Fen, deep FEN d Deep (160-300 cm), very fibric fen peat

TYF Fen, very deep FEN v Very deep (\>300 cm), very fibric fen peat

TYF Fen Collapse, deep FCD d Deep (160-300 cm), very fibric fen peat

TYF Fen Collapse, Var1 FCD 1 Deep (160-300 cm), very fibric fen peat
with a deep (\>40 cm) surface water layer

TYF Fen Collapse, very deep FCD v Very deep (\>300 cm), very fibric fen
peat

TYF Fen Collapse, Var2 FCD 2 Very deep (\>300 cm), very fibric fen peat
with a deep (\>40 cm) surface water layer

TMEF Thaw Fen, shallow TFN s Shallow (100-160 cm), stratified fen peat
overlying clay

TMEF Thaw Fen, very shallow TFN w Very shallow (40-100 cm), stratified
fen peat overlying clay

[Soils developed on sphagnum moss peat overlying collapsed palsa and
peat plateau peat materials overlying calcareous, fine textured,
glaciolacustrine sediments.]{.underline}

[Class]{.underline} [Soil Series/Complex Name]{.underline}
[Code]{.underline} [Var]{.underline}
[Characteristics/Description]{.underline}

TYF Bog Collapse, deep BGC d Deep (160-300 cm) peat, consisting of deep
(\>40 cm) sphagnum peat over collapsed peats

TYF Bog Collapse, very deep BGC v Very deep (\>300 cm) peat, consisting
of deep (\>40 cm) sphagnum peat over collapsed peat

[Soils developed on thin peat (40-160 cm) overlying noncalcareous,
glaciofluvial and glaciolacustrine, sand and gravel
deposits]{.underline}

[Class]{.underline} [Soil Series/Complex Name]{.underline}
[Code]{.underline} [Var]{.underline}
[Characteristics/Description]{.underline}

TF Sandy Bog, shallow SYB s Thin peat (40-100) cm dominantly composed in
upper layers of sphagnum moss peat. Usually underlain by a layer of well
decomposed, amorphous peat.

TF Sandy Bog, deep SYB d Similar to above but 100-160 cm deep.

[3.2.5 Permanently Frozen Organic Soils]{.underline}

[Soils developed on sedge peat with sphagnum moss or feather moss
surface layers overlying calcareous, fine textured, glaciolacustrine
sediments.]{.underline}

[Class]{.underline} [Soil Series/Complex Name]{.underline}
[Code]{.underline} [Var]{.underline}
[Characteristics/Description]{.underline}

MEOC Palsa PAA Moderately deep (1-2 m), sedge peat with thin (\<0.6 m)
sphanum cap. High ice content. Peat plateaus and low palsas.

MEOC Palsa, deep phase PAA d Deep to very deep (\>2 m to 5 m), sedge
peat with thin (\<0.6 m) sphagnum. High ice content. High palsas.

FIOC Palsa, variant 2 PAA 2 Similar to PAAd, but has deep sphagnum peat
surface layer

TMEOC Plateau PLT Shallow (\<1 m) sedge and sphagnum peat over
lacustrine clay.

[Soils developed on sphagnum moss peat and/or feather moss peat and
minor sedge peat overlying clacareous, fine textured, glaciolacustrine
sediments]{.underline}

[Class]{.underline} [Soil Series/Complex Name]{.underline}
[Code]{.underline} [Var]{.underline}
[Characteristics/Description]{.underline}

FIOC Cormorant Lake CMK Deep sphagnum peat; peat plateau and palsa.

TMEF Nichols Lake NIC A complex of soils developed on Veneer Bog, which
contains all or some of the following: sphagnum hummocks (TFI, TFIOC),
peaty Gleysols, shallow collapses (TF, TFIM), and minor small palsas
(TMEOC, TFIOC) over clayey deposits

[Class]{.underline} [Soil Series/Complex Name]{.underline}
[Code]{.underline} [Var]{.underline}
[Characteristics/Description]{.underline}

TFIOC Nicols Lake, var1 NIC 1 As above but contains \>10% permafrost on
an aerial basis

TF Nichols Lake, var2 NIC 2 Similar to NIC, but overlies bedrock within
100 cm from the surface

TMEOC Palsa Hummock PLH Shallow organic (0.3-1 m) over clay. Palsa like
in appearance. Mineral subsoil usually strongly mottled.

**3.3 Soil Series, Phases, Variants and Complex Descriptions**

[ATK - ATIK complex]{.underline}

The Atik complex soils form a complex of shallow, organic soils. These
soils are part of veneer bog terrain, which may be composed of all or
some of the following: low and high, small and large sphagnum hummocks,
thin peat veneer, shallow sedge filled collapses, and small palsas.

The vegetation consist of open or clumped black spruce, some tamarack,
willow, feather and sphagnum mosses, ericaceous shrubs and sedges.

The Atik complex soils include poorly drained Terric Mesisols (Atik
series), Terric Fibrisols, Terric Mesic Fibrisols and Terric Fibric
Mesisols. The variation in soils is caused by forest fires, which
infrequently and erratically burn these areas, causing all or some of
the peat to burnt off and varying drainage condition within the
peatland. The Atik soils have developed on little to moderately
decomposed moss and sedge peat. The lower peat is often humified and
amorphous, and overlies calcareous, clayey, glacio-lacustrine sediments.

The Atik soils have been mapped as part of the Nichols Lake (NIC)
complex, which includes all or some of the following associated soils:
La Perouse (LPR), and Medard (MDR) series and peaty phase, Thaw Fen,
very shallow phase (TFNw), and Palsa Hummock (PLH) soils.

[3.3.2 BDY - BALDY series]{.underline}

The Baldy soils have developed on gently sloping to gently undulating
sandy, glacio-fluvial and glacio-lacustrine deposits. The deposits are
generally deep and stratified, and may contain gravelly to loamy layers.
The materials are usually non-calcareous.

The vegetation is dominated by black spruce, willow and mosses. After
fire jack pine may be part of the vegetative mix.

The Baldy soils consist of poorly drained, Rego Gleysols developed on
slightly acidic to neutral sandy (S to LS texture) deposits. Most of the
Baldy soils have developed on reworked glacio-fluvial materials or
glacio-lacustrine deposits, especially in gently sloping areas with
subdued beach ridges and in level areas where shallow sandy materials
overlie clayey materials. The soils are gleyed and mottled and often
strongly iron stained. The water table is high in spring and early
summer, but may drops the control section in average years. The soils
are generally slightly acidic to neutral the upper part of the profile
and are neutral in the subsoil. Coarse fragments are minor and mostly in
the form of some cobbles and fine gravel lenses.

The Baldy soils have a peaty surface layer less than 15 cm thick. An
organic rich A less than 10 cm thick may be present. This horizon grades
into the C horizon. Soils with weak B horizons have been included into
the Baldy mapping unit. The B is characterized by an slight increase
pyrophosphate-extractable Al and Fe. The B grades gradually through a BC
to the C material.

Associated soils are imperfectly drained Pakwa (PKW) soils.

[BDYp - BALDY peaty phase]{.underline}

Baldy, peaty phase soils differ from Baldy series soils in having a
peaty surface 15 to 40 cm thick. The vegetation is more stunted and
consists of black spruce, willow and mosses, including sphagnum mosses.
These soils remain wet for along time, and are slow to thaw in spring.

[BGCd - BOG COLLAPSE deep phase]{.underline}

Bog Collapse, deep phase soils form a complex of organic soils, between
160 and 300 cm deep, that have developed on sedge and brown moss peat
and overlie clayey, calcareous glacio-lacustrine sediments. They
generally occur within the confines of palsa complexes and peat
plateaus.

Vegetation is dominated sphagnum mosses, small ericaceous shrubs, and
some sedge.

The Bog Collapse, deep phase soils consist dominantly of very poorly
drained Typic Fibrisols developed on over 40 cm of weakly decomposed
sphagnum peat overlying sedge and brown moss peat. Mesic Fibrisols and
Fibric Mesisols containing layers of more decomposed peat in the control
section are part of the complex. A thin layer of well decomposed,
amorphous bottom peat usually occurs at the contact with the mineral
subsoil.

The peat is largely derived from peat developed in a fen environment.
When permafrost developed in the fen palsa or peat plateau landforms
were formed, which have quite a different moisture regime. The surface
being raised above the surrounding terrain caused the surface to become
virtually unaffected by nutrient-rich groundwater, which resulted in an
ombrotrophic environment. This caused the development of bog vegetation
with a ground cover dominated by sphagnum mosses. This surface peat
derived from this vegetation is very acidic and nutrient poor.
Consequent thermokarsting caused these landforms to collapse, however
due to the location of the collapses very little or no influence of
nutrient-rich groundwater is possible and the collapses remain in an
ombrotrophic state.

The acid and nutrient poor environment favours the development of
sphagnum growth and the consequent formation of sphagnum peat. As a
result of the surface peat in these landforms is very acidic, although
the underlying peat grades to neutral with depth. The surface peat

is very fibric and has low bulk density. Very watery (hydric) layers may
present below the newly formed sphagnum peat. The underlying
glacio-lacustrine sediments are HC to C textured and are moderately to
very strongly calcareous. The water table is close to the surface for
most of the growing season.

Associated soils are Bog Collapse very deep phase (BGCv), and Palsa,
deep phase (PAAd) soils.

[BGCv - BOG COLLAPSE very deep phase]{.underline}

Bog Collapse, very deep phase soils form a complex of organic soils,
over 300 cm deep, that have developed on sedge and brown moss peat and
overlie clayey, calcareous glacio-lacustrine sediments. They generally
occur within the confines of palsa complexes and peat plateaus.

Vegetation is dominated sphagnum mosses, small ericaceous shrubs, and
some sedge.

The Bog Collapse, deep phase soils consist dominantly of very poorly
drained Typic Fibrisols developed on over 40 cm of weakly decomposed
sphagnum peat overlying sedge and brown moss peat. Mesic Fibrisols and
Fibric Mesisols containing layers of more decomposed peat in the control
section are part of the complex. A thin layer of well decomposed,
amorphous bottom peat usually occurs at the contact with the mineral
subsoil.

The peat is largely derived from peat developed in a fen environment.
When permafrost developed in the fen palsa or peat plateau landforms
were formed, which have quite a different moisture regime.

The surface being raised above the surrounding terrain caused the
surface to become virtually unaffected by nutrient-rich groundwater,
which resulted in an ombrotrophic environment. This caused the
development of bog vegetation with a ground cover dominated by sphagnum
mosses. This surface peat derived from this vegetation is very acidic
and nutrient poor. Consequent thermokarsting caused these landforms to
collapse, however due to the location of the collapses no or very little
influence of nutrient-rich groundwater is possible and the collapses
remain in an ombrotrophic state. The acid and nutrient poor environment
favours the development of sphagnum growth and the consequent formation
of sphagnum peat. As a result of the surface peat in these landforms is
very acidic, although the underlying peat grades to neutral with depth.

The surface peat is very fibric and has low bulk density. Very watery
(hydric) layers may present below the newly formed sphagnum peat. The
underlying glacio-lacustrine sediments are HC to C textured and are
moderately to very strongly calcareous. The water table is close to the
surface for most of the growing season.

Associated soils are Bog Collapse deep phase BGCd), and Palsa, very deep
phase (PAAv) soils.

[BRN - BRANNIGAN CREEK series]{.underline}

The Brannigan Creek series soils have developed on gently to moderately
sloping clayey, glacio-lacustrine blankets. The terrain is slightly
undulating to hummocky as a result of underlying bedrock topography,
which is modified, but not completely masked by the overlying
glacio-lacustrine deposits. The Brannigan Creek soils occupy level and
very gently sloping terrain. They are also found on flat apexes of
subdued hummocky terrain.

Native vegetation is mainly open, evenly spaced black spruce with an
understorey of swamp birch and willow and a ground cover of mixed mosses
and low ericaceous shrubs. This type of vegetation is sometimes, at
least in part, replaced by jack pine, trembling aspen and birch after
fire. Alder, swamp birch and willow shrubs are an important component of
the vegetative community. The ground cover is dominantly feather mosses
and some sphagnum mosses, with dwarf willow and herbs.

The Brannigan Creek series consists of Orthic Gleysol soils developed on
deep, moderately to strongly calcareous clayey (C and HC texture),
glacio-lacustrine sediments. The upper part of the soil consists usually
of a thin (\<10 cm), clay to heavy clay textured, fine granular to
massive, organically rich A horizon. The subsoil (C horizon) is often
varved with silty and clay laminae of varying thicknesses. Runoff is
slow and internal soil permeability is also slow because of the fine
texture of the materials, and lack of good structure close to the
surface. The groundwater level remains close to the surface for a
significant part of the growing season. The water table may be perched
on seasonal frost and/or massive subsoil. Lateral seepage tends to take
place along the contact of the peaty surface layers and the less
permeable, massive clay substrate. In the project soils with deep (\>10
cm),organic rich A horizons (Orthic Humic Gleysols) are included
Brannigan Creek mapping unit.

Associated soils are mostly La Perouse (LPR), Medard (MDR) and their
peaty phases, and Nichols Lake (NIC) soils.

[BRNp - BRANNIGAN CREEK peaty phase]{.underline}

The Brannigan Creek, peaty phase soil is similar to the Brannigan Creek
series, but has a peaty surface layer between 15 and 40 cm thick.
Vegetation is more bog like, with tree growth stunted, and moss
dominated ground cover.

[BTT - BUTTON series]{.underline}

Button soils have developed on gently to moderately sloping clayey to
fine loamy, glacio-lacustrine blankets. The terrain is slightly
undulating to hummocky as a result of underlying bedrock topography,
which is modified, but not completely masked by the overlying
glacio-lacustrine deposits. Button soils occupy lower slopes and fairly
level terrain.

Native vegetation is black spruce, trembling aspen and balsam poplar
with an understorey of willow and alder. Ground cover consists of mixed
mosses and herbs and grasses. This type of vegetation is sometimes, at
least in part, replaced by jack pine, trembling aspen and birch after
fire.

Button series soils consist of poorly drained Rego Gleysol soils
developed on shallow 20-50 cm), moderately calcareous, clayey (C and,
most often, HC textured), glacio-lacustrine sediments overlying fine
loamy (SICL to SIL), very strongly calcareous, glacio-lacustrine
sediments. The subsoil is commonly laminated (varved) with thick layers
of silt and much thinner clay layers. The silty subsoil may rest on
clayey materials. These soils are often alkaline close to the surface.
Internal drainage of Button soils is poor, due to the massive structure
of the silty C horizon. Surface runoff is slight due to landscape
position. Surface texture of the Button soils is clay to heavy clay, and
the upper 5 to 20 cm is often well aggregated (shotty). An organic
matter enriched A horizon (\<10 cm) may be present. Soils with a weakly
developed B have been included in the Button mapping unit.

Associated soils are imperfectly drained Roe Lake, variant 1 (ROK1), and
La Perouse, peaty phase (LPRp) soils.

[BTTp - BUTTON peaty phase]{.underline}

Button, peaty phase soils are much similar to Button series soils, but
differ in the amount of peat overlying the mineral material. These soils
have a peaty surface generally between 15 to 40 cm thick. As a result
vegetation is dominated by black spruce, mosses and willow shrubs. These
soils are wetter, and they take longer to thaw in spring.

[CLK - CLARKE series]{.underline}

The Clarke soils have developed on gently sloping to gently undulating
sandy, glacio-fluvial and glacio-lacustrine deposits. The deposits are
generally deep and stratified, and may contain gravelly to loamy layers.
The materials are usually non-calcareous.

The vegetation is dominated by jack pine, ericaceous shrubs, lichens and
mosses, but black spruce may be a significant a component.

The Clarke soils consist well to moderately well drained, Eluviated
Dystric Brunisols developed on slightly acidic to neutral sandy (S to LS
texture) deposits. Most of the deposits have been laid down as
glacio-fluvial materials, but some have been deposited in glacial lakes
or by the reworking of glacio-fluvial materials by lake waters
(glacio-lacustrine materials). The soils are generally moderately acidic
in the upper part of the profile and become slightly acidic to neutral
in the subsoil. Coarse fragments are minor and mostly in the form of
some cobbles and fine gravel lenses.

The duff layer is thin (2-5 cm), and generally lacks a H horizon thicker
than 0.5 to 1 cm. The eluviated A is also thin (3 to 6 cm), and is often
broken due to windthrow. The B is generally weakly developed and is
characterized by an slight increase pyrophosphate-extractable Al and Fe.
The B grades gradually through a BC to the C material.

Associated soils are Clarke, variant 1 (CLK1) soils and other variant
soils (with thin clay layers for example). Other associated soils are
coarse textured Partridge Crop (PCP) soils, and imperfectly drained
Pakwa (PKW) soils.

[CLK1 - CLARKE variant 1]{.underline}

The Clarke variant 1 soils are very much like the Clarke series soils,
but differ in containing significant layers of fine sand and/or loamy
fine sand within the control section. Included in this group of soils
are soils very much like Clarke series soils, but having thin clay
layers in part of the control section (See Young Pine, variant 1). These
soils have a slightly better water retention capability, resulting in
increased water availability for vegetative growth.

[CMK - CORMORANT LAKE complex]{.underline}

Cormorant Lake complex soils form a complex of permanently frozen,
organic soils, between 200 to 500 cm deep, that have developed on deep
sphagnum peat, which may overlie sedge and brown moss peat. The mineral
subsoil is calcareous, clayey, glacio-lacustrine sediment. These soils
occur on high palsas, and palsa complexes and peat plateaus. The palsas
rise several meters above the surrounding, nonfrozen terrain, while the
surface of peat plateaus is about one meter above the nonfrozen terrain.
The elevation of the surface is caused by the accumulation of excess ice
(in excess of pore space in nonfrozen peat and mineral deposits) in the
subsoil.

The vegetation is dominated by black spruce with a ground cover of
sphagnum moss, and ericaceous shrubs. Black spruce cover is usually open
on both palsas and peat plateaus.

The Cormorant Lake complex soils consist of poorly drained, Fibric
Organic Cryosols developed on 100 to 300 cm (and deeper) of very acid,
fibric sphagnum moss peat, which may overlie moderately decomposed
slightly acidic to neutral sedge and brown moss peat, which accumulated
in a fen environment. The sphagnum peat developed may have started
before or after permafrost caused the surface to be raised above the
surrounding terrain. This sphagnum accumulation occurred in an
ombrotrophic environment resulting in low nutrient status of the peat.
The underlying sediments are calcareous, clayey and glacio-lacustrine
origin.

The permafrost extends through the organic materials well into the
underlying mineral sediments Ice is in the form of veins and lenses, and
also in the form of layers (15 to 50 cm) of pure ice. The active layer
varies with density of tree cover, and surface configuration, but is
generally between 45 and 65 cm deep. In the latter part of the growing
season the surface peat may become dry.

The Cormorant Lake complex soils close association with Fen Collapse,
deep and very deep phase (FNCd and FNCv), Fen, deep and very deep
phase(FENd and FENv), and Bog Collapse, deep and very deep phase (BGCd
and BGCv) soils.

[FCDd - FEN COLLAPSE deep phase]{.underline}

Fen Collapse, deep phase soils form a complex of organic soils,
approximately 160 to 300 cm deep, that have developed on sedge and brown
moss peat and overlie clayey, calcareous glacio-lacustrine sediments.
They occur along the margins of palsas and peat plateaus.

Vegetation is dominated by sedges, and brown mosses, and some sphagnum
mosses. Swamp birch is sometimes present.

The Fen Collapse, deep phase soils consist dominantly of very poorly
drained Typic Fibrisols developed on weakly decomposed sedge and brown
moss peat. Mesic Fibrisols and Fibric Mesisols containing layers of more
decomposed peat in the control section are part of the complex. A thin
layer of well decomposed, amorphous bottom peat usually occurs as the
contact with the mineral subsoil.

The peat is largely of peat developed in a fen environment. When
permafrost developed the fen became palsa or peat plateau landforms,
which have quite a different moisture regime. By being raised above the
surrounding terrain the surface becomes virtually unaffected by
nutrient-rich groundwater, resulting in an ombrotrophic environment.
This results in a bog vegetation with a ground cover dominated by
sphagnum mosses. This causes the surface peat to become very acidic and
nutrient poor. Consequent thermokarsting caused these landforms to
collapse and to return to a stage in which, once again, nutrient-rich
groundwater affects the vegetation and peat development. As a result of
thermokarsting some of the peat slumps and layers will be mixed.

The peat accumulated since the collapse formed is usually very fibric
and has low bulk density. Also very watery (hydric) layers may present
in the peat profile. The peat is generally slightly acidic in the
surface and becomes neutral some distance below the surface. The
underlying glacio-lacustrine sediments are generally HC to C textured
and are moderately to very strongly calcareous. The water table is at or
close to the surface for most of the growing season.

Associated soils are Fen Collapse, very deep phase (FCDv), Fen Collapse,
variant 1 and 2 (FCD1 and FCD2), and Fen, very deep and deep phase (FENv
and FENd) soils.

[FCD1 - FEN COLLAPSE variant 1]{.underline}

The Fen Collapse, variant 1 soils are similar to the Fen Collapse, deep
phase soils, and have gone through similar developmental stages. Again
they form a complex of organic soils, approximately 160 to 300 cm deep,
that have developed on sedge and brown moss peat and overlie clayey,
calcareous glacio-lacustrine sediments and occur along the margins of
palsas and peat plateaus. Because these soils are found in recent
collapses the surface consists basically of a layer of water 40 cm or
more deep. This layer contains very little peat. The underlying peat is
similar to the one described for Fen Collapse, deep phase soils.

The vegetation is dominated by sedges.

Associated soils are Fen Collapse, deep phase (FCDd) soils.

[FCDv - FEN COLLAPSE very deep phase]{.underline}

Fen Collapse, very deep phase soils form a complex of organic soils,
over 300 cm deep, that have developed on sedge and brown moss peat and
overlie clayey, calcareous glacio-lacustrine sediments. They occur along
the margins of palsas and peat plateaus.

Vegetation is dominated by sedges, and brown mosses, and some sphagnum
mosses. Swamp birch is sometimes present.

The Fen Collapse, very deep phase soils consist dominantly of very
poorly drained Typic Fibrisols developed on weakly decomposed sedge and
brown moss peat. Mesic Fibrisols and Fibric Mesisols containing layers
of more decomposed peat in the control section are part of the complex.
A thin layer of well decomposed, amorphous bottom peat usually occurs as
the contact with the mineral subsoil.

The peat is largely derived from peat developed in a fen environment.
When permafrost developed in the fen palsa or peat plateau landforms
were formed, which have quite a different moisture regime. The surface
being raised above the surrounding terrain caused the surface to become
virtually unaffected by nutrient-rich groundwater, which resulted in an
ombrotrophic environment. This caused the development of bog vegetation
with a ground cover dominated by sphagnum mosses. This surface peat
derived from this vegetation is very acidic and nutrient poor.
Consequent thermokarsting caused these landforms to collapse and to
return to a stage in which, once again, nutrient-rich groundwater
affects the vegetation and peat development. As a result of
thermokarsting some of the peat slumps and layers will be mixed.

The peat accumulated since the collapse formed is usually very fibric
and has low bulk density. Also very watery (hydric) layers may present
in the peat profile. The peat is generally slightly acidic in the
surface and becomes neutral some distance below the surface. The
underlying glacio-lacustrine sediments are generally HC to C textured
and are moderately to very strongly calcareous. The water table is at or
close to the surface for most of the growing season.

Associated soils are Fen Collapse, deep phase (FCDd), Fen Collapse,
variant 1 and 2 (FCD1 and FCD2), and Fen, very deep and deep phase (FENv
and FENd) soils.

[FCD2 - FEN COLLAPSE variant 2]{.underline}

The Fen Collapse, variant 2 soils are similar to the Fen Collapse, very
deep phase soils, and have gone through similar developmental stages.
Again they form a complex of organic soils, and are more than 300 cm
deep. The soils have developed on sedge and brown moss peat and overlie
clayey, calcareous glacio-lacustrine sediments, and these soils occur
along the margins of palsas and peat plateaus. Because these soils are
found in recent collapses the surface consists basically of a layer of
water 40 cm or more deep. This layer contains very little peat. The
underlying peat is similar to the one described for Fen Collapse, very
deep phase soils.

The vegetation is dominated by sedges.

Associated soils are Fen Collapse, very deep phase (FCDv) soils.

[FENs - FEN shallow phase]{.underline}

Fen, shallow phase soils form a complex of organic soils, approximately
120 to 160 cm deep, that have developed on sedge and brown moss peat and
overlie clayey, calcareous glacio-lacustrine sediments. They occur in
small depressions and along the margins of basin fens.

Vegetation is dominated by sedges, and brown mosses. Swamp birch,
tamarack and herbs may be present.

The Fen, shallow phase soils consist dominantly of very poorly drained
Terric Fibrisols developed on weakly decomposed sedge and brown moss
peat. Terric Mesic Fibrisols and Terric Fibric Mesisols containing
layers of more decomposed peat are part of the complex. A thin layer of
well decomposed, amorphous bottom peat usually occurs as the contact
with the mineral subsoil. The peat is moderately to slightly acid in the
surface, but most of the peat is slightly acid to neutral and the peat
becomes weakly alkaline in the bottom layers. The underling
glacio-lacustrine sediments are generally HC to C textured and are
moderately to very strongly calcareous. The water table is at or close
to the surface for most of the growing season. The waters are
nutrient-rich (eutrophic or minerotrophic) through runoff from mineral
soils.

Associated soils are Fen, deep phase (FENd) and Thaw Fen, shallow phase
(TFNs) soils.

[FENd - FEN deep phase]{.underline}

Fen, deep phase soils form a complex of organic soils, approximately 160
to 300 cm deep, that have developed on sedge and brown moss peat and
overlie clayey, calcareous glacio-lacustrine sediments. They occur in
large depressions and in infilled lakes (basin fens).

Vegetation is dominated by sedges, and brown mosses. Swamp birch,
tamarack and herbs may be present.

The Fen, deep phase soils consist dominantly of very poorly drained
Typic Fibrisols developed on weakly decomposed sedge and brown moss
peat. Mesic Fibrisols and Fibric Mesisols containing layers of more
decomposed peat are part of the complex. A thin layer of well
decomposed, amorphous bottom peat usually occurs as the contact with the
mineral subsoil. The peat is moderately to slightly acid in the surface,
but most of the peat is slightly acid to neutral and the peat becomes
weakly alkaline in the bottom layers. The underlying glacio-lacustrine
sediments are generally HC to C textured and are moderately to very
strongly calcareous. The water table is at or close to the surface most
if the growing season. The waters are mainly nutrient-rich and
minerotrophic through runoff from mineral soils.

Associated soils are Fen, shallow phase (FENs) and Fen Collapse, deep
phase FCDd) soils.

[FENv - FEN very deep phase]{.underline}

Fen, very deep phase soils form a complex of organic soils, more than
300 cm deep, that have developed on sedge and brown moss peat and
overlie clayey, calcareous glacio-lacustrine sediments. They occur in
large depressions and in infilled lakes (basin fens).

Vegetation is dominated by sedges, and brown mosses. Swamp birch,
tamarack and herbs may be present.

The Fen, very deep phase soils consist dominantly of very poorly drained
Typic Fibrisols developed on weakly decomposed sedge and brown moss
peat. Mesic Fibrisols and Fibric Mesisols containing layers of more
decomposed peat are part of the complex. A thin layer of well
decomposed, amorphous bottom peat usually occurs as the contact with the
mineral subsoil. The peat is moderately to slightly acid in the surface,
but most of the peat is slightly acid to neutral and the peat becomes
weakly alkaline in the bottom layers. The underlying glacio-lacustrine
sediments are generally HC to C textured and are moderately to very
strongly calcareous. The water table is at or close to the surface most
if the growing season. The waters are mainly nutrient-rich and
minerotrophic through runoff from mineral soils.

Associated soils are Fen, deep phase (FENd) soils.

[GRS - GRASS RIVER complex]{.underline}

Grass River soils have developed on clayey and fine loamy, alluvial
materials deposited along rivers and creeks. The slopes are generally
gentle, except there where streams have cut into previously deposited
materials.

Vegetation varies with position along the banks and ranges from sedge,
alder and willow to balsam poplar dominated communities.

The Grass River complex consists of moderately well drained Cumulic
Regosols, imperfectly drained Gleyed Cumulic Regosols, and poorly
drained Rego Gleysols. All soils are characterized by stratification
caused by frequent flooding and the consequent deposition of fresh
alluvial material. As the alluvial material is derived from the
glacio-lacustrine deposits the materials are strongly calcareous and
generally clayey. Profile development is minimal, but the soils are
generally high in organic carbon due to incorporation of surface litter
in the soil.

[LPR - LA PEROUSE series]{.underline}

La Perouse soils have developed on gently to moderately sloping clayey,
glacio-lacustrine blankets. The terrain is slightly undulating to
hummocky as a result of underlying bedrock topography, which is
modified, but not completely masked by the overlying glacio-lacustrine
deposits. La Perouse soils occupy level and very gently sloping terrain.
They are also found on flat apexes of subdued hummocky terrain.

Native vegetation is mainly open, evenly spaced black spruce with an
understorey of swamp birch and willow and a ground cover of mixed mosses
and low ericaceous shrubs. This type of vegetation is sometimes, at
least in part, replaced by jack pine, trembling aspen and birch after
fire. Alder, swamp birch and willow shrubs are an important component of
the vegetative community. The ground cover is dominantly feather mosses
and some sphagnum mosses, with dwarf willow and herbs.

La Perouse series soils consist of Orthic Luvic Gleysol soils developed
on deep, moderately to strongly calcareous, fine textured,
glacio-lacustrine sediments. The surface textures of the La Perouse
soils is clay to heavy clay. The soils are clay and heavy clay
throughout, but sediments grade to dominantly clay materials containing
thin, silty textured varves in the C horizon. The thin surface organic
layer is generally peaty and consists of slightly decomposed mosses (Of
horizon) overlying an amorphous Oh. A thin organic enriched A overlies a
poorly developed eluviated A, which in turn overlies an illuviated B
horizon. These soils are poorly drained although evidence of gleying is
weakly expressed and is often lacking completely in the area studied.
Excess moisture in spring appears to move through the organic mat and
over and through the upper part of the mineral soil. Internal soil
permeability is moderate in the upper solum, but low in the subsoil.

Associated soils are imperfectly drained Roe lake (ROK) soils, La
Perouse, peaty phase (LPRp) soil and other soils belonging to the
Nichols Lake (NIC) complex.

[LPRp - La PEROUSE peaty phase]{.underline}

La Perouse, peaty phase soils are much similar to La Perouse series
soils, but differ in the amount of peat overlying the mineral soils. The
peaty phase soils have a peaty surface generally between 15 to 40 cm
thick. As a result vegetation is generally more stunted, the soils are
wetter, and they take longer to thaw in spring.

[LWP - LOW PINE series]{.underline}

Low Pine soils have developed on gently to moderately sloping or
hummocky, coarse sandy to gravelly, glacio-fluvial deposits having fine
textured (C and CL textured) subsoil within or just below 100 cm depth.
The presence of these finer textured layers suggest a complex deposition
history. The fine textured materials tend to be calcareous, suggesting
glacio-lacustrine origin. The coarse textured surface deposits may be in
part reworked by lake waters and strandlines (beaches) may be present.

The vegetative community is dominated by jack pine, ericaceous shrubs
(especially blueberry), mosses and lichens. Black spruce is usually
present. Vegetative growth varies and is probably affected by the fire
history of a particular area. Frequent, intense burns will tend to
deplete nutrient supply.

The Young Pine soils consist of imperfectly drained Eluviated Dystric
Brunisols developed on slightly acidic to neutral, sandy and gravelly
(CS, GRCS and VGCS), glacio-fluvial deposits overlying clayey (HC, C) or
fine loamy (CL) sediments. The sandy and gravelly soil material is
stratified, and usually contains one or more very gravelly layers. The
composition and thickness of the duff layer (LFH) depends on fire
history of the area. The organic surface is generally in the Young Jack
Pine area (often \<4 cm), and lacks a H horizon. In the Old Jack Pine
area some sections have very thin LF layers, while in some localities
they are 5 to 8 cm thick and include a thin H. The eluviated A is
strongly acidic, but thin and overlies a weak B. A transitional BC
separates the B and C horizons, which are slightly acidic to neutral.
The C becomes mottled and iron stained some distance above the clayey
layer. A perched water table persists well into the growing season.
Internal drainage is rapid in the coarse textured section of the
profile. Coarse fragments in the form of cobbles and stones are present
in the surface of most and may be locally plentiful.

Associated soils are Partridge Crop (PCP) and Young Pine (YGP) soils.

[LWP1 - LOW PINE variant 1]{.underline}

The Low Pine, variant 1 soils have developed on gently sloping to gently
undulating sandy, glacio-fluvial and glacio-lacustrine deposits. The
deposits consist of sandy materials overlying subsoil materials
containing fine textured glacio-lacustrine sediments.deposits are
generally stratified, and may contain gravelly to clayey layers.

The vegetation is dominated by jack pine, ericaceous shrubs, lichens and
mosses after fire, but black spruce and alder will become dominant at
time progresses.

The Low Pine, variant 1 soils consist of imperfectly drained, Gleyed
Eluviated Dystric Brunisols developed on slightly acidic to neutral
sandy (S to LS texture) deposits. Most of the Pakwa soils have developed
on reworked glacio-fluvial materials or glacio-lacustrine deposits,
especially in gently sloping areas with subdued beach ridges. The soils
are mottled and iron stained at a depth of about 50 cm from the surface.
A water table is usually present in spring and early summer, but drops
well below the control section in average years.The soils are generally
moderately acidic in the upper part of the profile and become neutral in
the subsoil. The fine textured subsoil or layers often contains free
carbonates and is neutral to slightly alkaline. Coarse fragments are
minor and mostly in the form of some cobbles and fine gravel lenses.

The duff layer is about 5 to 8 cm thick, and generally has a thin H
horizon (1 to 2 cm). The eluviated A varies in depth but is usually 5 to
8 cm thick. The upper part of the B is usually strongly developed but
thin, but grades rapidly in a weakly developed B horizon. The B horizon
is characterized by an slight increase pyrophosphate-extractable Al and
Fe. The B grades gradually through a BC to the C material.

Associated soils are Clarke (CLK), and Pakwa (PKW) soils.

[MDR - MEDARD series]{.underline}

The Medard series soils have developed on gently to moderately sloping
clayey, glacio-lacustrine blankets. The terrain is slightly undulating
to hummocky as a result of underlying bedrock topography, which is
modified, but not completely masked by the overlying glacio-lacustrine
deposits. The Medard soils occupy level and very gently sloping terrain.
They are also found on flat apexes of subdued hummocky terrain.

Native vegetation is mainly open, evenly spaced black spruce with an
understorey of swamp birch and willow and a ground cover of mixed mosses
and low ericaceous shrubs. This type of vegetation is sometimes, at
least in part, replaced by jack pine, trembling aspen and birch after
fire. Alder, swamp birch and willow shrubs are an important component of
the vegetative community. The ground cover is dominantly feather mosses
and some sphagnum mosses, with dwarf willow and herbs.

The Medard series consists of Rego Gleysol soils developed on deep,
moderately to strongly calcareous clayey (C and HC texture),
glacio-lacustrine sediments. The upper part of the soil consists usually
of a thin (\<10 cm), clay to heavy clay textured, fine granular to
massive, organically rich A horizon. The subsoil (C horizon) is often
varved with silty and clay laminae of varying thicknesses. Runoff is
slow and internal soil permeability is also slow because of the fine
texture of the materials, and lack of good structure close to the
surface. The groundwater level remains close to the surface for a
significant part of the growing season. The water table may be perched
on seasonal frost and/or massive subsoil. Lateral seepage tends to take
place along the contact of the peaty surface layers and the less
permeable, massive clay substrate.

In the project soils with deep (\>10 cm), organic rich A horizons (Rego
Humic GleysoLs) have been included in the Medard mapping unit.

Associated soils are mostly La Perouse (LPR), Brannigan Creek (BRN)
soils, and their peaty phases, and other Nichols Lake (NIC) complex
soils.

[MDRp - MEDARD peaty phase]{.underline}

The Medard, peaty phase soils are characterized by a 15 to 40 cm thick
layer of mesic forest peat on the surface. They may have a thin, dark
gray Ah horizon less than 5 cm thick. However, most Medard soils have
little or no A horizon and are characterized by a strongly gleyed,
yellowish brown or greyish brown, pseudo granular clay subsoil
immediately underlying the thin, peaty surface. This subsoil grades into
a greyish brown varved clay.

Associated soils are mostly La Perouse, peaty phase LPRp), Atik (ATK)
complex and Nichols Lake (NIC) complex soils.

[NIC - NICHOLS LAKE complex]{.underline}

The Nichols Lake complex soils form a complex of frozen and nonfrozen,
shallow organic soils, peaty and nonpeaty gleysolic soils. These soils
are part of veneer bog terrain, which may be composed of all or some of
the following: low and high, small and large sphagnum hummocks, thin
peat veneer, shallow sedge filled collapses, and small palsas.

The vegetation consist of open or clumped black spruce, some tamarack,
willow, feather and sphagnum mosses, ericaceous shrubs and sedges.

The Nichols Lake complex soils include poorly drained Terric Fibrisols,
Terric Mesic Fibrisols, Mesic Organic Cryosols (Nichols Lake series),
Terric Fibric Organic Cryosols, Orthic and Luvic Gleysols and their
peaty phases. The complexity of the soils is caused by forest fires,
which infrequently and erratically burn these areas, causing all or some
of the peat to burnt off. This changes the drainage and climate of the
soils, the vegetation and the soil development. Peat development will
start again in the severely burnt areas through paludification, or
continues in areas that were less affected by the forest fire.

Permafrost is present in this terrain, but covers usually only small
areas, and is mostly confined to larger sphagnum hummocks or areas that
are well shaded. The permafrost is usually not deep, and may occur as
shallow lenses under the hummocks. Small collapse depressions indicative
of more widespread permafrost in the past, and the development of small
palsas add to the complexity of the terrain and its soils.

The surface peat is generally very acidic, fibric sphagnum and/or
feather moss peat, which may rest on moderately decomposed moss peat, or
strongly decomposed, amorphous peat, which usually contains large
quantities of charcoal. The underlying mineral soil is calcareous,
clayey, glacio-lacustrine sediments. The mineral soil often is well
developed with eluviated A and illuviated B horizons. Gleying and/or
mottling may be completely lacking in these soils, although they are wet
for most of the year.

Included in the complex are are Atik (ATK), La Perouse (LPR), and Medard
(MDR) series and their peaty phases, Thaw Fen, very shallow phase
(TFNw), and Palsa Hummock (PLH) soils.

[NIC1 - NICHOLS LAKE variant 1]{.underline}

The Nichols Lake, variant 1 soils form a complex of soils similar to the
Nichols Lake complex, but have at least 10% permafrost (Terric Fibric
and Mesic Organic Cryosols) on an aerial basis.

[NIC2 - NICHOLS LAKE variant 2]{.underline}

The Nichols Lake, variant complex soils form a complex of soils somewhat
similar to the Nichols lake complex. These soils have bedrock at
approximately 100 cm depth from the surface. They occur on veneer bog
developed in depressional areas on bedrock. The peat deposits is
generally more uniform in depth, and gleysols occur usually only along
the margins of the unit. Unconsolidated mineral material, if present,
are usually shallow over bedrock, and consist of glacio-lacustrine,
glacio-fluvial or till deposits. Thus the Nichols Lake, variant 2 soils
consist dominantly of frozen and nonfrozen, shallow organic soils.

The vegetation consists of open or clumped black spruce, willow, feather
and sphagnum mosses, ericaceous shrubs and sedges.

The Nichols Lake, variant 2 soils include poorly drained, Terric and
Typic Fibrisols, Mesic Fibrisols and Terric Mesic Fibrisols, and Terric
Fibric Organic Cryosols. The complexity of the soils is caused by forest
fires, which occur frequently on bedrock areas these areas. This causes
the peat to be burnt back, and the formation of well decomposed and
charcoal rich layers in the peat deposits.

Permafrost is present in this terrain, but covers usually only small
areas, and is mostly confined to larger sphagnum hummocks or areas that
are well shaded. The permafrost is usually not deep, and may occur as
shallow lenses under the hummocks. The surface peat is generally very
acidic, fibric sphagnum and/or feather moss peat, which may rest on
moderately decomposed moss peat, or strongly decomposed, amorphous peat,
which usually contains large quantities of charcoal. The underlying
mineral soil ranges from calcareous, clayey, glacio-lacustrine sediments
to sandy and gravelly, acidic till.

[PAA - PALSA complex]{.underline}

Palsa complex soils form a complex of permanently frozen, organic soils,
between 100 and 200 cm deep, that have developed on sedge and brown moss
peat, overlain by a thin to moderately deep (\<60 cm), surface layer of
sphagnum and/or feather moss peat. The mineral subsoil is calcareous,
clayey, glacio-lacustrine sediment. These soils occur on low to medium
high palsas, palsa complexes and peat plateaus, which rise one to two
meters above the nonfrozen terrain as result of excess ice accumulation
in the subsoil.

The vegetation is dominated by black spruce with a ground cover of
sphagnum, feather mosses, and ericaceous shrubs. Black spruce cover on
palsas is usually closed, but is open on peat plateaus.

The Palsa soils consist of poorly drained, Mesic Organic Cryosols and
Fibric Organic Cryosols developed on 15 to 60 cm of very acid, fibric
sphagnum and/or feather moss peat, which overlies moderately decomposed
slightly acidic to neutral sedge and brown moss peat, which accumulated
in a fen environment. The sphagnum and feather moss peat developed after
permafrost caused the surface to be raised above the surrounding
terrain. This resulted in a change in moisture regime and lower nutrient
status of soil water (ombrotrophic conditions). As a result bog
vegetation dominated by sphagnum, feather mosses and black spruce
developed. The bottom peat is usually very well decomposed and
amorphous. This peat lies over top of strongly calcareous, clayey
glacio-lacustrine sediments.

The permafrost extends through the organic materials well into the
underlying mineral sediments Ice is in the form of veins and lenses, and
also in the form of layers (15 to 50 cm) of pure ice. The active layer
varies with type of vegetative cover, type of peat and surface
configuration, but is generally between 45 and 65 cm deep. In the latter
part of the growing season the surface peat may become very dry.

The Palsa complex soils occur in close association with Fen Collapse,
deep phase (FNCd), Fen, deep phase (FENd), and Bog Collapse, deep phase
(BGCd) soils.

[PAAd - PALSA deep phase]{.underline}

Palsa, deep phase soils form a complex of permanently frozen, organic
soils, between 200 to 500 cm deep, that have developed on sedge and
brown moss peat, overlain by a thin to moderately deep (\<60 cm),
surface layer of sphagnum and/or feather moss peat. The mineral subsoil
is calcareous, clayey, glacio-lacustrine sediment. These soils occur on
high palsas, and palsa complexes and peat plateaus. The palsas rise
several meters above the surrounding, nonfrozen terrain, while the
surface of peat plateaus is about one meter above the nonfrozen terrain.
The elevation of the surface is caused by the accumulation of excess ice
(in excess of pore space in nonfrozen peat and mineral deposits) in the
subsoil.

The vegetation is dominated by black spruce with a ground cover of
sphagnum, feather mosses, and ericaceous shrubs. Black spruce cover on
palsas is usually closed, but is open on peat plateaus.

The Palsa, deep phase soils consist of poorly drained, Mesic Organic
Cryosols and Fibric Organic Cryosols developed on 15 to 60 cm of very
acid, fibric sphagnum and/or feather moss peat, which overlies
moderately decomposed slightly acidic to neutral sedge and brown moss
peat, which accumulated in a fen environment. The sphagnum and feather
moss peat developed after permafrost caused the surface to be raised
above the surrounding terrain. This resulted in a change in moisture
regime and lower nutrient status of soil water (ombrotrophic
conditions). As a result bog vegetation dominated by sphagnum, feather
mosses and black spruce developed. The bottom peat is usually very well
decomposed and amorphous. This peat lies over top of strongly
calcareous, clayey glacio-lacustrine sediments.

The permafrost extends through the organic materials well into the
underlying mineral sediments Ice is in the form of veins and lenses, and
also in the form of layers (15 to 50 cm) of pure ice. The active layer
varies with type of vegetative cover, type of peat and surface
configuration, but is generally between 45 and 65 cm deep. In the latter
part of the growing season the surface peat may become very dry.

The Palsa complex soils occur in close association with Fen Collapse,
very deep phase (FNCv), Fen, very deep phase (FENv), and Bog Collapse,
very deep phase (BGCv) soils.

[PAA2 - PALSA variant 2]{.underline}

Palsa, variant 2 soils form a complex of permanently frozen, organic
soils, between 200 to 500 cm deep, that have developed on sedge and
brown moss peat, which is overlain by a deep (.60 cm), surface layer of
sphagnum moss peat. The mineral subsoil is calcareous, clayey,
glacio-lacustrine sediment. These soils occur on high palsas, and palsa
complexes and peat plateaus. The palsas rise several meters above the
surrounding, nonfrozen terrain, while the surface of peat plateaus is
about one meter above the nonfrozen terrain. The elevation of the
surface is caused by the accumulation of excess ice (in excess of pore
space in nonfrozen peat and mineral deposits) in the subsoil.

The vegetation is dominated by black spruce with a ground cover of
sphagnum moss, and ericaceous shrubs. Black spruce cover is usually open
on both palsas and peat plateaus.

The Palsa, variant 2 soils consist of poorly drained, Fibric Organic
Cryosols developed on 60 to 120 cm of very acid, fibric sphagnum moss
peat, which overlies moderately decomposed slightly acidic to neutral
sedge and brown moss peat, which accumulated in a fen environment. The
sphagnum peat developed after permafrost caused the surface to be raised
above the surrounding terrain. This resulted in a change in moisture
regime and lower nutrient status of soil water (ombrotrophic
conditions). As a result bog vegetation dominated by sphagnum and black
spruce developed. The bottom peat is usually very well decomposed and
amorphous. This peat lies over top of strongly calcareous, clayey
glacio-lacustrine sediments.

The permafrost extends through the organic materials well into the
underlying mineral sediments Ice is in the form of veins and lenses, and
also in the form of layers (15 to 50 cm) of pure ice. The active layer
varies with density of tree cover, type of peat and surface
configuration, but is generally between 45 and 65 cm deep. In the latter
part of the growing season the surface peat may become very dry.

The Palsa complex soils occur in close association with Fen Collapse,
very deep phase (FNCv), Fen, very deep phase (FENv), and Bog Collapse,
very deep (BGCv) phase soils.

[PCB - PARTRIDGE BEAK series]{.underline}

Partridge Beak soils have developed on gently to moderately sloping or
hummocky, coarse sandy to gravelly, glacio-fluvial deposits. These
deposits may be in part reworked by lake waters and strandlines
(beaches) may be present.

The vegetative community is dominated by jack pine, ericaceous shrubs
(especially blueberry), mosses and lichens. White birch, black spruce
and alder are locally significant vegetation components. Vegetative
growth varies and is probably affected by the fire history of a
particular area. Frequent, intense burns will tend to deplete the
nutrient supply.

The Partridge Beak soils consist of imperfectly drained Gleyed Eluviated
Dystric Brunisols developed on slightly acidic to neutral, sandy and
gravelly (CS, GRCS and VGCS), glacio-fluvial deposits. The soil material
is stratified, and usually contains one or more very gravelly layers.
The composition and thickness of the duff layer (LFH) depends on fire
history of the area. The organic surface is generally thin in the Young
Jack Pine area (often \<2 cm), and lacks a H horizon. In the Old Jack
Pine area some sections have very thin LF layers, while in some
localities they are 5 to 8 cm thick and have a thin H. The eluviated A
is strongly acidic, but thin and overlies a weak B. A transitional BC
separates the B and C horizons, which are slightly acidic to neutral.
Coarse fragments in the form of cobbles and stones are present in most
of the areas are locally plentiful, especially in the surface (stoniness
class 4 and 5).

The Partridge Beak soils have good internal drainage, but have some
excess moisture during part of the growing season as a result of lower
slope landscape position.

Associated soils are Partridge Crop (PCP), Young Pine (YGP) and Low Pine
(LWP) soils.

[PCH - PARTRIDGE HEAD series]{.underline}

Partridge Head soils have developed on gently to moderately sloping or
hummocky, coarse sandy to gravelly, glacio-fluvial deposits. These
deposits may be in part reworked by lake waters and strandlines
(beaches) may be present.

The vegetative community is dominated by black spruce, alder, willow and
mosses. Jack pine is present after forest fire.

The Partridge Head soils consist of poorly drained Orthic Gleysols
developed on slightly acidic to neutral, sandy and gravelly (CS, GRCS
and VGCS), glacio-fluvial deposits. The soil material is stratified, and
usually contains one or more very gravelly layers. The organic surface
is peaty and less than 15 cm thick. The peaty material is largely
derived from mosses. The thin (\< 10 cm) is organically enriched and
overlies a gleyed B. The subsoil is strongly gleyed. The water table is
high in spring and early summer, and in average years may persist within
1 m from the surface. Coarse fragments in the form of cobbles and stones
are present in most of the areas are locally plentiful, especially in
the surface (stoniness class 4 and 5). Included in the mapping unit are
soils with deeper peat surfaces.

Associated soils are Partridge Beak (PCB), Wet Pine (WTP) and Sandy Bog,
shallow phase (SYBs) soils.

[PCP - PARTRIDGE CROP series]{.underline}

Partridge Crop soils have developed on gently to moderately sloping or
hummocky, coarse sandy to gravelly, glacio-fluvial deposits. These
deposits may be in part reworked by lake waters and strandlines
(beaches) may be present.

The vegetative community is dominated by jack pine, ericaceous shrubs
(especially blueberry), mosses and lichens. White birch and alder may
locally be significant. Vegetative growth varies and is probably
affected by the fire history of a particular area. Frequent, intense
burns will tend to deplete nutrient supply.

The Partridge Crop soils consist of rapidly drained Eluviated Dystric
Brunisols developed on slightly acidic to neutral, sandy and gravelly
(CS, GRCS and VGCS), glacio-fluvial deposits. The soil material is
stratified, and usually contains one or more very gravelly layers. The
composition and thickness of the duff layer (LFH) depends on fire
history of the area. The organic surface is generally very thin in the
Young Jack Pine area (often \<2 cm), and lacks a H horizon. In the Old
Jack Pine area some sections have very thin LF layers, while in some
localities they are 5 to 8 cm thick and include a thin H. The eluviated
A is strongly acidic, but thin and overlies a weak B. A transitional BC
separates the B and C horizons, which are slightly acidic to neutral.
Internal drainage is rapid as water moves freely through the soil.
Coarse fragments in the form of cobbles and stones are present in most
of the areas are locally plentiful, especially in the surface (stoniness
class 4 and 5).

Associated soils are Partridge Crop, humus variant (PCPh) soils and
Young Pine (YGP) soils.

[PCPh - PARTRIDGE CROP humus variant]{.underline}

The Partridge Crop, humus variant soils are similar to the Partridge
Crop series soils except for having a LFH over 10 cm thick. These soils
are usually associated with a vegetation community that includes besides
jack pine white birch and, especially alder. Ground cedar is also often
present. These sites may be somewhat richer in nutrients, especially N,
and accumulate therefore thicker duff layers. The H horizon may be up to
4 cm thick.

[PKW - PAKWA series]{.underline}

The Pakwa soils have developed on gently sloping to gently undulating
sandy, glacio-fluvial and glacio-lacustrine deposits. The deposits are
generally deep and stratified, and may contain gravelly to loamy layers.
The materials are usually non-calcareous.

The vegetation is dominated by jack pine, ericaceous shrubs, lichens and
mosses after fire, but black spruce and alder will become dominant at
time progresses.

The Pakwa soils consist of imperfectly drained, Gleyed Eluviated Dystric
Brunisols developed on slightly acidic to neutral sandy (S to LS
texture) deposits. Most of the Pakwa soils have developed on reworked
glacio-fluvial materials or glacio-lacustrine deposits, especially in
gently sloping areas with subdued beach ridges. The soils are mottled
and iron stained at a depth of about 50 cm from the surface. A water
table is usually present in spring and early summer, but drops well
below the control section in average years.The soils are generally
moderately acidic in the upper part of the profile and become slightly
acidic to neutral in the subsoil. Coarse fragments are minor and mostly
in the form of some cobbles and fine gravel lenses.

The duff layer is about 5 to 8 cm thick, and generally has a thin H
horizon (1 to 2 cm). The eluviated A varies in depth but is usually 5 to
8 cm thick. The upper part of the B is usually strongly developed but
thin, but grades rapidly in a developed B. The B is characterized by an
slight increase pyrophosphate-extractable Al and Fe. The B grades
gradually through a BC to the C material.

Associated soils are Clarke (CLK), Clarke, variant 1 (CLK1) soils and
Young Pine, variant 1 (YGP1) soils (soils with thin clay layers). Other
associated soils are poorly drained Baldy (BDY) soils.

[PLH - PALSA HUMMOCK complex]{.underline}

The Palsa Hummock complex soils form a complex of shallow organic soils
(40 to 100 cm), and peaty gleysolic soils (\<40 cm peat) that are frozen
in the organic layer and/or in the underlying calcareous, clayey,
glacio-lacustrine subsoil. The landform is best classified as palsa or
palsa complex, although the peat is very shallow. These palsas occur
often in border area between drainage ways and mineral upland.

The vegetation is composed of closed black, spruce, shrubs, herbs and
feather moss.

The Palsa Hummock complex soils consist of poorly drained, Terric Mesic
and Humic Organic Cryosols, Gleysolic Turbic and Static Cryosols, peaty
phase. The mineral subsoil of these soils is strongly calcareous, clayey
(HC and C), glacio-lacustrine sediments, that are usually strongly
mottled or gleyed. The peat is at least in part derived from sedges and
brown mosses, which indicates that these palsas developed out of shallow
fen peatlands. The peat is generally moderately to well decomposed, and
especially the bottom peat is very well decomposed.

Associated soils include Sipiwesk (SWK) and Roe Lake (ROK) soils, and
Thaw Fen, shallow phase (TFNs) soils.

[PLT - PLATEAU complex]{.underline}

Plateau complex soils form a complex of permanently frozen, organic
soils, between 40 and 100 cm deep, that have developed on sedge and
brown moss peat, overlain by a thin deep (\<60 cm), surface layer of
sphagnum and/or feather moss peat. The mineral subsoil is calcareous,
clayey, glacio-lacustrine sediment. These soils occur on low palsas,
palsa complexes and peat plateaus, which rise less than one meter above
the nonfrozen terrain.

The vegetation is dominated by black spruce with a ground cover of
sphagnum, feather mosses, and ericaceous shrubs. The black spruce tree
cover is usually open.

The Plateau complex soils consist of poorly drained, Terric Mesic
Organic Cryosols and Terric Fibric Organic Cryosols developed on 15 to
60 cm of very acid, fibric sphagnum and/or feather moss peat, which
overlies moderately decomposed slightly acidic to neutral sedge and
brown moss peat, which accumulated in a fen environment. The sphagnum
and feather moss peat developed after permafrost caused the surface to
be raised above the surrounding terrain. This resulted in a change in
moisture regime and lower nutrient status of soil water (ombrotrophic
conditions). As a result bog vegetation dominated by sphagnum, feather
mosses and black spruce developed. The bottom peat is usually very well
decomposed and amorphous. This peat lies over top of strongly
calcareous, clayey glacio-lacustrine sediments.

The permafrost extends through the organic materials well into the
underlying mineral sediments Ice is in the form of veins and lenses. The
active layer varies with type of vegetative cover, type of peat and
surface configuration, but is generally between 45 and 65 cm deep. In
the latter part of the growing season the surface peat may become very
dry.

The Plateau complex soils occur in close association with Thaw Fen,
shallow and very shallow phase (TFNs and TFNw) soils.

[PPU - PIPUN series]{.underline}

Pipun soils have developed on gently to moderately sloping clayey to
fine loamy, glacio-lacustrine blankets. The terrain is slightly
undulating to hummocky as a result of underlying bedrock topography,
which is modified, but not completely masked by the overlying
glacio-lacustrine deposits. Pipun soils occupy apexes and upper slopes.

The vegetative community varies with the length of time since the last
forest fire. Black spruce is the dominant tree species, but is often
replaced for some time by jack pine, trembling aspen and birch in
various mixtures after fire. When stands mature the amount of alder and
willow shrub diminishes and the ground cover becomes dominantly feather
moss. Thus mature forest generally consists of a black spruce and
feather moss dominated community.

The Pipun series consists of well to moderately well drained Orthic Gray
Luvisol soils developed on shallow 20-50 cm), moderately calcareous,
clayey (C and, most often, HC textured), glacio-lacustrine sediments
overlying fine loamy (SICL to SIL), very strongly calcareous,
glacio-lacustrine sediments. The subsoil is commonly laminated (varved)
with thick layers of silt and much thinner clay layers. The silty
subsoil may rest on clayey materials. Although the parent material is
calcareous the upper part of the solum is acidic. The pH becomes neutral
to slightly alkaline in the subsoil. Internal drainage of Pipun soils is
generally good in the upper part of the solum due to good aggregation.
Surface runoff is slight on gentle to moderate slopes due to good
internal drainage and the common presence of a moderately deep duff
layer (LFH). The H layer is usually well decomposed and finely
aggregated. The eluviated A horizon is often platy and/or fine
subangular blocky and overlies a strong, fine to medium, subangular
blocky, illuvial B. A fine to medium subangular blocky B. A transitional
BC horizon is usually present as an intergrade to the C horizon. The
solum thickness ranges from 20 to about 50 cm.

Soils most often associated with the Pipun soils are Imperfectly drained
Roe Lake, variant 1 (ROK1) soils, Sipiwesk (SWK) and Wabowden (WBW)
soils.

[ROK - ROE LAKE series]{.underline}

Roe Lake soils have developed on gently to moderately sloping clayey,
glacio-lacustrine blankets. The terrain is slightly undulating to
hummocky as a result of underlying bedrock topography, which is
modified, but not completely masked by the overlying glacio-lacustrine
deposits. The Roe Lake soils occur on flat apexes and upper slopes of
subdued, very gently sloping terrain and on the mid to lower slopes of
moderately sloping areas.

The vegetative community varies with the length of time since the last
forest fire. Black spruce is the dominant tree species, but is often
replaced by jack pine, trembling aspen and birch in various mixtures
following fire. Ground cover is dominated by feather mosses, and alder
and willow are usually present.

The Roe Lake series consists of Gleyed Gray Luvisol soils developed on
deep (\>100 cm), moderately to strongly calcareous, textured non-stony,
clayey (C and, most often, HC texture) glacio-lacustrine sediments.
Surface textures are clay and the clayey textured subsoil which is
varved with very thin silt lenses. The Roe Lake soils are imperfectly
drained, surface runoff in summer is slow to moderate and the
groundwater level is within one metre of the surface during spring and
early summer.

The Roe Lake soils are moderately well developed, the depth of leaching
ranging from 30 to 60 cm. A moderate thick (8 to 12 cm) LFH horizon,
comprised mainly of feather moss and forest litter is underlain by a
light coloured, clayey textured A horizon with weak, platy structure. A
greyish brown, clayey AB transitional horizon separates the Ae from a
brownish gray, fine clayey Bt horizon characterized by weak to moderate,
fine to medium subangular blocky structure. The clay enriched B horizon
grades through a transitional BC horizon into a moderately calcareous,
brown and yellowish brown, massive clay C horizon. The C horizon is
gleyed and mottled, which features increase in intensity at lower depths
in the profile.

Associated soils are moderately well drained Sipiwesk (SWK) and Wabowden
(WBW) soils and poorly drained Medard (MDR) and La Perouse (LPR) soils.

[ROK1 - ROE LAKE variant 1]{.underline}

The Roe Lake, variant 1 soils are much like the Roe Lake series, but
differ in number of aspects. They have shallower profiles due to a
strongly calcareous, silty clay loam textured subsoil within 30 to 50 cm
from the surface. The upper part of the solum is clay and is similar to
the upper part of the Roe Lake series profile.

[SWK - SIPIWESK series]{.underline}

Sipiwesk soils have developed on gently to moderately sloping clayey,
glacio-lacustrine blankets. The terrain is slightly undulating to
hummocky as a result of the underlying bedrock topography, which is
modified, but not completely masked by the overlying glacio-lacustrine
deposits. The Sipiwesk soils occupy apexes and upper slopes.

The vegetative community varies with the amount of time expired since
the last forest fire. Black spruce is the dominant tree species, but is
often replaced for some time by jack pine, trembling aspen and birch in
various mixtures after fire. When stands mature the amount of alder and
willow shrub diminishes and the ground cover becomes dominantly feather
moss. Thus mature forest generally consists of a black spruce and
feather moss dominated community.

The Sipiwesk series consists of well to moderately drained Orthic Gray
Luvisol soils developed on moderately to very strongly calcareous,
clayey (C and, most often, HC texture), glacio-lacustrine sediments. The
subsoil is usually laminated (varved), having alternating thin layers of
clay and silt. The subsoil usually contains more silt than the upper
part of the solum (SIC and, less often, SICL texture). Although the
parent material is calcareous the upper part of the solum is acidic. The
pH becomes neutral to slightly alkaline in the subsoil. Internal
drainage is generally good in the upper portion of the soil due to
strong aggregation of A and B horizons, but drainage is slow in the
subsoil. Surface runoff of summer precipitation is slight on gentle to
moderate slopes due to a favourable soil structure and the water
absorbing qualities of the forest floor.

Under natural, undisturbed conditions a Sipiwesk soil in the study area
is characterized by a 5 to 15 cm thick LFH (duff) layer consisting of
feather mosses, needles, leaves and other tree and shrub debris, and
remnants of vascular plants in varying stages of decomposition. The H
horizon consisting of well decomposed, often granulated, amorphous
material is generally thin (1 to 4 cm). The A horizon is moderately
leached, and is either platy or granular or both. A transitional horizon
to the subangular blocky B is often lacking. The illuvial B horizon has
a moderate to strong coarse granular to fine or medium subangular blocky
primary structure, which breaks readily to finer aggregates when
handled. A thin transitional horizon to the calcareous C is most times
present. Depth of the solum ranges from 30 to well over 50 cm.

Soils most often associated with the Sipiwesk soils are Wabowden (WBW)
soils (strong, coarse structure), Pipun (PPU) soils (SICL subsoil within
50 cm from the surface), and imperfectly drained Roe Lake (ROK) soils.

[SWK - SIPIWESK cryic phase]{.underline}

The Sipiwesk, cryic phase (SWKz) differs from the Sipiwesk series in
having a permanently frozen layer in the subsoil. This layer starts
usually at a depth of between 90 and 110 cm, and has only low to medium
ice content.

[SYBd - SANDY BOG deep phase]{.underline}

Sandy Bog, deep phase soils have developed on moderately deep (100 to
160 cm) peat deposits overlying gently sloping, coarse sandy to
gravelly, glacio-fluvial deposits. The mineral deposits may be in part
reworked by lake waters and strandlines (beaches) may be present. The
peat is largely derived from sphagnum mosses, which are little
decomposed in the surface peat, but are well decomposed close to the
contact with the mineral soil.

The vegetative community is dominated by black spruce, swamp birch,
ericaceous shrubs and mosses.

The Sandy Bog, deep phase soils consist of poorly drained, very strongly
acidic Terric Fibrisols and Terric Fibric Mesisol soils developed on
slightly decomposed sphagnum and/or feather moss peat, overlying
amorphous, strongly decomposed peat. The underlying mineral material
consists of slightly acidic to neutral, sandy and gravelly (CS, GRCS and
VGCS), glacio-fluvial deposits. The mineral material is stratified, and
usually contains one or more very gravelly layers. The mineral soil
profile is similar to the Partridge Head profile. The subsoil is
strongly gleyed. The water table is high in spring and early summer, and
remains in the control section in most years. Coarse fragments like
cobbles and stones are present in the mineral material and especially at
the contact with the overlying peat.

Associated soils are Partridge Head (PCH), and Sandy Bog, shallow phase
(SBYs) soils.

[SYBs - SANDY BOG shallow phase]{.underline}

Sandy Bog, shallow phase soils have developed on thin (40 to 100 cm)
peat deposits overlying gently sloping, coarse sandy to gravelly,
glacio-fluvial deposits. The mineral deposits may be in part reworked by
lake waters and strandlines (beaches) may be present. The peat is
largely derived from feather and sphagnum mosses, which are little
decomposed in the surface peat, but are well decomposed close to the
contact with the mineral soil.

The vegetative community is dominated by black spruce, swamp birch,
willow and mosses. Jack pine is present after forest fire.

The Sandy Bog, shallow phase soils consist of poorly drained, very
strongly acidic Terric Fibrisols developed on slightly decomposed
sphagnum and/or feather moss peat, overlying amorphous, strongly
decomposed peat. The underlying mineral material consists of slightly
acidic to neutral, sandy and gravelly (CS, GRCS and VGCS),
glacio-fluvial deposits. The mineral material is stratified, and usually
contains one or more very gravelly layers. The mineral soil profile is
similar to the Partridge Head profile. The subsoil is strongly gleyed.
The water table is high in spring and early summer, and remains in the
control section in most years. Coarse fragments like cobbles and stones
are present in the mineral material and especially at the contact with
the overlying peat.

Associated soils are Partridge Head (PCH), and Sandy Bog, deep phase
(SBYd) soils.

[TBL - TURNBULL series]{.underline}

Turnbull soils have developed on moderately sloping clayey,
glacio-lacustrine veneer. The terrain is moderately undulating to
hummocky due to the underlying bedrock topography, which is only
partially masked by the overlying glacio-lacustrine deposits. The
Turnbull soils occur on flat apexes and mid slopes of gently sloping
terrain.

The vegetative community varies with the length of time since the last
forest fire. Black spruce is the dominant tree species, but is often
replaced by jack pine, trembling aspen and birch in various mixtures
following fire. Groundcover is dominated by feather mosses, and alder
and willow are usually present.

The Turnbull series consists of Gleyed Gray Luvisol soils developed on
shallow (\>100 cm), moderately to strongly calcareous, textured
non-stony, clayey (C and, most often, HC texture) glacio-lacustrine
sediments. Surface textures are clay and the clayey textured subsoil
which is varved with very thin silt lenses. The Turnbull soils are
imperfectly drained, surface runoff in summer is slow to moderate and a
water table is present during spring and early summer.

The Turnbull soils are moderately well developed, the depth of leaching
ranging from 30 to 60 cm. A moderate thick (8 to 12 cm) LFH horizon,
comprised mainly of feather moss and forest litter is underlain by a
light coloured, clayey textured A horizon with weak, platy structure. A
greyish brown, clayey AB transitional horizon separates the Ae from a
brownish gray, fine clayey Bt horizon characterized by weak to moderate,
fine to medium subangular blocky structure. The clay enriched B horizon
grades through a transitional BC horizon into a moderately calcareous,
brown and yellowish brown, massive clay C horizon. The C horizon is
gleyed and mottled, which features increase in intensity at lower depths
in the profile.

Associated soils are moderately well drained Warren Landing (WRL),
Sipiwesk (SWK) and Wabowden (WBW) soils. and imperfectly drained Roe
Lake (ROK) soils.

[TFNs - THAW FEN shallow phase]{.underline}

Thaw Fen, shallow phase soils form a complex of organic soils, between
100 and 160 cm deep, that have developed on sedge and brown moss peat
and overlie clayey, calcareous glacio-lacustrine sediments. They occur
in drainage ways formerly occupied palsas and peat plateaus.

Vegetation is dominated by sedges, and brown mosses, and some sphagnum
mosses. Swamp birch is usually present.

The Thaw Fen, shallow phase soils consist dominantly of very poorly
drained Terric Mesic Fibrisols developed on fibric and mesic, stratified
sedge and brown moss peat. Terric Fibric Mesisols and Terric Fibrisols
also form part of the complex.A thin layer of well decomposed, amorphous
bottom peat usually occurs at the contact with the mineral subsoil. The
peat is largely derived from peat developed in a fen environment.
Although peat accumulated when the frozen organic landforms were
prevalent forms part of the mixture. As most of the palsas or peat
plateaus have collapsed in their entirety or remain in small parts the
runoff from bordering mineral uplands results in nutrient-rich
groundwater. The peat accumulated since the collapse formed is usually
very fibric and has a low bulk density. The peat is generally slightly
acidic in the surface, but is neutral to slightly alkaline at the
mineral contact. The underlying glacio-lacustrine sediments are
generally HC to C textured and are moderately to very strongly
calcareous. The water table is at or close to the surface for most of
the growing season.

Associated soils are Thaw Fen, very shallow phase TFNw), Palsa (PAA) and
Plateau (PLT) soils.

[TFNw - THAW FEN very shallow phase]{.underline}

Thaw Fen, very shallow phase soils form a complex of organic soils,
between 40 and 100 cm deep, that have developed on sedge and brown moss
peat and overlie clayey, calcareous glacio-lacustrine sediments. They
occur in drainage ways formerly occupied by palsas and peat plateaus and
in low lying areas.

Vegetation is dominated by sedges, and brown mosses, and some sphagnum
mosses. Swamp birch is sometimes present an large amounts.

The Thaw Fen, very shallow phase soils consist dominantly of very poorly
drained Terric Mesic Fibrisols and Terric Fibric Mesisols developed on
fibric and mesic, stratified sedge and brown moss peat. A thin layer of
well decomposed, amorphous bottom peat usually occurs at the contact
with the mineral subsoil. The peat is largely derived from peat
developed in a fen environment. Although peat accumulated under
permafrost conditions (bog environment) is sometimes part of the
mixture. These soils are usually associated with remnants of small
palsas or veneer bog areas. Due to runoff from bordering mineral uplands
the ground water is nutrient-rich. The peat accumulated since the
collapses were formed is usually very fibric and has a low bulk density.
The peat is generally slightly acidic in the surface, but is neutral to
slightly alkaline at the mineral contact. The underlying
glacio-lacustrine sediments are generally HC to C textured and are
moderately to very strongly calcareous. The water table is at or close
to the surface for most of the growing season.

Associated soils are Thaw Fen, shallow phase (TFNs), Plateau (PLT), and
Palsa Hummock (PLH) soils.

[TYL - TYRRELL series]{.underline}

Tyrrell soils have developed on moderately sloping clayey,
glacio-lacustrine veneer. The terrain is moderately undulating to
hummocky due to the underlying bedrock topography, which is only
partially masked by the overlying glacio-lacustrine deposits. Tyrrell
soils on flat apexes of hummocky terrain, where deposits are shallow
over bedrock.

Native vegetation is mainly black spruce with an understorey of willow
and a ground cover of mixed mosses and low ericaceous shrubs. This type
of vegetation is sometimes, at least in part, replaced by jack pine,
trembling aspen and birch after fire. Alder and willow shrubs are an
important component of the vegetative community. The ground cover is
dominantly feather mosses and some sphagnum mosses, with willow and
herbs.

Tyrrell series soils consist of Orthic Gleysol soils developed on
shallow (\<100 cm), moderately to strongly calcareous, fine textured,
glacio-lacustrine sediments overlying bedrock. The surface textures of
the Tyrrell soils is clay to heavy clay. The soils are clay and heavy
clay throughout, but sediments grade to materials containing thin, silty
textured varves in the C horizon. The thin surface organic layer is
generally peaty and consists of slightly decomposed mosses (Of horizon)
overlying an amorphous Oh. A thin organic enriched A overlies a poorly
developed, gleyed B. These soils have a high water table during spring
and early summer.

Associated soils are imperfectly drained Roe Lake (ROK) and Turnbull
(TBL) soils. Nichols Lake (NIC) complex soils and La Perouse, peaty
phase (LPRp) soils are found as well.

[WBW - WABOWDEN series]{.underline}

Wabowden soils have developed on gently to moderately sloping clayey,
glacio-lacustrine blankets. The terrain is slightly undulating to
hummocky as a result of underlying bedrock topography, which is
modified, but not completely masked by the overlying glacio-lacustrine
deposits. Wabowden soils occupy apexes and upper slopes.

The vegetative community varies with the length of time since the last
forest fire. Black spruce is the dominant tree species, but is often
replaced for some time by jack pine, trembling aspen and birch in
various mixtures after fire. When stands mature the amount of alder and
willow shrub diminishes and the ground cover becomes dominantly feather
moss. Thus mature forest generally consists of a black spruce and
feather moss dominated community.

The Wabowden series consists of well to moderately well drained Orthic
Gray Luvisol soils developed on deep, moderately to very strongly
calcareous, clayey (C and, most often, HC textured), glacio-lacustrine
sediments. The subsoil is commonly laminated (varved) with alternating
layers of clay and silt. An increase in silt content with depth is
common in the subsoil, which is often silty clay in texture, and
occasionally grades to silty clay loam at 100 cm depth or deeper.
Although the parent material is calcareous the upper part of the solum
is acidic. The pH becomes neutral to slightly alkaline in the subsoil.
Internal drainage of Wabowden soils is generally good in the upper part
of the solum due to strong aggregation in creating cracks and fissures.
Surface runoff is slight on gentle to moderate slopes due to good
internal drainage and the common presence of a moderately deep duff
layer (LFH). The H layer is usually well decomposed and finely
aggregated. The eluviated A horizon is often platy and/or fine
subangular blocky and overlies a strong, coarse, subangular blocky AB,
which grades into a strong, coarse blocky or medium to coarse columnar,
illuvial B. A fine to medium subangular blocky B usually underlies the
upper B horizon. A transitional BC horizon is usually present as an
intergrade to the C horizon. The solum thickness ranges from 30 to over
50 cm.

Soils most often associated with the Wabowden soils are Sipiwesk (SWK)
soils (strong, fine structure), Pipun (PPU) soils (SICL subsoil within
50 cm from the surface), and imperfectly drained Roe Lake (ROK) soils.

[WBWz - WABOWDEN cryic phase]{.underline}

The Wabowden, cryic phase soils are similar to the series except for the
presence of a permanently frozen layer in the subsoil. This layer is
encountered at a depth of 90 to 110 cm below the surface. Ice content is
low, with little ice visible.

[WRL - WARREN LANDING series]{.underline}

Warren Landing soils have developed on gently to moderately sloping
clayey, glacio-lacustrine veneer. The terrain is moderately undulating
to hummocky due to the underlying bedrock topography, which is modified,
but not completely masked by the overlying glacio-lacustrine deposits.
Warren Landing soil occupy apexes and upper slopes.

The vegetative community varies with the length of time since the last
forest fire. Black spruce is the dominant tree species, but is often
replaced for some time by jack pine, trembling aspen and birch in
various mixtures after fire. When stands mature the amount of alder and
willow shrub diminishes and the ground cover becomes dominantly feather
moss. Thus mature forest generally consists of a black spruce and
feather moss dominated community.

The Warren Landing series consists of well to moderately well drained
Orthic Gray Luvisol soils developed on shallow (50-100 cm), moderately
to strongly calcareous, clayey (C and, most often, HC textured),
glacio-lacustrine sediments. The subsoil is commonly laminated (varved)
with alternating layers of clay and silt. An increase in silt content
with depth is common in the subsoil, which is often silty clay in
texture, and occasionally grades to silty clay loam. Although the parent
material is calcareous the upper part of the solum is acidic. The pH
becomes neutral to slightly alkaline in the subsoil. Internal drainage
of Warren Landing soils, although generally good in the upper part of
the solum due to strong aggregation with cracks and fissures, is impeded
by the presence of bedrock within 100 cm of the surface. Surface runoff
is moderate due to moderate slopes.

The duff layer is about 4 to 10 cm thick, with a thin H horizon. The
eluviated A horizon is often platy and/or fine subangular blocky and
overlies a strong, medium to coarse, subangular blocky AB, which grades
into a strong, coarse blocky, illuvial B. A fine to medium subangular
blocky B usually underlies the upper B horizon. A transitional BC
horizon is usually present as an intergrade to the C horizon. The solum
thickness ranges from 30 to over 50 cm.

Soils most often associated with the Warren Landing soils are deeper
Sipiwesk (SWK) and Wabowden (WBW) soils, Pipun (PPU) type soils and
imperfectly drained soils like Turnbull (TBL) and Roe Lake (ROK) soils.

[WTP - WET PINE series]{.underline}

Wet Pine soils have developed on level sections of gently to moderately
sloping or hummocky, coarse sandy to gravelly, glacio-fluvial deposits.
These deposits may be in part reworked by lake waters and strandlines
(beaches) may be present. The coarse sandy material overlies fine
textured sediments within 1 m from the surface.

The vegetative community is dominated by black spruce, alder, willow and
mosses. Jack pine is present after forest fire.

The Wet Pine soils consist of poorly drained Orthic Gleysols developed
on slightly acidic to neutral, sandy and gravelly (CS, GRCS and VGCS),
glacio-fluvial deposits. The soil material is stratified, and usually
contains one or more very gravelly layers. The subsoil consists of or
contains clayey (HC to CL) layers, which are likely of glacio-lacustrine
origin. These sediments are often calcareous and slightly alkaline in
reaction. The organic surface is peaty and less than 15 cm thick. The
peat material is largely derived from mosses. The thin (\< 10 cm) is
organically enriched and overlies a gleyed B. The subsoil is strongly
gleyed. The water table is high in spring and in early summer, and, in
average years, will remain within 1 m from the surface. Coarse fragments
in the form of cobbles and stones are present in most of the areas are
locally plentiful, especially in the surface (stoniness class 4 and 5).
Included in the mapping unit are soils with deeper peat surfaces.

Associated soils are Partridge Beak (PCB), Partridge Head (PCH) and
Sandy Bog, shallow phase (SYBs) soils.

[WTP1 - WET PINE variant 1]{.underline}

The Wet Pine, variant 1 soils have developed on gently sloping to gently
undulating sandy, glacio-fluvial and glacio-lacustrine deposits. The
deposits are stratified and overlie fine textured (HC to CL) layers in
the subsoil, which sediments are likely of glacio-lacustrine origin.

The vegetation is dominated by black spruce, willow and mosses. After
fire jack pine may be part of the vegetative mix.

The Wet Pine soils consist of poorly drained, Rego Gleysols developed on
slightly acidic to neutral sandy (S to LS texture) deposits. Most of the
Wet Pine soils have developed on reworked glacio-fluvial materials or
glacio-lacustrine deposits, especially in gently sloping areas with
subdued beach ridges and in level areas where shallow sandy materials
overlie clayey materials. The sandy materials are usually
non-calcareous, but the fine textured glacio-lacustrine sediments may
contain free carbonates within the control section. The soils are gleyed
and mottled and often strongly iron stained. The water table is high in
spring and early summer, and may remain throughout the growing season
within 1 m from the surface. The soils are generally slightly acidic to
neutral the upper part of the profile and are neutral to slightly
alkaline in the subsoil. Coarse fragments are minor and mostly in the
form of some cobbles and fine gravel lenses.

The Wet Pine, variant 1 soils have a peaty surface layer less than 15 cm
thick. An organic rich A less than 10 cm thick may be present. This
horizon grades into the C horizon. Soils with weak B horizons have been
included into the Wet Pine, variant 1 mapping unit.

Associated soil are Pakwa (PKW) and Baldy (BDY) soils, and peaty phases.

[YGP - YOUNG PINE series]{.underline}

Young Pine soils have developed on gently to moderately sloping or
hummocky, coarse sandy to gravelly, glacio-fluvial deposits having fine
textured (C and CL textured) subsoil within or just below 100 cm depth.
The presence of these finer textured layers suggest a complex deposition
history. The fine textured materials tend to be calcareous, suggesting
glacio-lacustrine origin. The coarse textured surface deposits may be in
part reworked by lake waters and strandlines (beaches) may be present.

The vegetative community is dominated by jack pine, ericaceous shrubs
(especially blueberry), mosses and lichens. Black spruce is usually
present. Vegetative growth varies and is probably affected by the fire
history of a particular area. Frequent, intense burns will tend to
deplete nutrient supply.

The Young Pine consist of well to moderately well drained Eluviated
Dystric Brunisols developed on slightly acidic to neutral, sandy and
gravelly (CS, GRCS and VGCS), glacio-fluvial deposits overlying clayey
(HC, C) or fine loamy (CL) sediments. The sandy and gravelly soil
material is stratified, and usually contains one or more very gravelly
layers. The composition and thickness of the duff layer (LFH) depends on
fire history of the area. The organic surface is generally in the Young
Jack Pine area (often \<4 cm), and lacks a H horizon. In the Old Jack
Pine area some sections have very thin LF layers, while in some
localities they are 5 to 8 cm thick and include a thin H. The eluviated
A is strongly acidic, but thin and overlies a weak B. A transitional BC
separates the B and C horizons, which are slightly acidic to neutral.
The C becomes mottled and iron stained some above the clayey layer. A
perched water table is present in the early part of the growing season.
Internal drainage is rapid in coarse textured section of the profile.
Coarse fragments in the form of cobbles and stones are present in the
surface of most and may be locally plentiful.

Associated soils are Partridge Crop (PCP), and Low Pine (LWP) soils.

[YGP1 - YOUNG PINE variant 1]{.underline}

The Young Pine, variant 1 soils have developed on gently sloping to
gently undulating sandy, glacio-fluvial and glacio-lacustrine deposits.
The deposits consist of sandy materials overlying subsoil materials
containing fine textured glacio-lacustrine sediments.

The vegetation is dominated by jack pine, ericaceous shrubs, lichens and
mosses, but black spruce may be a significant a component.

The Young Pine, variant 1 soils consist well to moderately well drained,
Eluviated Dystric Brunisols developed on slightly acidic to neutral
sandy (S to LS texture) overlying or containing fine textured (C and CL)
layers in the subsoils. The sandy material has been laid down as
glacio-fluvial materials, but some have been deposited in glacial lakes
or by the reworking of glacio-fluvial materials by lake waters
(glacio-lacustrine materials). The sandy deposits are generally
stratified, and may contain some fine gravelly layers. The clayey
materials are usually are generally weakly to moderately calcareous and
probably of glacio-lacustrine origin. The soils are generally moderately
acidic in the upper part of the profile and become slightly acidic to
neutral in the subsoil. Coarse fragments are minor and mostly in the
form of some cobbles and fine gravel lenses in the sandy materials.

The duff layer is thin (2-5 cm), and generally lacks a H horizon thicker
than 0.5 to 1 cm. The eluviated A is also thin (3 to 6 cm), and is often
broken due to windthrow. The B is generally weakly developed and is
characterized by an slight increase pyrophosphate-extractable Al and Fe.
The B grades gradually through a BC to the C material. The C horizon
overlying clayey subsoil is either gleyed, mottled or iron stained. A
perched water table is present during the early growing season.

Associated soils are Clarke (CLK) soils, and imperfectly drained Pakwa
(PKW) and Low Pine, variant 1 (LWP1) soils.

**BIBLIOGRAPHY**

Agriculture Canada Expert Committee on Soil Survey, 1987. The Candian
System of Soil

> Classification. 2nd ed. Agric. Can. Publ. 1646. 164 pp.

Beke, G. J., H. Veldhuis, and J. Thie, 1973. Bio-physical Land Inventory
of the Churchill-

> Nelson Rivers Study Area, North-central Manitoba. Canada-Manitoba Soil
> Surv. Winnipeg, Manitoba. Rep. and maps.

Klassen, R. W., 1983. Lake Agassiz and the Late Glacial History of
Northern Manitoba. [In]{.underline}

> Glacial Lake Agassiz, Teller and Clayton eds. Geo. Assoc. Can.,
> Special Paper 26.Univ. Toronto Press. p 97-116.

Manitoba Ecoclimatic Regions Working Group, 1985. Ecoclimatic Regions of
Manitoba. Draft. Winnipeg, Manitoba.

Mills, G. F., H. Veldhuis, and R. G. Eilers, 1987. Thermal and Moisture
Regime Characteristics of a Veneer Bog in North-central Manitoba.
[In]{.underline} Proc. Symposium \'87 Wetlands/Peatlands, Edmonton,
Alberta, Canada. Compiled by Rubec and Overend. pp 45-52.

Veldhuis, H., and G. F. Mills, 1976. Soils of Focal Study Site No.1,
INCO project, Thompson, Manitoba. Canada-Manitoba Soil Surv., Winnipeg,
Manitoba. Rep. and map.

Veldhuis, H., and K. L. Dutchak, 1978. Soils of the Background Focal
Site, Orr Lake, INCO Project, Thompson, Manitoba. Canada-Manitoba Soil
Surv., Winnipeg, Manitoba. Rep. and map.

Veldhuis, H., and V. I. Burachynsky, 1979. Soils of Monitoring Sites 28,
49, 50 and 51, INCO Project, Thompson, Manitoba. Canda-Manitoba Soil
Surv., Winnipeg, Manitoba. Rep. and map.

Veldhuis, H., G. F. Mills, D. B. Forrester, 1979. Biophysical Land
Classification Sipiwesk 63P and Split Lake 64A (se1/4), Manitoba.
Manitoba Dep. Mines, Nay.Res. and Env. Tech. Rep. No. 79-2. Guide and
map.

**APPENDIX A**

**GLOSSARY**

[AASHO classification]{.underline} (soil engineering) - The official
classification of soil materials and soil aggregate mixtures for highway
construction used by the American Association of State Highway
Officials.

[Acid soil]{.underline} - A soil having a pH less than 7. See pH and
Reaction, soil.

[Alkaline soil]{.underline} - A soil having a pH greater than 7. See
Reaction, soil.

[Alluvium]{.underline} - A general term for all deposits of rivers and
streams.

[Arable soil]{.underline} - Soil suitable for plowing and cultivation.

[Association]{.underline} - A sequence of soils of about the same age,
derived from similar parent material, and occurring under similar
climatic conditions but showing different characteristics due to
variations in relief and in drainage.

[1/3 Atmosphere Moisture]{.underline} - The moisture percentage on dry
weight basis of a soil sample that has been air dried, screened,
saturated and subjected to a soil moisture tension of 345 cm of water
through a permeable membrane for a period of 48 hours. It approximates
the soil moisture retention capacity.

[Available nutrient]{.underline} - That portion of any element or
compound in the soil that can be readily absorbed and assimilated by
growing plants.

[Available soil moisture]{.underline} - The portion of water in a soil
that can be readily absorbed by plant roots: generally considered to be
that water held in the soil up to approximately 15 atmospheres pressure.

[Bearing capacity]{.underline} - Capacity of soil (in moist to wet
conditions) to support loads such as buildings, people, vehicles, and
animals.

> [Bedrock]{.underline} - The solid rock that underlies soil and
> regolith or that is exposed at the surface.
>
> [Boulders]{.underline} - Stones which are larger than 60 cm in
> diameter.
>
> [Bulk density]{.underline} - The weight of oven dry soil (105 degrees
> C) divided by its volume at field moisture conditions, expressed in
> grams per cubic centimeter.
>
> [Buried soil]{.underline} - Soil covered by an alluvial, loessial, or
> other deposit, usually to a depth greater than the thickness of the
> solum.
>
> [Calcareous soil]{.underline} - Soil containing sufficient calcium
> carbonate (often with magnesium carbonate) to effervesce visibly when
> treated with hydrochloric acid.
>
> [Calcium Carbonate Equivalent]{.underline} - Refers to the percent of
> carbonates in the soil expressed on the basis of calcium carbonate.
> Terms used to express the carbonate contents of soils are:
>
> noncalcareous. . . . . . . . . . . .\<1%

weakly calcareous. . . . . . . . . 1-5%

moderately calcareous. . . . . . 6-15%

strongly calcareous. . . . . . . 16-25%

v\. strongly calcareous . . . . . 26-40%

extremely calcareous . . . . . . \>40%

> [Capillary fringe]{.underline} - A zone of essentially saturated soil
> just above the water table. The size distribution of the pores
> determines the extent and degree of the capillary fringe.
>
> [Carbon-nitrogen ratio (C/N ratio)]{.underline} -The ratio of the
> weight of organic carbon to the weight of total nitrogen in a soil or
> in an organic material.
>
> [Cation Exchange Capacity (CEC)]{.underline} - A measure of the total
> amount of exchangeable cations that can be held by a soil. Expressed
> in milliequivalents per 100g of soil.

[Clay]{.underline} - As a soil separate, the mineral soil particles less
than 0.002 mm in diameter: usually consisting largely of clay minerals.
As a soil textural class, soil materials that contain 40 or more percent
clay, less than 45 percent sand and less than 40 percent silt.

[Cobbles]{.underline} - Rock fragments 8 to 25 cm in diameter.

[Color]{.underline} - Soil colors are compared with a Munsell color
chart. The Munsell system specifies the relative degrees of the three
simple variables of color: hue, value and chroma. For example: 10YR 6/4
means a hue of 10YR, a value of 6, and a chroma of 4.

[Complex (soil)]{.underline} - A mapping unit used in detailed and
reconnaissance soil surveys where two or more soil series that are so
intimately intermixed in an area that it is impractical to separate them
at the scale of mapping used.

[Concretions]{.underline} - Hard grains, pellets or nodules from
concentration of compounds in the soil that cement soil grains together.

[Conductivity, electrical]{.underline} - A physical quantity that
measures the readiness with which a medium (irrigation water and soil
extracts) transmits electricity. It ex-presses the concentration of salt
in terms of the conductance (reciprocal of the electric resistance in
ohms) in milliSiemens per cm (or expressed as deciSiemens per meter -
dS/m).

[Consistence (soil)]{.underline} - The mutual attraction of the
particles in a soil mass, or their resistance to separation or
deformation. It is described in terms such as loose, soft, friable,
firm, hard, sticky, plastic or cemented.

[Consumptive use factor (CU)]{.underline} - The ratio of consumptive use
of water by a crop to potential evapotranspiration and transpiration. An
actively growing crop that completely covers the soil over a large area
and that has an ample supply of readily available soil water has a
consumptive use factor of 1.0.

[Consumptive use of water]{.underline} - The sum of the depths of water
transpired by the plants and evaporated from the soil surface and from
intercepted precipitation. It may be less or greater than potential
evapotranspiration.

> [Contour]{.underline} - An imaginary line connecting points of equal
> elevation on the surface of the soil.
>
> [Cover]{.underline} - This term generally has one of the following
> meanings:

1\. Vegetation or other material providing protection

2\. In forestry, low growing shrubs and herbaceous plants under trees
(i.e., ground cover vs. tree cover)

3\. Any vegetation producing a protective mat on or just above the soil
surface.

> [Creep (soil)]{.underline} - Slow mass movement of soil and soil
> material down rather steep slopes primarily under the influence of
> gravity, but aided by saturation with water and by alternate freezing
> and thawing.
>
> [Decile portion]{.underline} - A one-tenth portion. As used in the
> soil map symbol A7-B3 means that the A soils cover seven tenths and
> the B soils cover three tenths of the map unit.
>
> [Delta]{.underline} - A fluvial or glaciofluvial fan shaped deposit at
> the mouth of a river that empties into a lake or sea.
>
> [Deflocculate]{.underline} - To separate or to break up soil
> aggregates into individual particles by chemical or physical means or
> both.
>
> [Degradation (of soils)]{.underline} - The changing of a soil to a
> more highly leached and more highly weathered condition, usually
> accompanied by morphological changes such as the development of an
> eluviated light colored (Ae) horizon.
>
> [Dispersion]{.underline} - Is rated high, moderate or low depending on
> how readily the soil structure breaks down or slakes because of excess
> moisture. A rating of high indicates that soil aggregates slake
> readily;
>
> a rating of low indicates that aggregates are resistant to dispersion
> and remain clumped together.

[Drainage (soil)]{.underline} - (1) The rapidity and extent of the
removal of water from the soil by runoff and flow through the soil to
underground spaces. (2) As a condition of the soil, it refers to the
frequency and duration of periods when the soil is free of saturation.

> Drainage in soil reports is described on the basis of actual moisture
> content in excess of field capacity and length of the saturation
> period within the plant root zone. The terms are as follows:
>
> [Very rapidly drained]{.underline} - Water is removed from the soil
> very rapidly in relation to supply. Excess water flows downward very
> rapidly if underlying material is pervious. There may be very rapid
> subsurface flow during heavy rainfall provided there is a steep
> gradient. Soils have very low available water storage capacity
> (usually less than 2.5 cm) within the control section and are usually
> coarse in texture, or shallow, or both. Water source is precipitation.
>
> [Rapidly drained]{.underline} - Water is removed from the soil rapidly
> in relation to supply. Excess water flows downward if underlying
> material is pervious. Subsurface flow may occur on steep gradients
> during heavy rainfall. Soils have low available water storage capacity
> (2.5-4 cm) within the control section, and are usually coarse in
> texture, or shallow, or both. Water source is precipitation.
>
> [Well drained]{.underline} - Water is removed from the soil readily
> but not rapidly. Excess water flows downward readily into underlying
> pervious material or laterally as subsurface flow. Soils have
> intermediate available water storage capacity (4-5 cm) within the
> control section, and are generally intermediate in texture and depth.
> Water source is precipitation. On slopes subsurface flow may occur for
> short durations but additions are equalled by losses. These soils are
> usually free of mottles within 100 cm of the surface but may be
> mottled below this depth. Soil horizons are usually bright colored.
>
> [Moderately well drained]{.underline} - Water is removed from the soil
> somewhat slowly in relation to supply. Excess water is removed
> somewhat slowly due to low perviousness, shallow water table, lack of
> gradient, or some combination of these. Soils have intermediate to
> high water storage capacity (5-6cm) within the control section and are
> usually medium to fine in texture. Soils are commonly mottled in the
> 50 to 100 cm depth. Colors are dull brown in the subsoil with stains
> and mottles.
>
> [Imperfectly drained]{.underline} - Water is removed from the soil
> sufficiently slowly in relation to supply to keep the soil wet for a
> significant part of the growing season. Excess water moves slowly
> downward if precipitation is major supply. If subsurface water or
> groundwater, or both, is the main source, flow rate may vary but the
> soil remains wet for a significant part of the growing season.
> Precipitation is the main source if available water storage capacity
> is high; contribution by subsurface flow or groundwater flow, or both,
> increases as available water storage capacity decreases. Soils have a
> wide range in available water supply, texture, and depth, and are
> gleyed phases of well drained subgroups. These soils generally have
> mottling below the surface layers and generally have duller colors
> with depth, generally brownish gray with mottles of yellow and gray.
>
> [Poorly drained]{.underline} - Water is removed so slowly in relation
> to supply that the soil remains wet for a comparatively large part of
> the time the soil is not frozen. Excess water is evident in the soil
> for a large part of the time. Subsurface flow or groundwater flow, or
> both, in addition to precipitation are main water sources; there may
> also be a perched water table, with precipitation exceeding
> evapotranspiration. Poorly drained soils have a wide range in
> available water storage capacity, texture, and depth, and are gleyed
> subgroups, Gleysols, and Organic soils.
>
> [Very poorly drained]{.underline} - Water is removed from the soil so
> slowly that the water table remains at or on the surface for the
> greater part of the time the soil is not frozen. Excess water is
> present in the soil for the greater part of the time. Groundwater flow
> and subsurface flow are major water sources. Precipitation is less
> important except where there is a perched water table with
> precipitation exceeding evapotranspiration. These soils have a wide
> range in available water storage capacity, texture, and depth, and are
> either Gleysolic or Organic.

[Dryland farming]{.underline} - The practice of crop production in low
rainfall areas without irrigation.

[Eluvial horizon]{.underline} - A horizon from which material has been
removed in solution or in water suspension.

[Eolian]{.underline} - Soil material accumulated through wind action.

[Erosion]{.underline} - The wearing away of the land surface by
detachment and transport of soil and rock material through the action of
moving water, wind or other geological processes. The ratings of erosion
are:

Erosion 1 slightly eroded - soil with a sufficient amount of the A
horizon removed that ordinary tillage will bring up and mix the B
horizon or other lower lying horizons with surface soil in the plow
layer.

Erosion 2 moderately eroded - soil with all of the A horizon and a part
of the B or other lower lying horizons removed. The plow layer consists
mainly of the original horizons below the A or below the original plow
layer.

Erosion 3 severely eroded - soils have practically all of the original
surface soil removed. The plow layer consists mainly of C horizon
material, especially on knolls and steep upper slope positions.

[Evapotranspiration]{.underline} - The combined loss of water from a
given area, and during a specific period of time, by evaporation from
the soil surface and transpiration from plants.

> [Field Moisture Equivalent]{.underline} - The minimum moisture content
> at which a drop of water placed on a smoothed surface of the soil will
> not be absorbed immediately by the soil, but will spread out over the
> surface and give it a shiny appearance.
>
> [Flood plain]{.underline} - The land bordering a stream, built up of
> sediments from overflow of the stream and subject to inundation when
> the stream is at flood stage.
>
> [Fluvial deposits]{.underline} - All sediments past and present,
> deposited by flowing water, including glaciofluvial deposits.
>
> [Frost heave]{.underline} - The raising of the surface caused by ice
> in the subsoil.
>
> [Friable]{.underline} - Soil aggregates that are soft and easily
> crushed between thumb and forefinger.
>
> [Glaciofluvial deposits]{.underline} - Material moved by glaciers and
> subsequently sorted and deposited by streams flowing from the melting
> ice. These deposits are stratified and may occur in the form of
> outwash plains, deltas, kames, eskers and kame terraces.
>
> [Gleyed soil]{.underline} - An imperfectly or poorly drained soil in
> which the material has been modified by reduction or alternating
> reduction and oxidation. These soils have lower chromas or more
> prominent mottling or both in some horizons than the associated
> well-drained soil.
>
> [Gleysolic]{.underline} - An order of soils developed under wet
> conditions and permanent or periodic reduction. These soils have low
> chromas or prominent mottling or both, in some horizons.
>
> [Gravel]{.underline} - Rock fragments 2 mm to 7.5 cm in diameter.
>
> [Ground Moraine]{.underline} - An unsorted mixture of rocks, boulders,
> sand, silt and clay deposited by glacial ice. The predominant material
> is till; most till is thought to have accumulated under the ice by
> lodgment, but some till has been let down from the upper surface of
> the ice by ablation. Resorting and modification may have taken place
> to some extent by wave-action of glacial melt waters. The topography
> is most commonly in the form of undulating plains with gently sloping
> hills and enclosed depressions.

[Groundwater]{.underline} - Water beneath the soil surface, usually
under conditions where the voids are completely filled with water
(saturation).

[Halophytic vegetation]{.underline} - Vegetation that grows naturally in
soils having a high content of various salts. It usually has fleshy
leaves or thorns and resembles desert vegetation.

[Horizon (soil)]{.underline} - A layer in the soil profile approximately
parallel to the land surface with more or less well-defined
characteristics that have been produced through the operation of soil
forming processes.

[Horizon boundary]{.underline} - The lower boundary of each horizon is
described by indicating its distinctness and form. The distinctness
depends on the abruptness of vertical change (thickness). The form
refers to the variation of the boundary plane.

[Distinctness]{.underline} -

> abrupt - less than 2 cm
>
> clear - 2 to 5 cm
>
> gradual - 5 to 15 cm
>
> diffuse - more than 15 cm

[Form]{.underline} -

> smooth - nearly plain
>
> wavy - pockets are wider than deep
>
> irregular - pockets are deeper than wide

broken - parts of the horizon are unconnected with other parts

[Humic layer]{.underline} - A layer of highly decomposed organic soil
material containing little fibre.

[Hydraulic Conductivity]{.underline} - Refers to the effective flow
velocity or discharge velocity in soil at unit hydraulic gradient. It is
an approximation of the permeability of the soil and is expressed in cm
per hour. The classes are described in general or specific terms as:

High \>15

Very rapid \>50

Rapid 15-50

Medium 0.5-15

Mod. rapid 5.0-15\
Moderate 1.5-5.0

Mod. slow 0.5-1.5

Low \<0.5

Slow 0.15-0.5

Very slow 0.015-0.15

Extremely slow \<.015

> [Hydrologic cycle]{.underline} - The conditions through which water
> naturally passes from the time of precipitation until it is returned
> to the atmosphere by evaporation and is again ready to be
> precipitated.
>
> [Hydrophyte]{.underline} - Plants growing in water or dependent upon
> wet or saturated soil conditions for growth.
>
> [Illuvial horizon]{.underline} - A soil horizon in which material
> carried from an overlying layer has been precipitated from solution or
> deposited from suspension. The layer of accumulation.
>
> [Impeded drainage]{.underline} - A condition that hinders the movement
> of water by gravity through the soils.
>
> [Inclusion]{.underline} - Soil type found within a mapping unit that
> is not extensive
>
> enough to be mapped separately or as part of a complex.
>
> [Infiltration]{.underline} - The downward entry of water into the soil
>
> [Irrigation]{.underline} - The artificial application of water to the
> soil for the benefit of growing crops.
>
> [Irrigation requirement (IR)]{.underline} - Refers to the amount of
> water exclusive of effective precipitation that is required for crop
> production.
>
> [Lacustrine deposits]{.underline} - Material deposited by or settled
> out of lake waters and exposed by lowering of the water levels or
> elevation of the land. These sediments range in texture from sand to
> clay and are usually varved (layered annual deposits).
>
> [Landforms]{.underline} - See Description of Landforms
>
> [Landscape]{.underline} - All the natural features such as fields,
> hills, forest, water, etc., which distinguish one part of the earth\'s
> surface from another part.

[Leaching]{.underline} - The removal from the soil of materials in
solution.

[Liquid limit (upper plastic limit)]{.underline} -The water content
corresponding to an arbitrary limit between the liquid and plastic
states of consistency of a soil. The water content at this boundary is
defined as that at which a pat of soil cut by a groove of standard
dimensions will flow together for a distance of l.25 cm under the impact
of 25 blows in a standard liquid limit apparatus.

[Lineal shrinkage]{.underline} - This is the decrease in one dimension
expressed as a percentage of the original dimension of the soil mass
when the moisture content is reduced from a stipulated percentage
(usually field moisture equivalent) to the shrinkage limit.

[Mapping Unit]{.underline} - Any delineated area shown on a soil map
that is identified by a symbol. A mapping unit may be a soil unit, a
miscellaneous land type, or a soil complex.

[Marsh]{.underline} - Periodically flooded or continually wet areas
having the surface not deeply submerged. It is covered dominantly with
sedges, cattails, rushes or other hydrophytic plants.

[Mature soil]{.underline} - A soil having well-developed soil horizons
produced by the natural processes of soil formation.

[Mesophyte]{.underline} - Plants requiring intermediate moisture
conditions and are not very resistant to drought.

[Microrelief]{.underline} - Small-scale, local differences in relief
including mounds, swales or hollows.

[Milliequivalent (me)]{.underline} - One-thousandth of an equivalent. An
equivalent is the weight in grams of an ion or compound that combines
with or replaces one gram of hydrogen. The atomic or formula weight
divided by valence.

[Mottles]{.underline} - Irregularly marked spots or streaks, usually
yellow or orange but sometimes blue. They are described in order of
abundance (few, common, many), size (fine, medium, coarse) and contrast
(faint, distinct, prominent). Mottles in soils indicate poor aeration
and lack of good drainage.

> [Organic carbon]{.underline} - Carbon derived from plant and animal
> residues.
>
> [Organic matter]{.underline} - The fraction of the soil which consists
> of plant and animal residues at various stages of decomposition, cells
> and tissues of soil organisms and substances synthesized by the soil
> population. It is determined on soils that have been sieved through a
> 2.0 mm sieve. It is estimated by multiplying the organic carbon by a
> factor of 1.72.
>
> [Outwash]{.underline} - Sediments \"washed out\" beyond the glacier by
> flowing water and laid down in thin beds or strata. Particle size may
> range from boulders to silt.
>
> [Ovendry soil]{.underline} - Soil that has been dried at 105 degrees C
> until it has reached constant weight.
>
> [Parent material]{.underline} - The unaltered or essentially unaltered
> mineral or organic material from which the soil profile develops by
> pedogenic processes.
>
> [Particle size, soil]{.underline} - The grain size distribution of the
> whole soil including the coarse fraction. It differs from texture,
> which refers to the fine earth (less than 2mm) fraction only. In
> addition, textural classes are usually assigned to specific horizons
> whereas soil family particle-size classes indicate a composite
> particle size of a part of the control section that may include
> several horizons. See Textural Triangle at end of Glossary.
>
> The particle-size classes for family groupings are as follows:
>
> [Fragmental]{.underline} - Stones, cobbles and gravel, with too little
> fine earth to fill interstices larger than 1 mm.
>
> [Sandy-skeletal]{.underline} - Particles coarser than 2 mm occupy 35%
> or more by volume with enough fine earth to fill interstices larger
> than 1 mm; the fraction finer than 2 mm is that defined for the sandy
> particle size class.
>
> [Loamy-skeletal]{.underline} - Particles 2 mm-25 cm occupy 35% or more
> by volume with enough fine earth to fill interstices larger than 1 mm;
> the fraction finer than 2 mm is that defined for the loamy
> particle-size class.
>
> [Clayey-skeletal]{.underline} - Particles 2 mm-25 cm occupy 35% or
> more by volume with enough fine earth to fill interstices larger than
> 1 mm; the fraction finer than 2 mm is that defined for the clayey
> particle size class.
>
> [Sandy]{.underline} - The texture of the fine earth includes sands and
> loamy sands, exclusive of loamy very fine sand and very fine sand
> textures; particles 2 mm- 25 cm occupy less than 35% by volume.
>
> [Loamy]{.underline} - The texture of the fine earth includes loamy
> very fine sand, very fine sand, and finer textures with less than 35%
> clay; particles 2 mm-25 cm occupy less than 35% by volume.
>
> [Coarse-loamy]{.underline} A loamy particle size that has 15% or more
> by weight of fine sand (0.25-0.1 mm) or coarser particles, including
> fragments up to 7.5 cm, and has less than 18% clay in the fine earth
> fraction.
>
> [Fine-loamy]{.underline} - A loamy particle size that has 15% or more
> by weight of fine sand (0.25-0.1 mm) or coarser particles, including
> fragments up to 7.5 cm, and has 18-35% clay in the fine earth
> fraction.
>
> [Coarse-silty]{.underline} - A loamy particle size that has less than
> 15% of fine sand (0.25-0.1 mm) or coarser particles, including
> fragments up to 7.5 cm, and has less than 18% clay in the fine earth
> fraction.
>
> [Fine-silty]{.underline} - A loamy particle size that has less than
> 15% of fine sand (0.25-0.1 mm) or coarser particles, including
> fragments up to 7.5 cm, and has 18-35% clay in the fine earth
> fraction.
>
> [Clayey]{.underline} - The fine earth contains 35% or more clay by
> weight and particles 2mm-25 cm occupy less than 35% by volume.
>
> [Fine-clayey]{.underline} - A clayey particle size that has 35-60%
> clay in the fine earth fraction.
>
> [Very-fine-clayey]{.underline} - A clayey particle size that has 60%
> or more clay in the fine earth fraction.
>
> [Ped]{.underline} - An individual soil aggregate such as granule,
> prism or block formed by natural processes (in contrast with a clod
> which is formed artificially).
>
> [Pedology]{.underline} - Those aspects of soil science involving
> constitution, distribution, genesis and classification of soils.
>
> [Percolation]{.underline} - The downward movement of water through
> soil; specifically, the downward flow of water in saturated or nearly
> saturated soil at hydraulic gradients of 1.0 or less.
>
> [Permafrost]{.underline} -

1\. Perennially frozen material underlying the solum.

2\. A perennially frozen soil horizon.

> [Permafrost table]{.underline} - The upper boundary of permafrost,
> usually coincident with the lower limit of seasonal thaw (active
> layer).
>
> [Permeability]{.underline} - The ease with which water and air pass
> through the soil to all parts of the profile. See hydraulic
> conductivity.
>
> [pH]{.underline} - The intensity of acidity and alkalinity, expressed
> as the negative logarithm of the hydrogen ion concentration. A pH of 7
> is neutral, lower values indicate acidity and higher values alkalinity
> (see Reaction, soil).
>
> [Phase, soil]{.underline} - A soil phase is used to characterize soil
> and landscape properties that are not used as criteria in soil
> taxonomy. The major phase differentiae are: slope, erosion,
> deposition, stoniness, texture, salinity, and calcareousness.
>
> [Plastic Limit]{.underline} - The water content corresponding to an
> arbitrary limit between the plastic and the semisolid states of
> consistency of a soil.
>
> [Plasticity Index]{.underline} - The numerical difference between the
> liquid and the plastic limit. The plasticity index gives the range of
> moisture contents within which a soil exhibits plastic properties.
>
> [Potential evapotranspiration (PE)]{.underline} - The maximum quantity
> of water capable of being lost as water vapor, in a given climate, by
> a continuous stretch of vegetation covering the whole ground and well
> supplied with water.

[Profile, soil]{.underline} - A vertical section of the soil through all
its horizons and extending into the parent material.

[Reaction, soil]{.underline} - The acidity or alkalinity of a soil.

Soil reaction classes are characterized as follows:

extremely acid pH\<4.5

very strongly acid 4.5 to 5.0

strongly acid 5.1 to 5.5

medium acid 5.6 to 6.0

slightly acid 6.1 to 6.5

neutral 6.6 to 7.3

mildly alkaline 7.4 to 7.8

mod. alkaline 7.9 to 8.4

strongly alkaline 8.5 to 9.0

very strongly alkaline \>9.0

[Regolith]{.underline} - The unconsolidated mantle of weathered rock and
soil material on the earth\'s surface.

[Relief]{.underline} - The elevation of inequalities of the land surface
when considered collectively.

[Runoff]{.underline} - The portion of the total precipitation on an area
that flows away through stream channels. Surface runoff does not enter
the soil. Groundwater runoff or seepage flow from groundwater enters the
soil before reaching the stream.

[Saline Soil]{.underline} - A nonalkali soil containing soluble salts in
such quantities that they interfere with the growth of most crop plants.
The conductivity of the saturation extract is greater than 4
millisiemens/cm (ms/cm), the exchangeable-sodium percentage is less than
15, and the pH is usually less than 8.5. Approximate limits of salinity
classes are:

non-saline 0 to 4 mS/cm

weakly saline 4 to 8 mS/cm

mod. saline 8 to 15 mS/cm

strongly saline \>15 mS/cm

[Salinization]{.underline} - The process of accumulation of salts in the
soil.

> [Salt-Affected Soil]{.underline} - Soil that has been adversely
> modified for the growth of most crop plants by the presence of certain
> types of exchangeable ions or of soluble salts. It includes soils
> having an excess of salts, or an excess of exchangeable sodium or
> both.
>
> [Sand]{.underline} - A soil particle between 0.05 and 2.0 mm in
> diameter. The textural class name for any soil containing 85 percent
> or more of sand and not more than 10 percent of clay.
>
> [Saturation Percentage]{.underline} - The moisture percentage of a
> saturated soil paste, expressed on an oven dry weight basis.
>
> [Seepage]{.underline} -

1\. The escape of water downward through the soil.

2\. The emergence of water from the soil along an extensive line of
surface in contrast to a spring where water emerges from a local spot.

> [Series, soil]{.underline} - A category in the Canadian System of Soil
> Classification. It consists of soils that have soil horizons similar
> in their differentiating characteristics and arrangement in the
> profile, except for surface texture and are formed from a particular
> type of parent material.
>
> [Shrinkage limit]{.underline} - This is the moisture content at which
> an equilibrium condition of volume change is reached and further
> reduction in moisture content will not cause a decrease in the volume
> of the soil mass.
>
> [Shrinkage ratio]{.underline} - This is the ratio between the volume
> change and a corresponding change in moisture content. It equals the
> apparent specific gravity of the dried soil.
>
> [Silt]{.underline} - (a) Individual mineral particles of soil that
> range in diameter between 0.05 to .002 mm. (b) Soil of the textural
> class silt contains greater than 80 percent silt and less than 12
> percent clay.
>
> [Slickenside]{.underline} - Smoothed surfaces along planes of weakness
> resulting from the movement of one mass of soil against another in
> soils dominated by swelling clays.

[Sodium-Adsorption Ratio (S.A.R.)]{.underline} - A ratio for soil
extracts and irrigation waters used to express the relative activity of
sodium ions in exchange reactions with other cations in the soil SAR =
Na/((Ca+Mg)/2)1/2 where the cation concentrations are expressed as
milliequivalents per litre.

[Soil]{.underline} - The unconsolidated mineral material on the
immediate surface of the earth that serves as a natural medium for the
growth of land plants. Soil has been subjected to and influenced by
genetic and environmental factors of: parent material, climate
(including moisture and temperature effects), macro- and microorganisms,
and topography, all acting over a period of time.

[Solum]{.underline} - The upper horizons of a soil above the parent
material and in which the processes of soil formation are active. It
usually comprises the A and B horizons.

[Stones]{.underline} - Rock fragments greater than 25 cm in diameter.

[Stoniness]{.underline} - The percentage of land surface occupied by
stones. The classes of stoniness are defined as follows:

> [Stones O. Nonstony]{.underline} \-- Land having less than 0.01% of
> surface occupied by stones.
>
> [Stones 1. Slightly stony]{.underline} \-- Land having 0.01-0.1% of
> surface occupied by stones. Stones 15-30 cm in diameter, 10-30 m
> apart. The stones offer only slight to no hindrance to cultivation.
>
> [Stones 2. Moderately stony]{.underline} \-- Land having 0.1-3% of
> surface occupied by stones. Stones 15-30 cm in diameter, 2-10 m apart.
> Stones cause some interference with cultivation.
>
> [Stones 3. Very stony]{.underline} \-- Land having 3-15% of surface
> occupied by stones. Stones 15-30 cm in diameter, 1-2 m apart. There
> are sufficient stones to constitute a serious handicap to cultivation.
>
> [Stones 4. Exceedingly stony]{.underline} \-- Land having 15-50% of
> surface occupied by stones. Stones 15-30 cm in diameter, 0.7-1.5 m
> apart. There are sufficient stones to prevent cultivation until
> considerable clearing has been done.
>
> [Stones 5. Excessively stony]{.underline} \-- Land having more than
> 50% of surface occupied by stones. Stones 15-30 cm in diameter, less
> than 0.7 m apart. The land is too stony to permit cultivation.
>
> [Storage Capacity]{.underline} - Refers to the maximum amount of
> readily available water that can be stored within the rooting zone of
> a crop in a given soil. For practical irrigation purposes, 50 percent
> of the total soil water between field capacity and wilting point may
> be considered as readily available.
>
> [Stratified materials]{.underline} - Unconsolidated sand, silt and
> clay arranged in strata or layers. In stratified materials, a bed is a
> unit layer distinctly separable from other layers and is one or more
> cm thick but a lamina is a similar layer less than 1 cm thick.
>
> [Structure]{.underline} - The combination or arrangement of primary
> soil particles into aggregates of secondary soil particles, units or
> peds, which are separated from each other by surfaces of weakness.
> Structure is expressed in terms of [grade]{.underline}, size
> [class]{.underline} and shape [type]{.underline}. Grade refers to the
> distinctness of aggregate development, and is described as
> structureless, weak, moderate or strong. Structureless refers to the
> absence of observable aggregation of definite orderly arrangement; the
> term amorphous is used if soil is massive or coherent, single-grained
> if noncoherent. The weak to strong aggregates vary in size and are
> described by class as fine, medium, coarse, and very coarse depending
> on the shape types. The shape types refers to the dominant
> configuration of the aggregates and the way they are accommodated. The
> general shape types are plate-like, block-like and prism-like. The
> terms are:
>
> [Platy]{.underline} - Having thin, plate-like aggregates with faces
> mostly horizontal.
>
> [Prismatic]{.underline} - Having prism-like aggregates with tops and
> edges, appear plane, level and somewhat angular.
>
> [Columnar]{.underline} - Having prism-like aggregates with vertical
> edges near the top of columns, not sharp.
>
> [Granular]{.underline} - Having block-like aggregates that appear as
> spheroids or polyhedrons having plane or curved surfaces which have
> slight or no accommodation to the faces of the surrounding peds.

[Blocky]{.underline} - Having block-like aggregates with sharp, angular
corners.

[Subangular blocky]{.underline} - Having block-like aggregates with
rounded and flattened faces and rounded corners.

By convention an aggregate is described in the order of grade, class and
type, e.g. strong, medium, blocky. In the parent material of soils the
material with structural shapes may be designated as pseudo-blocky,
pseudo-platy, etc.

[Soil Survey]{.underline} - The systematic examination, description,
classification, and mapping of soil in an area.

[Sulfate Hazard]{.underline} - Refers to the relative degree of attack
on concrete by soil and water containing various amounts of sulfate
ions. It is estimated from electrolyte measurements and salt analysis on
selected profiles and soil samples, and by visual examination of free
gypsum within the profile during the course of soil investigation.

[Swamp]{.underline} - See Description of Landforms

[Texture, soil]{.underline} - The relative proportions of the fine earth
(less than 2 mm.) fraction of a soil. Textural classes are usually
assigned to specific horizons whereas family particle size classes
indicate a composite particle size of a portion of the control section
that may include several horizons. See Texture Triangle at end of
Glossary. The size range of the constituent primary particles are as
follows:

Diameter (mm)

Very coarse sand 2.0-1.0

Coarse sand 1.0-0.5

Medium sand 0.5-0.25

Fine sand 0.25-0.10

Very fine sand 0.10-0.05

Silt 0.05-0.002

Clay \< 0.002

Fine clay \< 0.0002

> [Till, glacial]{.underline} - Unstratified glacial deposits consisting
> of clay, sand, gravel, and boulders intermingled in any proportion.
>
> [Tilth]{.underline} - The physical condition of soil as related to its
> ease of tillage, fitness as a seedbed, and its impedance to seedling
> emergency and root penetration.
>
> [Topography]{.underline} - Refers to the percent slope and the pattern
> or frequency of slopes in different directions. A set of 10 slope
> classes are used to denote the dominant but not necessarily most
> abundant slopes within a mapping unit.

Slope Slope Percent Approx.

Class Name slope degrees

1 level 0-0.5 0

2 nearly level .5-2.5 .3-1.5

3 very gentle 2-5 1-3

4 gentle 6-9 3.5-5

5 moderate 10-15 6-8.5

6 strong 16-30 9-17

7 very strong 31-45 17-24

8 extreme 46-70 25-35

9 steep 71-100 35-45

10 very steep \>100 \>45

> [Underground runoff]{.underline} - (or seepage) Water flowing towards
> stream channels after infiltration into the ground.
>
> [Unified Soil Classification System\|]{.underline} (engineering) - A
> classification system based on the identification of soils according
> to their particle size, gradation, plasticity index and liquid limit.
>
> [Urban Land]{.underline} - Areas so altered or obstructed by urban
> works or structures that identification of soils is not feasible.
>
> [Variant, soil]{.underline} - A soil whose properties are believed to
> be sufficiently different from other known soils to justify a new
> series name, but comprising such a limited geographic area that
> creation of a new series is not justified.

[Varve]{.underline} - A distinct band representing the annual deposit in
sedimentary materials regardless of origin and usually consisting of two
layers, one thick light colored layer of silt and fine sand laid down in
the spring and summer, and the other a thin, dark colored layer of clay
laid down in the fall and winter.

[Water balance, soil]{.underline} - Is the daily amount of readily
available water retained by the soil. The daily soil-water balance is
decreased by the amount that the daily consumptive use exceeds the daily
rainfall. When daily rainfall exceeds the consumptive use, the daily
balance increases by the amount of the difference unless the soil-water
balance is at storage capacity, in which case the excess is assumed to
be lost by runoff or deep percolation.

[Water table]{.underline} - (groundwater surface; free water surface;
groundwater elevation) Elevation at which the pressure in the water is
zero with respect to the atmospheric pressure.

[Water table depths]{.underline} - (cm)

Generally High \<100

Very High 0-50

Moderately High 250-100

Medium High 100-150

Generally Low \>150

Medium Low 150-200

Low \>200

Moderately Low 200-300

Very Low \>300

[Water-holding capacity]{.underline} - The ability of a soil to hold
water against the force of gravity in a freely drained soil.

[Weathering]{.underline} - The physical and chemical disintegration,
alteration and decomposition of rocks and minerals at or near the
earth\'s surface by atmospheric agents.

[Xerophyte]{.underline} - Plants capable of surviving extended periods
of soil drought.

**APPENDIX B**

**SOIL HORIZON DESIGNATIONS**

**ORGANIC HORIZONS**

Organic horizons are found in Organic soils, and commonly at the surface
of mineral soils. They may occur at any depth beneath the surface in
buried soils, or overlying geologic deposits. They contain more than 17%
organic carbon (approximately 30% organic matter) by weight. Two groups
of these horizons are recognized, O horizons and the L, F, and H
horizons.

O This is an organic horizon developed mainly from mosses, rushes, and
woody materials.

Of The fibric horizon is the least decomposed of all the organic soil
materials. It has large amounts of well- preserved fiber that are
readily identifiable as to botanical origin. A fibric horizon has 40% or
more of rubbed fiber by volume and a pyrophosphate index of 5 or more.
If the rubbed fiber volume is 75% or more, the pyrophosphate criterion
does not apply.

Om The mesic horizon is the intermediate stage of decompostion with
intermediate amounts of fiber, bulk density and water-holding capacity.
The material is partly altered both physically and biochemically. A
mesic horizon is one that fails to meet the requirements of fibric or
humic.

Oh The humic horizon is the most highly decomposed of the organic soil
mate- ials. It has the least amount of fiber, the highest bulk density,
and the lowest saturated water-holding capacity. It is very stable and
changes very little physically or chemically with time unless it is
drained. The humic horizon has less than 10% rubbed fiber by volume and
a pyrophosphate index of 3 or less.

LFH These organic horizons developed primarily from leaves, twigs, woody
materials and a minor component of mosses under imperfectly to well
drained forest conditions.

L This is an organic horizon characterized by an accumulation of organic
matter in which the original structures are easily discernible.

F This is an organic horizon characterized by an accumulation of partly
decomposed organic matter. The original structures in part are difficult
to recognize. The horizon may be partly comminuted by soil fauna as in
moder, or it may be a partly decomposed mat permeated by fungal hyphae
as in mor.

> H This is an organic horizon characterized by an accumulation of
> decomposed organic matter in which the original structures are
> indiscernible. This material differs from the F horizon by its greater
> humification chiefly through the action of organisms. It is frequently
> intermixed with mineral grains, especially near the junction with the
> mineral horizon.

**MASTER MINERAL HORIZONS**

Mineral horizons are those that contain less than 30% organic matter by
weight as specified for organic horizon.

A This is a mineral horizon or horizons formed at or near the surface in
the zone of leaching or removal of materials in solution and suspension
or of maximum in situ accumulation of organic matter, or both. Included
are:

1\. horizons in which organic matter has accumulated as a result of
biological activity (Ah);

2\. horizons that have been eluviated of clay, iron, alumin-ium, or
organic matter, or all of them (Ae);

3\. horizons having characteristics of 1) and 2) above but transitional
to underlying B or C (AB or A and B);

4\. horizons markedly disturbed by cultivation or pasture (Ap).

B This is a mineral horizon or horizons characterized by one or more of
the following:

1\. an enrichment in silicate clay, iron, aluminum, or humus, alone or
in combination (Bt,Bf,Bfh,Bhf, and Bh);

2\. a prismatic or columnar structure that exhibits pronounced coatings
or stain-ings and significant amount of exchangeable Na (Bn);

3\. an alteration by hydrolysis, reduction, or oxidation to give a
change in color or structure from horizons above or below, or both, and
does not meet the requirements of 1) and 2) above (Bm,Bg).

C This is a mineral horizon or horizons comparatively unaffected by the
pedogenic processes operative in A and B, excepting (i) the process of
gleying, and (ii) the accumulation of calcium and magnesium carbonates
and more soluble salts (Cca,Csa,Cg, and C). Marl and diatomaceous earth
are considered to be C horizons.

R This is consolidated bedrock that is too hard to break with the hands
or to dig with a spade when moist and that does not meet he requirement
of a C horizon. The boundary between the R layer and overlying
unconsolidated material is called a lithic contact.

W This is a layer of water in Gleysolic, Organic, or Cryosolic soils. It
is called a hydric layer in Organic soils.

**LOWER-CASE SUFFIXES**

b Buried soil horizon.

c A cemented (irreversible) pedo-genic horizon. The ortstein of a
Podzol, and a layer cemented by calcium carbonate and a duripan are
examples.

ca A horizon with secondary carbonate enrichment where the concentration
of lime exceeds that present in the unenriched parent material. It is
more than 10 cm thick, and if it has a CaCO3 equivalent of less than 15
percent it should have at least 5 percent more CaCO3 equivalent than the
parent material (IC). If it has more than 15 percent CaCO3 equivalent it
should have 1/3 more CaCO3 equivalent than the IC. If no IC is present,
this horizon is more than 10 cm thick and contains more than 5 percent
by volume of secondary carbonates in concretions or soft, powdery forms.

cc Cemented (irreversible) pedogenic concretions.

e A horizon characterized by the eluviation of clay, iron, aluminum, or
organic matter alone or in combination. When dry, it is usually higher
in color value by 1 or more units than an underlying B horizon. It is
used with A (Ae).

f A horizon enriched with amorphous material, principally Al and Fe
combined with organic matter. It usually has a hue of 7.5YR or redder or
its hue is 10YR near the upper boundary and becomes yellower with depth.
When moist, the chroma is higher than 3 or the value is 3 or less. It
contains 0.6% or more pyrophosphate-extractable Al+Fe in textures finer
than sand and 0.4% or more in sands (coarse sand, sand, fine sand, and
very fine sand). The ratio of pyrophosphate-extractable Al+Fe to clay
(less than 0.002mm) is more than 0.05 and organic C exceeds 0.5%.
Pyrophosphate-extractable Fe is at least 0.3%, or the ratio of organic C
to pyrophosphate-extractable Fe is less than 20, or both are true. It is
used with B alone (Bf), with B and h (Bhf), with B and g (Bfg), and with
other suffixes. The criteria for \"f\" do not apply to Bgf horizons. The
following horizons are differentiated on the basis of organic carbon
content: Bf - 0.5% to 5% organic carbon. Bhf-more than 5% organic
carbon.

g A horizon characterized by gray colors, or prominent mottling, or
both, indicative of permanent or periodic intense reduction. Chromas of
the matrix are generally 1 or less. It is used with A and e (Aeg); with
B alone (Bg); with B and f (Bfg); with B, h, and f (Bhfg); with B and t
(Btg); with C alone (Cg); with C and k (Ckg); and several others. In
some reddish parent materials, matrix colors of reddish hues and high
chromas may persist despite long periods of reduction. In these soils,
horizons are designated as g if there is gray mottling or if there is
marked bleaching on ped faces or along cracks.

Aeg This horizon must meet the definitions of A,e, and g.

Bg These horizons are analogous to Bm horizons but they have colors
indicative of poor drainage and periodic reduction. They include
horizons occurring between A and C horizons in which the main features
are (i) colors of low chroma, that is: chromas of 1 or less, without
mottles on ped surfaces or in the matrix if peds are lacking; or chromas
of 2 or less in hues of 10YR or redder, on ped surfaces or in the matrix
if peds are lacking, accompanied by more prominent mottles than those in
the C horizon; or hues bluer than 10Y, with or without mottles on ped
surfaces or in the matrix if peds are lacking. (ii) colors indicated in
(i) and a change in structure from that of the C horizons. (iii) color
indicated in (i) and illuviation of clay too slight to meet the
requirements of Bt; or accumulation or iron oxide too slight to meet the
limits of Bgf. (iv) colors indicated in (i) and removal of carbonates.
Bg horizons occur in some Orthic Humic Gleysols and some Orthic
Gleysols.

Bfg, Bhfg, Btg, and others. When used in any of these combinations the
limits set for f, hf, t, and others must be met.

Bgf The dithionite-extractable Fe of this horizon exceeds that of the IC
by 1% or more. Pyrophosphate-extractable Al + Fe is less than the
minimum limit specified for \'f\' horizons. This horizon occurs in Fera
Gleysols and Fera Humic Gleysols, and possibly below the Bfg of gleyed
Podzols. It is distinguished from the Bfg of gleyed Podzols on the basis
of the extractability of the Fe and Al. The Fe in the Bgf horizon is
thought to have accumulated as a result of the oxidation of ferrous
iron. The iron oxide formed is not associated intimately with organic
matter or with Al, and it is sometimes crystalline. The Bgf horizons are
usually prominently mottled, with more than half of the soil material
occurring as mottles of high chroma.

Cg, Ckg, Ccag, Csg, Csag. When g is used with C alone, or with C and one
of the lowercase suffixes k, ca, s, or sa, it must meet the definition
for C and for the particular suffix.

h A horizon enriched with organic matter. It is used with A alone (Ah);
or with A and e (Ahe); or with B alone (Bh); or with B and f (Bhf).

Ah A horizon enriched with organic matter that either has a color value
at least one unit lower than the underlying horizon or contains 0.5%
more organic carbon than the IC, or both. It contains less than 17%
organic carbon by weight.

Ahe An Ah horizon that has undergone eluviation as evidenced, under
natural conditions, by streaks and splotches of differing shades of gray
and often by platy structure. It may be overlain by a darker-colored Ah
and underlain by a lighter colored Ae.

Bh This horizon contains more than 1% organic carbon, less than 0.3%
pyrophosphate-extractable

> Fe, and has a ratio of organic carbon to pyrophosphate-extractable of
> 20 or more. Generally the color value and chroma are less than 3 when
> moist.

Bhf Defined under \'f\'.

j Used as a modifier of the suffixes e, f, g, n, and t to denote an
expression of, but failure to meet, the specified limits of the suffix
it modifies. It must be placed to the right and adjacent to the suffix
it modifies. For example Bfgj means a Bf horizon with weak expression of
gleying; Bfjgj means a B horizon with weak expression of both \'f\' and
\'g\' features.

Aej It denotes an eluvial horizon that is thin, discontinuous or
slightly discernible.

Btj It is a horizon with some illuviation of clay, but not enough to
meet the limits of Bt.

Btgj, Bmgj. Horizons that are mottled but do not meet the criteria of
Bg.

Bfj It is a horizon with some accumulation of pyrophosphate-extractable
Al and Fe but not enough to meet the limits of Bf.

Bntj or Bnj. Horizons in which development of solonetzic B properties is
evident but insufficient to meet the limits for Bn or Bnt.

k Denotes the presence of carbonate, as indicated by visible
effervescence when dilute HCl is added. Most often it is used with B and
m (Bmk) or C (Ck), and occasionally with Ah or Ap (Ahk, Apk), or organic
horizons (Ofk, Omk).

m A horizon slightly altered by hydrolysis, oxidation, or solution, or
all three, to give a change in color or structure, or both. It has:

1\. Evidence of alteration in one of the following forms:

a\) Higher chromas and redder hues than the underlying horizons.

b\) Removal of carbonates, either partially (Bmk) or completely (Bm).

2\. Illuviation, if evident, too slight to meet the requirements of a Bt
or a podzolic B.

3\. Some weatherable minerals.

4\. No cementation or induration and lacks a brittle consistence when
moist. This suffix can be used as Bm, Bmgj, Bmk, and Bms.

n A horizon in which the ratio of exchangeable Ca to exchangeable Na is
10 or less. It must also have the following distinctive morphological
characteristics: prismatic or columnar structure, dark coatings on ped
surfaces, and hard to very hard consistence when dry. It is used with B,
as Bn or Bnt.

p A horizon disturbed by man\'s activities, such as cultivation,
logging, habitation, etc. It is used with A and O.

s A horizon with salts, including gypsum, which may be detected as
crystals or veins, as surface crusts of salt crystals, by depressed crop
growth, or by the presence of salt-tolerant plants. It is commonly used
with C and k (Csk), but can be used with any horizon or combination of
horizon and lowercase suffix.

sa A horizon with secondary enrichment of salts more soluble than
calcium and magnesium carbonates, in which the concentration of salts
exceeds that present in the unenriched parent material. The horizon is
10 cm or more thick. The conductivity of the saturation extract must be
at least 4 ms/cm and must exceed that of the C horizon by at least
onethird.

t An illuvial horizon enriched with silicate clay. It is used with B
alone (Bt), with B and g (Btg), with B and n (Bnt), etc.

Bt A Bt horizon is one that contains illuvial layer lattice clays. It
forms below an eluvial horizon, but may occur at the surface of a soil
that has been partially truncated. It usually has a higher ratio of fine
clay to total clay than IC. It has the following properties:

1\. If any part of an eluvial horizon remains and there is no lithologic
discontinuity between it and the Bt horizon, the Bt horizon contains
more total and fine clay than the eluvial horizons, as follows:

a\) If any part of the eluvial horizon has less than 15% total clay in
the fine earth fraction (2mm) the Bt horizon must contain at least 3%
more clay, e.g., Ae 10% clay Bt minimum 13% clay.

b\) If the eluvial horizon has more than 15% and less than 40% total
clay in the fine earth fraction, the ratio of the clay in the Bt horizon
to that in the eluvial horizon must be 1.2 or more, e.g., 20% clay
increase in the Bt over Ae.

c\) If the eluvial horizon has more than 40% total clay in the fine
earth fraction, the Bt horizon must contain at least 8% more clay than
the eluvial horizon, e.g. Ae 50% clay; Bt at least 58% clay.

2\. A Bt horizon must be at least 5 cm thick. In some sandy soils where
clay accumulation occurs in the lamellae, the total thickness of the
lamellae should be more than 10 cm in the upper 150 cm of the profile.

3\. In massive soils the Bt horizon should have oriented clays in some
pores and also as bridges between the sand grains.

4\. If peds are present, a Bt horizon shows clay skins on some of the
vertical and horizontal ped surfaces and in the fine pores, or shows
oriented clays in 1% or more of the cross section, as viewed in thin
section.

5\. If a soil shows a lithologic discontinuity between the eluvial
horizon and the Bt horizon, or if only a plow layer overlies the Bt
horizon, the Bt horizon need show only clay skins in some part, either
in some fine pores or on some vertical and horizontal ped surfaces. Thin
sections should show that some part of the horizon has about 1% or more
of oriented clay bodies.

Btj, Btj, and Btg are defined under j and g.

u A horizon that is markedly disrupted by physical or faunal processes
other than cryoturbation. Evidence of marked disruption such as the
inclusion of material from other horizons, absence of the horizon, etc.
must be evident in at least half of the cross section of the pedon. Such
turbation can result from blowdown of trees, mass movement of soil on
slopes, and burrowing animals. It can be used with any horizon or
subhorizon with the exception of A or B alone; e.g. Aeu, Bfu, BCu.

x A horizon of fragipan character. A fragipan is a loamy subsurface
horizon of high bulk density and very low organic matter content. When
dry, it has a hard consistence and seems to be cemented. When moist, it
has moderate to weak brittleness. It frequently has bleached fracture
planes and is overlain by a friable B horizon. Air dry clods of fragic
horizons slake in water.

y A horizon affected by cryoturbation as manifested by disrupted and
broken horizons, incorporation of materials from other horizons and
mechanical sorting in at least half of the cross section of the pedon.
It is used with A, B, and C alone or in combination with other
subscripts, e.g. Ahy, Ahgy, Bmy, Cy, Cgy, Cygj, etc.

z A frozen layer. It may be used with any horizon or layer, e.g. Ohz,
Bmz, Cz, Wz.