SOILS of CENTRAL and NORTHERN NEW BRUNSWICK New Brunswick Soil Survey Report No

SOILS OF CENTRAL AND NORTHERN NEW BRUNSWICK New Brunswick Soil Survey Report No. 12

Research Branch - Potato Research Centre - Fredericton New Brunswick 2005

Agriculture and Agriculture et Agri-Food Canada Agroalimentaire Canada Canada SOILS OF CENTRAL AND NORTHERN NEW BRUNSWICK New Brunswick Soil Survey Report No. 12

H. W. Rees, S. H. Fahmy, C. Wang and R. E. Wells

Potato Research Centre Agriculture and Agri-Food Canada Fredericton, New Brunswick

PRC Contribution No. 05-01 (Map sheet)

Agriculture and Agri-Food Canada Research Branch 2005

Copies of this publication are available from:

Potato Research Centre, Agriculture and Agri-Food Canada P. O. Box 20280, 850 Lincoln Road, Fredericton, New Brunswick, E3B 4Z7

New Brunswick Department of Agriculture, Fisheries and Aquaculture Box 6000, Lincoln Road, Fredericton, New Brunswick, E3B 5H1

Electronic copies of this publication and digital maps are available for downloading free of charge from the Agriculture and Agri-Food Canada web site of the Canadian Soil Information System (CanSIS) at: http://sis.agr.gc.ca/cansis

Correct citation as follows:

Rees, H. W., Fahmy, S. H., Wang, C. and Wells, R. E. 2005. Soils of Central and Northern New Brunswick. Potato Research Centre, Research Branch, Agriculture and Agri-Food Canada, Fredericton, N. B. 137 pp with map. iii

CONTENTS

ACKNOWLEDGMENTS...... vii SUMMARY...... viii INTRODUCTION...... 1

PART 1. GENERAL DESCRIPTION OF THE AREA...... 3 Location and extent ...... 3 Land use...... 3 Forestry...... 3 Agriculture...... 4 Mining...... 4 Recreation...... 4 Land ownership...... 5 Physiography, topography, drainage and bedrock geology ...... 5 Climate...... 8 Atmospheric climate...... 8 Soil climate...... 9 Vegetation ...... 9

PART 2. SOIL FORMATION AND CLASSIFICATION...... 11 Surficial geology...... 11 Soil parent materials ...... 11 Mineral soils...... 11 Organic soils...... 12 Soil development and soil forming factors...... 13 Soil profile...... 14 System of soil classification...... 15 Soil Orders in central and northen New Brunswick...... 16 Brunisolic Soils ...... 16 Gleysolic Soils ...... 16 Luvisolic Soils ...... 16 Organic Soils ...... 16 Podzolic Soils ...... 16 Regosolic Soils ...... 19 Impact of agriculture on soil classification...... 20 Relationship between soil classification and soil mapping...... 20

PART 3. SOIL MAPPING METHODOLOGY...... 21 Office m ethods...... 21 Field m ethods...... 21 M ap sym bol...... 22 Land types ...... 27 Soil correlation with established soil concepts...... 27

PART 4. SOIL ASSOCIATION IDENTIFICATION KEY AND GENERAL DESCRIPTION...... 31 Key to soil association parent materials...... 31 Soil association general description...... 31 Acadie Siding Association...... 31 Barrieau-Buctouche A ssociation...... 35 Belldune R iver Association...... 37 Big Bald Mountain Association...... 38 Boston Brook Association...... 40 Caribou Association...... 42 Carleton Association...... 44 Catamaran Association...... 47 iv

Gagetown Association...... 49 Grand Falls Association...... 51 Guim ond R iver Association...... 53 Holm esville Association...... 55 Interval Association...... 57 Jacquet River Association...... 59 Juniper Association...... 61 Lavillette Association...... 63 Long Lake Association...... 65 M aliseet Association...... 67 M cG ee Association...... 68 M uniac Association...... 71 Nigadoo R iver Association...... 73 Parleeville Association...... 74 Popple Depot A ssociation...... 76 Reece Association...... 77 Richibucto Association ...... 80 Riverbank Association...... 82 Rogersville Association ...... 84 Stony B rook Association...... 85 St. Quentin Association...... 87 Sunbury Association...... 89 Tetagouche Association...... 91 Tetagouche Falls Association...... 92 Thibault Association...... 94 Tracadie Association...... 96 Tuadook Association...... 98 Violette A ssociation...... 100 Land types...... 102 Salt Marsh...... 102 Sand Dunes...... 102 W ater...... 102

PART 5. ELECTRONIC DATA FILES...... 103 File structure...... 103 Project File (PF)...... 103 Polygon attribute table file (PAT)...... 104 Soil M ap Unit File (SM UF)...... 104 Soil N am e File (SNF)...... 104 Soil L ayer File (SLF)...... 105

PART 6. INTERPRETATIONS - SINGLE FACTOR AND GENERAL AGRICULTURE AND FORESTRY RATINGS ...... 107 Single-factor soil map unit conditions ...... 107 Canada Land Inventory Classification ...... 110 Soil capability classification for agriculture...... 110 Land capability classification for forestry ...... 111

REFERENCES...... 127 GLOSSARY - GENERAL TERMS...... 129 GLOSSARY - ROCK TYPES ...... 135 APPENDIX - COMMON AND SCIENTIFIC NAMES OF TREES...... 137 v

LIST OF TABLES AND ILLUSTRATIONS

TABLES

1. Soil association members of the central and northern New Brunswick map area classified according to the C anadian System of Soil C lassification ...... 18 2. Soil m apping legend ...... 23 3. C orrelation of soil associations m apped in central and northern N ew Brunswick with established soil series ...... 28 4. K ey to soil association parent materials in the central and northern N ew Brunswick m ap area .. 32 5. Selected interpretations of soil map units ...... 112

FIGURES

1. Areas of New Brunswick for which reconnaissance soil surveys have been published by New Brunswick Soil Survey ...... 1 2. Physiographic regions of the survey area ...... 6 3. B edrock geology of the survey area...... 7 4. Climatic zones within the survey area ...... 9 5. Forest regions and sections within the survey area...... 10 6. D iagram m atic horizon patterns of various soil profiles...... 17 7. Location of m apped A cadie Siding soils ...... 31 8. Location of m apped B arrieau-Buctouche soils ...... 35 9. W ell drained B arrieau-Buctouche soil profile ...... 36 10. Location of m apped B elledune River soils ...... 37 11. W ell drained B elledune River soil profile ...... 38 12. Location of m apped B ig B ald M ountain soils ...... 39 13. Big Bald M ountain soil association landscape showing “tors” ...... 39 14. W ell drained B ig B ald M ountain soil profile ...... 39 15. Location of m apped B oston Brook soils ...... 41 16. Location of m apped C aribou soils ...... 42 17. Well drained Caribou soil profile, veneer phase ...... 43 18. Location of m apped C arleton soils ...... 45 19. W ell drained C arleton soil profile ...... 46 20. Location of m apped C atam aran soils ...... 47 21. M oderately w ell drained C atamaran soil profile ...... 48 22. Location of m apped G agetown soils ...... 49 23. Rapidly drained Gagetown soil profile ...... 50 24. Location of m apped G rand Falls soils ...... 51 25. Rapidly drained Grand Falls soil profile ...... 52 26. Location of m apped G uim ond R iver soils ...... 53 27. Location of m apped H olm esville soils ...... 55 28. Well drained Holmesville soil profile, cultivated ...... 56 29. Provincial soil badge ...... 56 30. Location of m apped Interval soils ...... 57 31. Interval soil association landscape ...... 58 32. Im perfectly drained Interval soil profile ...... 58 33. Location of m apped Jacquet R iver soils ...... 59 34. Location of m apped Juniper soils ...... 61 35. Juniper soil association landscape and surface stones/boulders ...... 61 36. W ell drained Juniper soil profile ...... 62 37. Location of m apped L avillette soils ...... 63 38. Lavillette soil association landscape ...... 64 39. Location of m apped L ong L ake soils ...... 65 40. W ell drained L ong L ake soil profile ...... 66 vi

FIGURES cont’d

41. Location of m apped M aliseet soils ...... 67 42. Location of m apped M cG ee soils ...... 69 43. W ell drained M cG ee soil profile ...... 70 44. Location of m apped M uniac soils ...... 71 45. Location of m apped N igadoo R iver soils ...... 73 46. W ell drained N igadoo R iver soil profile ...... 73 47. Location of m apped Parleeville soils ...... 75 48. Location of m apped Popple Depot soils ...... 76 49. Location of m apped R eece soils ...... 78 50. W ell drained R eece soil profile ...... 79 51. Location of m apped R ichibucto soils ...... 80 52. Well drained Richibucto soil profile, veneer phase ...... 81 53. Location of m apped R iverbank soils ...... 82 54. Rapidly drained Riverbank soil profile ...... 83 55. Location of m apped R ogersville soils ...... 84 56. Location of m apped Stony B rook soils ...... 86 57. M oderately w ell drained Stony B rook soil profile ...... 87 58. Location of m apped St. Quentin soils ...... 88 59. Location of m apped Sunbury soils ...... 89 60. W ell drained Sunbury soil profile ...... 90 61. Location of m apped T etagouche soils ...... 91 62. Location of m apped T etagouche Falls soils ...... 92 63. W ell drained T etagouche Falls soil profile ...... 93 64. Location of m apped T hibault soils ...... 94 65. W ell drained T hibault soil profile ...... 95 66. Location of m apped T racadie soils ...... 97 67. Poorly drained Tracadie soil profile ...... 97 68. Location of m apped T uadook soils ...... 98 69. W ell drained T uadook soil profile ...... 99 70. Location of m apped V iolette soils ...... 100 71. M oderately w ell drained V iolette soil profile ...... 101 vii

ACKNOWLEDGMENTS

The authors extend special recognition to the Laboratory and office space were provided by following: D. Keys, formerly New Brunswick Agriculture Canada's Fredericton Research Station Departm ent of Natural Resources, Mineral (now Agriculture and Agri-Food C anada’s Potato Resources Branch, Peatland Inventory Section, who Research C entre). provided inform ation on the organic soils of the area; B. M . Sm ith (retired), New Brunswick Department The soil map and illustrations were prepared by Janet of Natural Resources, Forest Management Branch, Cummings and A ndré Villeneuve, Canadian Soil who supplied data from the New Brunswick Forest Information System (CanSIS), Eastern C ereal and Inventory; staff of the Analytical Service Laboratory Oilseed Research C entre, Agriculture and Agri-Food of Agriculture Canada's Land Resource Research Canada, Ottawa. Centre (now Agriculture and Agri-Food Canada’s Eastern Cereal and Oilseed Research Centre), who Acknowledgment is made to Gary Patterson, Acting conducted soil chemical and physical analyses in National Soil Correlator, Agriculture and Agri-Food support of field work; and the many others who Canada, Truro, Nova Scotia, for his technical review assisted in field work, laboratory analyses, and of the m anuscript. drafting. viii

SUMMARY

The area surveyed encompasses most of central and northern Lawrence and Boreal Forest Regions. Impeded drainage in New Brunswick, occupying 2.79 million ha (6.89 million ac) the lowlands has lead to a prevalence of pure stands of black or approximately one third of the total land area of the spruce, red spruce, and balsam fir or mixed wood in which province. This includes all of Restigouche and Gloucester these species are associated with eastern white pine, red counties, most of Northumberland county, the northern half maple, trembling aspen, sugar maple, yellow birch, and of York county and the northeast tip of Carleton county. The white birch. While the higher altitudes of the New survey area occupies parts of the Maritime Plain, New Brunswick Highlands section are dominated by coniferous Brunswick Highlands, Chaleur Uplands and Notre Dame forests of balsam fir, black spruce, white spruce and white Mountains of the Appalachian Region. The level to gently birch, at lower altitudes, crests and upper slopes are forested undulating landscapes of the Maritime Plain along the Gulf with sugar maple, yellow birch and beech; middle slopes of St. Lawrence are strongly contrasted by the rugged, more include a component of red and white spruce, eastern hilly nature of the Highlands, Uplands and Mountains, hemlock and balsam fir; and lower slopes and depressions which reach elevations of in excess of 800 m. The area is support primarily coniferous stands of spruces, fir, eastern drained mainly by tributaries of the Saint John River to the white cedar and tamarack. The Chaleur Uplands are west, the Miramichi River to the east and the Restigouche similarly characterized by forests of sugar maple, beech and and Nepisiguit Rivers to the north. yellow birch on the hill tops with balsam fir and spruce in the valleys. In the northwest, the Notre Dame Mountains are Despite its mid-latitude maritime location, the survey area dominated by coniferous forest cover types of balsam fir, has a modified continental climate with prevailing westerly black spruce and white spruce with some eastern white cedar winds blowing offshore, resulting in a more extreme climate and white birch. similar to inland Canada. Within the survey area two influences dominate the climate - the moderating effect of Forest production and forestry-related activities constitute the Atlantic Ocean along the eastern shore and the cooling the single largest land use. More than 90% of the area is effect of increased elevations in central and northwestern productive woodland, whereas less than 2% of the land base New Brunswick. Annual daily mean air temperature ranges is used for agricultural purposes. Most of the agricultural from 2.0 to 5.2oC. The southern and eastern most areas have activity in the survey area is scattered along the north shore the longest frost-free periods with in excess of 130 days from Campbellton and Dalhousie through Belledune and while in the central and northwestern regions the average Bathurst over to Caraquet and then south along the east frost-free period is less than 90 days. Annual precipitation coast from Shippegan and Tracadie down to the ranges from 1000 to over 1200 mm per year, of which 280 Newcastle-Chatham area, and somewhat inland along the to 380 cm (280 to 380 mm of water equivalent) occur as Miramichi River and its tributaries. Another area of snowfall. Mean annual soil temperature varies from 2 to agricultural significance is the St. Quentin-Kedgwick area. 8°C. In general, farmlands occur in small parcels interspersed between larger areas of forested land. Bedrock geology is relatively simple and uncomplicated in the northeastern Maritime Plain portion of the survey area, Soil parent materials vary widely but are dominated by ice- with 90% underlain by horizontal to gently dipping, Penn- deposited sediments. Glaciers, which covered the entire sylvanian age, sedimentary rocks, predominately gray-green region during Wisconsin glaciation, scoured all preglacial sandstone. The Chaleur Upland and Notre Dame Mountains surfaces and subsequently deposited a mantle of glacial drift to the west are underlain by a mixture of vertically-standing of varying thickness. Thickness of the drift generally ranges greywacke, slate, sandstone, limestone and conglomerate from less than 1 to 2.5 m. Of the glacial materials, thin with minor volcanic rocks of rhyolite, trachyte and basaltic deposits consisting of less than 1 m of loamy-textured, flows. The Miramichi Highlands are underlain by a number compact, lodgment tills or slightly thicker 1 to 2 m of coarse of bedrock types, with the northern portions consisting of loamy-textured, loose, ablational till, are by far the most formations of silicic volcanic rocks, rhyolite, rhyolite- abundant. The general direction of glacier movement was to porphyry, silicic tuffaceous rocks and metamorphosed the southeast. Thus, texture, color and coarse fragment equivalents, quartz and quartz-feldspar schist, with some lithology of lodgment tills closely resemble the underlying mafic volcanic flows. The southern portion is rich in bedrock or bedrock to the northwest. Ablation tills may granites and granodiorites with argillaceous sedimentary have a more wide-ranging lithological composition and rocks, greywacke, quartz, conglomerate and minor weaker ties to the underlying bedrock type. Excluding the limestone, tuff and volcanic flows. northern half of the Acadian Peninsula where reddish brown tills are common, most tills are yellowish to olive brown or Central and northern New Brunswick includes parts of three grey. Relatively few glaciofluvial deposits are present. major forest regions - the Acadian, Great Lakes-St. Following deglaciation, the lowlands portion of the survey ix area was submerged by sea water. However, marine deposi- Reduced soil quality for biological growth as a result of low tions are confined to a narrow zone along the coastline. Both fertility (caused by a lack of available nutrients, high acidity, fine- and coarse-textured marine sediments occur. Soil and and low exchange capacity), and adverse climate, prevails climatic conditions of the region promote paludification throughout the survey area, as it does throughout most of (the formation of peat), especially in the lowlands portion. Atlantic Canada. Undesirable soil structure and low per- Some bogs have attained thicknesses of more than 5 m. meability, often resulting in excess soil moisture, are Alluvial deposits, although associated to some degree with inherent limitations in the compact lodgment tills. Slope most stream and river courses, are restricted in area. limitations occur throughout much of the upland and highland areas. Excessive stoniness plagues the looser, Of the nine orders defined in The Canadian System of Soil ablational tills. Low moisture-holding capacity affects the Classification, six are present in the study area: Brunisolic, coarse-textured marine and glaciofluvial materials. The Gleysolic, Luvisolic, Organic, Podzolic, and Regosolic more fertile alluvial deposits are subject to flooding. Most orders. Podzolization is the dominant soil-forming process. organic soils are considered as nonproductive forest lands, Well-drained Podzols dominate the morainal tills in the and their potential for agricultural development is, at best, Upland and Highland areas while imperfectly drained Luvi- moderate. sols and poorly drained Gleysols dominate the morainal tills on the Maritime Plain lowlands. Luvisolic development in Interpretations for agriculture and forestry uses vary greatly these acidic materials is weakly expressed. In general, the with soil material and site conditions. Alluvial deposits are strongest Luvisolic development is found in the marine clays the best sources for topsoil. Sands are abundant along the scattered along the coast.. Well- and imperfectly drained, coast, but deposits are typically thin in nature. Gravel coarse-textured, marine and glaciofluvial deposits are also reserves are scattered sparsely throughout the inland portion Podzols. Their poorly drained counterparts are usually of the survey area. Organic soils are potential sources of Brunisols. Regosols are found on alluvial sites where horticultural and fuel peat. ongoing deposition disrupts horizon formation. Soils of the Organic order are either deep accumulations of poorly to very poorly drained sphagnum, or thinner deposits of moderately decomposed sedge-sphagnum or well decomposed forest peats. They occur throughout the study area but are most prominent in the Maritime Plain. x 1

INTRODUCTION

Soil survey is "the whole procedure involved in making a Initial soils mapping was conducted from 1978 to 1981, and soil resource inventory. It includes the initial plan, the field the information was placed on open file. This publication investigations, creating the legend, drawing the map, presents the completed results of the survey, consisting of describing and sampling the soils, analysing the samples, two components-- the report and the soil map. writing the report and preparing the interpretations" (Map- ping Systems Working Group, 1981). The report is divided into six parts. Part 1 describes the location and extent of the surveyed area, the present land This report is the twelfth in a series dealing with soils and uses, and the natural resources - physiography, topography, landscapes in New Brunswick (Fig. 1). The area is located drainage, vegetation, climate, and bedrock geology. Part 2 in central and northern New Brunswick. Soils were mapped discusses soil formation and explains how soils are clas- at a l:250 000 exploratory level, with the objectives of sified. It also outlines soil parent materials and modes of providing an inventory of soil resources by showing their deposition and summarizes soil development and the system distribution on a map and describing their characteristics and of classification used. Part 3 deals with soil mapping limitations. Such base information is a prerequisite for procedures. Part 4 includes a key to soil association parent competent resource management and land use planning. materials and describes the mapped soil associations in Information provided in this report was designed to be terms of topographic conditions, material composition, multipurpose in nature. drainage, classification, and related soils. Part 5 outlines how the data is stored in electronic files that allow for greater ability to manipulate and apply the information in a consistent and timely manner. Part 6 presents general interpretations of the soil map units for agriculture and forestry.

While the text of the report provides technical information on soil and landscape properties and rates general suitabilities of the mapped soils, the distribution (location and extent) of the various kinds of soils are displayed on a 1:300,000 scale line map located in the pocket on the inside of the back cover of the report. A published map scale of 1:300,000 was used for logistical reasons - overall map size, and the ability to present the entire map on one sheet. The map includes a map legend which briefly summarizes soil properties and landscape features typical of each mapped soil association or land type.

Limitations to the use of the soils information conveyed by the soil map and report must be appreciated. The data presented is generally only for soil materials to a depth of one metre. Discussions on materials below 1 metre are estimates based on occasional field observations. Also, the reliability and accuracy of this data is commensurate with a 1:250 000 map scale. Because of this exploratory scale of mapping, significant areas of soils that differ from the identified dominant soils may be included in the map units. Figure 1. Areas of New Brunswick for which reconnaissance Enlargement or “blowing up” of this map can cause a soil surveys have been published by New Brunswick Soil serious misunderstanding of the detail of mapping and can Survey. result in erroneous interpretations. The information in this soil survey provides a preliminary definition or overview of Information provided in this report is relevant for provincial, the general qualities of the different land areas within the regional and national land use planning,, but it should also mapped area. It does not eliminate the need for on-site prove useful to urban developers, foresters, highway investigation, testing and analysis before implementing any engineers, land use planners, and interested members of the intended use. public, as well as to farmers, agricultural engineers, and agronomists. 2 3

PART 1. GENERAL DESCRIPTION OF THE AREA

LOCATION AND EXTENT Forestry Forested lands account for 92.9% of the survey area. This The area surveyed encompasses most of central and northern represents in excess of 2.59 million ha. Of these forested New Brunswick. The location of the map area, with respect lands 93.4% is stocked, 3.9% is disturbed (planted, cut or to other published soil survey report map areas, is shown in burnt) and 2.7% is nonproductive (Smith 1982). Average Fig. 1. More specifically its boundary runs east along the volume of harvestable wood (greater than 12 cm dbh, New Brunswick - Quebec border to Chaleur Bay, south diameter at breast height or 4.5 ft above the forest floor) along the Northumberland Strait coastline to Miramichi Bay, varies from 50 to 125 cubic metres per hectare (Smith west along the Little SW Miramichi River to longitude 65o 1982). The coastal lowlands around Point Verte, Bathurst, 45', south to latitude 46o 30', west to longitude 66o 30', south Caraquet, Burnsville, Tabusintac and Chatham average only to latitude 46o 00', west to the Nackawic Stream, northwest 50 to 90 m3/ha. The depleted condition of these forests is along the Nackawic Stream to longitude 67o 22.5', north to due to insect infestations (primarily spruce budworm), latitude 46o 30', east to longitude 67o 00', north to the disease, fire and mismanagement (high-grading, little or no Victoria county line, northeast along the Victoria county line reforestation, etc.) This area of northeastern New to the York county line, northeast along the York county Brunswick has experienced the most severe levels of annual line to the Northumberland county line, northwest along the burn in the province. Mean annual burn is 0.43%, which Northumberland county line to the Restigouche county line, represents a fire rotation period of about 230 years (Wein and then northwest along the Restigouche county line to the and Moore, 1977.). In contrast to this, the central and New Brunswick - Quebec border. This includes all of western uplands average 90 to 125 m3 of merchantable wood Restigouche and Gloucester counties, most of volume per hectare. The most productive regions within this Northumberland county, the northern half of York county area are around States Brook-Menneval in the northwest and and the northeast tip of Carleton county. It covers parts of Serpentine Lake-Tuadook Lake-McKendrick the national topographic map-sheets (1:250,000 scale) for Lake-Hayesville-Coldstream-Millville in the southwest, Bathurst (21-P), Campbellton (21-O), Edmundston (21-N), where average hectare yields are 110 to 125 m3. Spruce Matane (22-B), Moncton (21-I), and Woodstock (21-J). budworm infestations are a serious problem, but their control through aerial spray programs is probably more The survey area occupies 2.79 million ha (6.89 million ac) successful than in settled areas where spraying was either or approximately one third of the total land area of the banned or less effective due to the sporadic pattern of province. The principal centres of population within the area application. North central and northwestern New Brunswick are the cities of Bathurst (pop. 15,705) and Campbellton are also areas of low annual burn. Large fires have only (9,818), the towns of Caraquet (4,315), Dalhousie (5,707), occurred recently, corresponding to improved access for tree Lameque (1,571), Newcastle (6,284), Shippagan (2,726) and harvesting and recreation . Tracadie (2,452) and the major villages of Atholville (1,694), Balmoral (1,823), Bas Caraquet (1,859), Beresford Softwoods predominate, especially spruce and balsam fir, (3,652), Charlo (1,603), Neguac (1,755), Petit Rocher with lesser amounts of jack pine, white pine, red pine and (1,860) and Saint Quentin (2,334). cedar. Hardwoods, sugar maple, red maple, yellow birch, white birch, ash, beech and poplar, make up 15 to 45% of the forest community. (See the section on vegetation for a LAND USE more detailed account of species distribution.). However, the total hardwood harvest is only about 10% of the total Major land users within the survey area are forestry, wood fibre harvest, indicating that hardwood is being agriculture, urbanization, mining and recreation. Land use significantly under-utilized. status is summarized below: While forest harvesting operations are for the most part Forest 92.9% labor intensive, skidders and chainsaws are increasingly Agriculture 2.0% giving way to more highly mechanized systems (feller Old Fields 0.8% bunchers, short wood harvesters, etc.). Most of the wood Water 0.9% fibre harvested is consumed by the pulp and paper industry. Open Wetlands 1.9% Several pulp and paper mills are located within the study Occupied (cities, towns, airports, etc.) 0.6% area (Athoville, Dalhousie, Bathurst, Newcastle) and a Facilities (roads, power lines, etc.) 0.8% number in close proximity (Nackawic, Edmundston). Products produced include kraft pulp, groundwood pulp, Source: Smith (1982). sulphide pulp, container board and newsprint. There are numerous sawmills operating within the area. Many of the 4 smaller mills are portable or home-made and operate In the southern portion of the survey area there is some intermittently. However, there are also a number of larger general farming in the Stanley-Williamsburg and Burtts mills with annual production exceeding 3 million fbm (foot- Corner-Millville areas. Dairy operations are particularly board-measure, equivalent to a piece of wood measuring 12" prevalent in the Burtts Corner-Millville area. x 12" square by 1" thick ). In addition to the pulpwood and sawlogs, other softwood products include veneer logs, Mining "stud" logs, poles and cedar logs. Hardwood products As a result of its complex geological history, central and include veneer logs, spoolwood and fuelwood. Christmas northen New Brunswick possess a great variety of mineral tree and maple syrup production are other woodland uses. resources. These include metals, non-metallic industrial Although small in land area involved, they are important minerals, fuel-energy resources and structural materials (N. assets in local economics. B. Department of Commerce and Development No date).

Agriculture Metallic mineral occurrences are concentrated in the central Agricultural land use within the study area accounts for highlands portion of the study area from approximately 2% of the total land area, representing some Campbellton-Bathurst south to Fredericton. Hugh 55,800 ha of cleared land (Smith 1982). An additional 0.8% zinc-copper-silver deposits were found near Bathurst in or 21,000 ha is abandoned farmland consisting of old fields 1952. They are presently being mined by Brunswick Mining reverting to forest. This indicates a 27% reduction in and Smelting Corporation Limited. A second operation, farmland, which is comparable to the provincial decline of Heath Steele Mines Limited, located northwest of 35% in total improved farmland over the period 1961 to Newcastle, was closed down due to low world metal prices. 1981 (N. B. Department of Agriculture and Rural Other metallic mineral discoveries include gold, iron, Development 1981). Agricultural development is strongly uranium, manganese, cobalt, nickel, tin, tungsten, beryl and related to the land base. With the exception of the flourite. Kedgwick-St. Quentin area, all of the central and northwestern portions of the study area are completely Non-metallic industrial minerals include limestone, granite, devoid of farmed land. Climatic, topographic and/or soil phosphate, marble, diabase, slates and silica. Only the conditions are too severe to permit agricultural limestone and silica are being actively worked and extracted. establishment. Undulating and gently rolling topography Both are at sites near Bathurst. coupled with more suitable soil parent materials (ie less stony and rocky), have allowed for a successful agricultural Fuel-energy resources are limited in their abundance. sector in the Kedgwick-St. Quentin vicinity, built around a Drillings have revealed coal deposits scattered along the worked farmland base of about 8,000 ha. Mixed farming is Northumberland Shore from Tabusintac to the norm, however, some specialization has taken place in Shippegan-Caraquet, but quantities and quality do not potato production. Other field crops include hay, oats and warrant development at the present time. Explorations have barley and minor amounts of mixed grain and corn. identified uranium deposits in the central highlands which show potential. Organic soils in the northeast are a source Most of the agricultural activity in the survey area is of peat which is presently being "mined" for horticultural scattered along the north shore from Campbellton and purposes. Suitability as an energy source is being Dalhousie through Belledune and Bathurst over to Caraquet considered. Experimentation with peat fueled greenhouse and then south along the east coast from Shippegan and heating was tried. Tracadie down to the Newcastle-Chatham area, and somewhat inland along the Miramichi River and its Sand, gravel and other aggregate structural materials are tributaries. Farmlands occur in small parcels interspersed quarried throughout the area. Most such operations are between larger areas of forested land. Most of the relatively small, servicing local needs only. Processing may topography is level to undulating and so it holds more or may not involve some screening. Some bedrock promise for agriculture, however, it is more likely that early materials, granites, slates, sandstone, etc., are also being settlement patterns are responsible for this agricultural utilized for things such as building materials, road fill and development. For many, farming has supplemented logging riprap. or fishing, or vice versa. Farming is general in nature, including the production of cattle, hogs and poultry and Recreation dairy and the associated cultivation of fields crops such as The recreational base in central and northern New hay, oats, barley and small areas of mixed grains and corn. Brunswick includes over 350 km of coastline, 2.7 million ha Vegetable production of potatoes, cabbage, cauliflower, of wilderness land and hundreds of small rivers, lakes and carrots and the like is for local consumption. Wild streams (N. B. Department of Commerce and Development blueberries are a traditional crop which is being encouraged No date). Recreational use of the land has become through land clearing and management of natural stands. increasingly important in recent years. Most of the recreational activity is centered on hunting and fishing. 5

Numerous species of both large and small game abound: of the New Brunswick Highlands. The Maritime Plain is moose, deer, bear, coyote, bobcat, muskrat, raccoon, fox, characterized by flat to gently undulating landscapes. mink, rabbit, ducks, geese, partridge and woodcock. Most Because of its flatness and owing to the nature of the soil noteworthy to the fisherman are the abundant salmon parent materials deposited during glaciation and post glacial streams, the Nashwaak, the Restigouche and the headwaters marine submergence, drainage is for the most part imperfect. of the infamous Miramichi. Other recreational activities Drainage is highly dependent upon relief. Well drained soils include canoeing, hiking, swimming, rock collecting, and are restricted to crests and upper slope positions. More nature watching in the summer, and snowshoeing, skiing and extensive areas of better drainage are associated with steeper snowmobiling in the winter. There are several game refuges slopes along the transition to the New Brunswick Highlands and provincial parks. Mount Carleton Provincial Park in or where streams are more strongly incised. The Nashwaak north central New Brunswick is particularly scenic. It also Hills are an example of this. They are well drained because encompasses the highest peak in the province, Mount of higher relief. The Nashwaak Hills are also the only Carleton, at 820 m above sea level (asl). portion of the Maritime Plains within the study area that do not drain into the Gulf of St Lawrence. The Nashwaak Hills Land Ownership drain via the Nashwaak and Saint John Rivers into the Bay Land ownership is divided into three categories: Crown of Fundy. The Central Lowlands and the southern portion land, 70%; large freehold, 9%; and small freehold, 21% of the Acadian Peninsula subdivisions of the Maritime Plain (Smith 1982). Crown lands are administered by the are drained by the Miramichi River into the Gulf of St provincial government. Freehold refers to lands that are Lawrence. The Central Lowlands consist of broad flat areas privately owned. Small freehold are parcels with less then with weakly expressed valleys. Other than for the areas 200 ha of land, usually in or adjacent to settled areas; large adjacent to the Southwest Miramichi River where local relief freehold are parcels with more than 200 ha of land. The is more pronounced, drainage is at best fair. A very poorly basic land tenure pattern of the study area was determined defined north-south oriented trough called the Curventon- by early settlement. Land ownership impacts directly on Bathurst Valley (Rampton et al. 1984) occurs along the land use. Distribution of small freehold properties is almost western edge of the Acadian Peninsula, separating it from identical to that of farmland distribution. Early land grant the New Brunswick Highlands. The Curventon-Bathurst patterns and subsequent subdivision of these original parcels Valley bottom is imperfect to poorly drained, with somewhat from generation to generation has resulted in numerous better drainage in the series of benches forming the valley relatively small land holdings. This is further aggravated by sides. Trough drainage is either north via the Nepisiguit the urbanization of rural lands. Large freehold properties River or south via the Northwest Miramichi River. The are concentrated in the southern portion of the survey area Acadian Peninsula is a gently sloping, eastward-facing around Tuadook Lake, Hayesville and Napadogan. Less imperfectly drained plain that descends from 150 m extensive blocks of large freehold are found along the elevation adjacent to the Curventon-Bathurst Valley to sea northwestern boundary, adjacent to Madawaska and Victoria level along the coast. It is drained by the Bartibog, Counties. As with Crown land, all large freehold is forested. Tabusintac, Tracadie and Pokemouche rivers into the Gulf In all freehold land, both large and small, the mineral rights of Saint Lawrence. Areas of better drainage occur where have been retained by the Province. these rivers are more deeply incised into the bedrock. The Maritime Plain is dominated by grey-green Pennsylvanian sandstone bedrock (Fig. 3) with only minor locally occurring PHYSIOGRAPHY, TOPOGRAPHY, DRAINAGE AND shale, siltstones and conglomerates. Some redbeds occur, BEDROCK GEOLOGY the largest concentration of which are in an area south of Bathurst. Most of the major landforms in central and northern New Brunswick are the result of tectonic (broad regional The New Brunswick Highlands with their more rugged and assemblage of structural or deformational features of the hilly landscapes are in stark contrast to the gently undulating earth crust) and erosional forces at play over the past Maritime Plain. Rampton et al (1984) subdivided this 135,000,000 years (Rampton et al. 1984). The survey area portion of the study area into four major divisions: the occupies parts of the Maritime Plain, New Brunswick Eastern, Northern, Central and Southern Miramichi Highlands, Chaleur Uplands and Notre Dame Mountains Highlands. The Eastern Miramichi Highlands are essentially (Fig. 2) of the Appalachian Region (Bostock 1970). a transition zone between the Maritime Plain and the new Brunswick Highlands proper. Elevations are typically below The Maritime Plain portion is also known as either the 350 m and landforms gently rolling with moderately good Central and Eastern Lowlands (Putnam 1952) or the New drainage. Gauthier (1983) described the Northern Brunswick Lowlands (Weeks 1957, Rampton et al. 1984). Miramichi Highlands as having “the highest summits of New It rises from sea level along the Northumberland Strait to Brunswick. They form a central undulating high plateau elevations greater than 150 m (500 ft) at its western boun- with an average elevation well above 600 metres. Mount dary where it grades into the Miramichi Highlands portion Carleton is the highest peak with an elevation of 820 6

Figure 2. Physiographic regions of the survey area based on Bostock (1970) as modified by Rampton et al. (1984).

metres.” Relief exceeds 200 m and streams are deeply subdivision. Elevations range from 350 to 600 m in the incised resulting in a preponderance of well drained Central Miramichi Highlands but seldom exceed 300 m in conditions. As a result of deep entrenching, the streams are the Southern zone. While both areas are generally well typically rock-walled. Some less elevated broad drained, impeded drainage occurs in some localized valleys depression areas occur to the south and east of this central in the Central Miramichi Highlands and broader core zone. Drainage is provided by the Nepisiguit River to depressional areas in the Southern Miramichi Highlands. the north, the Miramichi River to the east and the Tobique The Central Miramichi Highlands are drained solely by and Serpentine Rivers to the west. The Central and tributaries of the Miramichi River. The Southern Miramichi Southern Miramichi Highlands are progressively lower in Highlands drain into the Saint John Watershed primarily via elevation and less pronounced in topography, grading from the Becaguimec, Keswick and Nashwaak Rivers. The a more hilly aspect in the Central Miramichi Highlands to Miramichi Highlands are underlain by a number of bedrock rolling landscapes in the Southern Miramichi Highland types. The northern portion consists of Ordovician 7

Figure 3. Bedrock geology of the survey area based on Potter et al. (1979). formations of silicic volcanic rocks, rhyolite, rhyolite- The Chaleur Uplands consist of a plateau extending from porphyry, silicic tuffaceous rocks and metamorphosed west of the Restigouche River to a transition zone with the equivalents, quartz, and quartz-feldspar schist with some New Brunswick Highlands that runs from north of Mount mafic volcanic flows in a distinctive circular pattern. South Carleton over to Bathurst. The eastern boundary of the of this are parallel formations of Devonian granites and Chaleur Uplands (Fig. 3) is a modification of Bostock’s granodiorites, Ordovician argillaceous sedimentary rocks, (1970) physiographic divisions as suggested by Rampton et greywacke, quartz, conglomerate and minor limestone, tuff al. (1984) to better align physiographic units with major and volcanic flows, and Silurian greywacke, slate, siltstone, structural elements of the region. The Uplands tend to be sandstone, conglomerate and limestone. Minor areas of lower in elevation and less rugged than their adjacent Mississippian and/or Pennsylvanian red to grey counterparts, the New Brunswick Highlands on the east and conglomerate and siltstone are also present. Notre Dame Mountains on the west. Excluding the narrow Chaleur Coastal Plain and the localized Campbellton Hills, 8 the Chaleur Uplands portion of the study area is dominated 1966). The prevailing westerly winds in Maritime Canada by two subdivisions, the Saint Quentin Plateau and the blow offshore, resulting in a more extreme climate similar to Jacquet Plateau. The Jacquet Plateau is east of the inland Canada (Dzikowski et al. 1984). In general, weather Upsalquitch River. It consists of a north-sloping plateau changes are numerous with the passage of low pressure air ranging in elevation from 450 m along its southern border masses from interior North America. Summers are cool, with the Highlands to less than 100 m as it approaches winters are cold and snowy, and springs are short and late. Chaleur Bay. A series of northeast running ridges occur Near the coast, the ocean moderates the continental south of Dalhousie. Drainage is via the deeply incised influence. Coastal areas tend to have long but cool growing Upsalquitch, Jacquet and Tetagouche Rivers in a northerly seasons, while sheltered inland valleys have shorter but or northeasterly direction. These rivers are all steep-sided, warmer growing seasons. Advantages of a prolonged rock-walled, V-shaped drainage channels in their upper growing season along the coast are offset by cooler reaches. Bedrock geology consists of Silurian and Devonian temperatures. However, the waters of the Gulf of Saint greywacke, slate, shale, sandstone, limestone and Lawrence are warmer in the summer and colder (frozen) in conglomerate with minor volcanic rocks of rhyolite, trachyte the winter than the Atlantic Ocean, resulting in less of a and basaltic flows. The Saint Quentin Plateau falls mostly moderating effect. between the deeply incised Restigouche and Upsalquitch Rivers. Elevations are in the 300 to 425 m range. Relief Annual daily mean air temperature ranges from 2.0 to 5.2oC. averages less than 100 m and is considerably less Winter temperature extremes in January can drop down to pronounced than in the Highlands. Although drainage is for below -40oC in the highlands and uplands. Annual the most part moderate, the gently rolling to undulating precipitation ranges from 1000 to over 1200 mm per year, nature of the landscapes lead to some low lying, flat areas of which 280 to 380 cm are snowfall. Snow cover helps to being poorly drained. The Campbellton Hills are a localized minimize the impact of low winter temperatures on ground series of ridges and hills running parallel to the Restigouche vegetation. Although slightly heavier in late fall and early River from west of Dalhousie to the Upsalquith River. winter, precipitation is distributed fairly evenly throughout Elevations are usually in excess of 300 m with relief varying the year, providing adequate moisture (375 to more than 500 from 50 to 150 m, resulting in typically well drained mm) during the growing season of May to September. conditions. Underlying bedrock is a mixture of greywacke, Occasional dry periods do occur. Excess moisture resulting slate, sandstone and conglomerate, with some limestone and from snowmelt is common in spring. volcanic rocks. The Chaleur Coastal Plain is a narrow (2-10 km wide), low lying (less than 80 m elevation), gently Duration of daylight (sunrise to sunset) ranges from about 9 sloping, imperfectly to moderately well drained, plain hours in December to about 16 hours in June. However, the adjacent to Chaleur Bay underlain by the same bedrock as rather cloudy conditions typical of the area result in con- found in the adjoining Jacquet Plateau.. siderably less sunshine hours--especially along the coast of the Northumberland Strait. The Kedgwick Ridge Highlands subdivision of the Notre Dame Mountains occupies the area west of the Restigouche The average frost free period (days from last spring frost River from the Restigouche County line north and west to until first fall frost) varies greatly depending upon latitude, the Quebec interprovincial border. As the name implies, elevation, topography and distance from the coast. The these highlands or mountains are more rugged and exhibit southern and eastern most areas have the longest frost-free greater relief than found in the Chaleur Uplands to the east. periods with in excess of 130 days (May 23 to September Elevations range from 450 to 600 m with relief of 100 to 30) while in the central and northwestern regions the 250 m. More deeply incised tributaries of the Restigouche average frost-free period is less than 90 days (June 14 to River, including the Kedgwick River, result in narrow September 1). valleys and greater relief along the eastern edge of the area. This area is predominately well drained. The western half Dzikowski et al. (1984) stratified the atmospheric climate of of the subdivision is more rolling with less relief. Here, the study area based on annual growing degree-days (above broad, flatter valleys with poorer drainage separate the well 5oC) and May to September rainfall (Fig. 4). This map drained uplands. The underlying bedrock consists of provides information on the distribution of heat units and Devonian shale, limestones and sandstone, with minor growing season precipitation within the area. In general, greywacke, tuff and volcanic rocks. areas with higher heat units and moderate precipitation are more favourable for agriculture. The Exploratory Soil Survey of Central and Northern New Brunswick has areas CLIMATE falling within climatic zones 2A, 2B, 3A, 3B, 3C, 3D, 4C and 4D. Within these zones, annual degree-days (greater Atmospheric climate than 5oC) vary from 1200 to 1800 and May to September Despite its mid-latitude maritime location, the survey area precipitation from 350 to 550 mm. While other parameters has a modified continental climate (Chapman and Brown can be used to stratify climatic conditions, the map in Fig.4 9

complex and indirect. Soil climate responds to atmospheric climate, but these changes are a function of time and of soil conditions--soil moisture content, depth, surface cover, and site position. Based upon temperature and moisture conditions for biologically significant periods of the year, Clayton et al. (1977) classified the soil climate of the lowlands portion of the surveyed area as Humid Boreal and for the uplands portions, primarily Perhumid Cryoboreal. The Humid Boreal areas are characterized by a mean annual soil temperature, measured at a depth of 50 cm, of 5 to 8°C and mean summer (June, July, and August) soil temperature of 15 to 18°C. In most years, no soils are dry for as long as 90 consecutive days; thus, water deficits are slight during the growing season (2.5 to 6.4 cm). As with atmospheric climate, marine influence results in a modified regime along the coast. The Perhumid Boreal areas are characterized by a mean annual soil temperature of 2 to 8°C and mean summer soil temperature of 8 to 15°C. The soils are moist all year, seldom being dry, with no significant water deficits in the growing season (less than 2.5 cm).

VEGETATION

According to Rowe (1972), central and northern New Figure 4. Climatic zones within the survey area based on Brunswick includes parts of three major forest regions - the Dzikowski et al. (1984). Acadian, Great Lakes-St. Lawrence and Boreal Forest Regions (Fig. 5). However, given that the survey area is on the border of these zones, being at the southwestern extreme provides a good representation of climatic trends and of the Boreal Forest Zone, the eastern extreme of the Great variability within the study area. Within the survey area two Lakes-St. Lawrence Forest Region and the northwestern influences dominate the climate--the moderating effect of extreme of the Acadian Forest Region, the forest stands tend the Atlantic Ocean along the eastern shore and the cooling to be somewhat intra-zonal. effect of increased elevations in central and northwestern New Brunswick. Essentially, annual heat units decrease and Forests of the Notre Dame Mountains in western growing season rainfall increases along two transects going Restigouche County are part of the Gaspe Section of the from south to north and from east to west. The more highly Boreal Forest Region. Although mixed conifer-hardwood elevated areas in the central and northern portions are colder stands occur, the dominant forest cover type is conifers: and receive more May to September precipitation than the balsam fir, black spruce and white spruce, often with eastern coastal and southern regions. The lower temperatures are a white cedar. White birch is a common hardwood function of more northern latitudes, higher elevations and component in these stands. greater distance from the coast. As Dzikowski et al. (1984) explain, lower precipitation along the coast is “caused by the East of this, the Chaleur Uplands fall in the Temiscouata- air descending and warming, thus being able to hold more Restigouche Section of the Great Lakes-St. Lawrence Forest water and producing less precipitation. In effect, the Region. Rowe (1972) describes these forests as topography shelters these areas from storm winds. Air “characterized by sugar maple, beech and yellow birch on masses moving into north eastern coastal New Brunswick the hill tops with balsam fir and white spruce in the valleys. have lost much of their moisture over the central highlands ... Eastern white cedar of good size is common on lower resulting in lower precipitation in these areas.” slopes. On hillsides and low rocky knolls balsam fir forms mixtures with yellow birch, white birch and, formerly at Soil climate least, with the eastern white and red pines. Though much Although implications of the atmospheric climate have been reduced in importance relative to their earlier status, the well documented, knowledge of the interaction between pines are locally abundant, and eastern white pine shows up atmospheric and soil climates is essential for various land prominently in second growth stands which have sprung up uses, in particular, productive plant growth as related to following fire. Alluvial flats support balsam poplar, black subaerial development and for some engineering ash, white elm and white spruce. Other species distributed applications. This relationship, although possible, is often through the Section are red maple, white birch and jack pine, 10

middle slopes include a component of red and white spruce, eastern hemlock and balsam fir; and lower slopes and depressions support primarily coniferous stands of spruces, fir, eastern white cedar and tamarack. Northern reaches of this Section have a more boreal-like coniferous-dominated forest type as found in the adjacent New Brunswick Uplands Section. White birch, red maple and trembling aspen are common successional species after harvesting and/or fire. Grey birch, eastern white pine, red pine, jack pine, red maple and black ash are restricted to local occurrences. A small area of Carleton Section forest types occur along the southwestern edge of the survey area. Hardwood stands of sugar maple, beech, yellow birch, red maple and white ash predominate but yellow birch, balsam fir, eastern hemlock and eastern white pine occur in the mixed wood transitional forests that grade into the higher altitudes of the Upper Miramichi-Tobique Section to the east. Poorly drained areas support stands that include eastern white cedar, black ash, red maple and white elm along with black spruce, balsam fir and some eastern hemlock. Small areas of the “Southern” Uplands Section occur just north of Fredericton and along the eastern side of the New Brunswick Highlands. Tolerant hardwoods - sugar maple, beech and yellow birch - occupy crests and upper slopes while red maple, white birch, balsam fir, red spruce, eastern white pine and eastern Figure 5. Forest regions and sections within the survey area hemlock dominate lower slopes. Black spruce, tamarack, based on Rowe (1972). eastern white cedar and red maple populate poorly drained areas. the latter species forming locally important pulpwood On the Maritime Plain, impeded drainage has lead to a stands. Both white birch and aspen regeneration are prolific prevalence of pure stands of black spruce, red spruce, and following fire. Black spruce and tamarack are found on balsam fir or mixed wood in which these species are bottomlands and in boggy areas.” associated with eastern white pine, red maple, trembling aspen, sugar maple, yellow birch, and white birch. Forest The New Brunswick Highlands and Maritime Plain portions conditions and species distribution largely reflect the effect of the study area are part of the Acadian Forest Region. of: a high level of annual burn; extensive logging activities; More specifically, Rowe (1972) has subdivided the New and repeated infestations of spruce budworm. As a result, Brunswick Highlands area into the New Brunswick Uplands, correlation of vegetation with soils and landform is poor. Upper Miramichi-Tobique, Carleton and “Southern” Balsam fir has been infested and defoliated by spruce bud- Uplands Sections. The Maritime Plain area falls within the worm to the point that mature stands are relatively sparse, Eastern Lowlands Section. High altitudes result in the New but regeneration of balsam fir is quite common throughout. Brunswick Uplands Section being dominated by coniferous Pure stands of American beech, with some sugar maple and forests, with a noticeable boreal similarity. Balsam fir, black yellow birch and a scattering of spruce and fir, are common spruce, white spruce and white birch dominate. White pine, on exposed ridges. On extensive flat-lying poorly drained eastern hemlock and red spruce occur sporadically. Coarser areas, swamps and peat bogs of sphagnum moss-ericaceous textured soils and frequent forest fires has increased the shrub complexes are interspersed with stands of black presence of trembling aspen, jack pine, white birch, eastern spruce and tamarack, and some eastern white cedar. white pine and red pine. Tolerant hardwoods are scarce. Eastern hemlock, once well represented, is now limited in The Upper Miramichi-Tobique Section has a more extent, as the result of repeated cuttings and fires. Exposure pronounced hardwood component. Crests and upper slopes to wind reduces tree stature along the coast. are forested with sugar maple, yellow birch and beech; 11

PART 2. SOIL FORMATION AND CLASSIFICATION

SURFICIAL GEOLOGY differentiate from glacial tills. Only those areas dominated by parent materials of a residual nature were included and Excluding the continuous processes of weathering, the mapped in this category. Most exposed bedrock surfaces surficial geology of the survey area has developed primarily have some weathering, but this is usually limited to the as a result of four primary phenomena: glaciation, submer- upper 0.5 m of rock (Rampton et al. 1984). However, gence, alluviation, and paludification (Rampton et al. 1984). deeper bedrock weathering is associated with some areas of Of these, the effects of glaciation are predominant, with oth- sandstone bedrock in the Maritime Plain and granitic er processes acting as modifiers While glacial and post- bedrock in the New Brunswick Highlands. These areas of glacial events over the more recent 600,000 years have lead more deeply weathered bedrock are thought to be preglacial to only minor modifications of pre-glacial landscapes, they in origin (Chalmers 1888, Wang et al. 1981). While the have had major impacts on soil parent material composition sandstone bedrock may be weathered to a depth of up to 2 and distribution. During one stage of the Pleistocene epoch, m in some localized areas of the Maritime Plain, it is Wisconsinan ice covered the entire province of New generally overlain by other soil forming parent materials and Brunswick. All preglacial surfaces were scoured and subse- mapped accordingly. More deeply weathered granites are quently covered by a mantle of glacial drift of varying scattered throughout the New Brunswick Highlands. These thickness. With deglaciation, which is thought to have deposits are extensive enough to have been mapped as a occurred about 10,000 to 12,000 BP (before present), the unique soil association They also occur as undesignated low-lying Maritime Plain was subjected to a period of components of related till soils. Rotting of granitic bedrock shallow marine submergence. Maximum marine has produced ellipsoidal-shaped tors or core stones on some submergence is thought to have been about 120 m above sea of the higher mountain peaks. A mantle of grus, consisting level (asl). Postglacial submergence was followed by a of coarse-grained fragments resulting from the disintegration period of emergence, during which the relative levels of the of the granite, occurs over most such areas. In general, soils land and ocean attained present day status. This emergence mapped as residual consist of a complex mixture of was at least partially completed by 8000 BP. The most disintegrated bedrock, colluvium (materials deposited by active post-submergence processes of material deposition mass-wasting, usually at the base of a steep slope) and some are those of alluviation (materials deposited by present glacial till material. rivers and streams) and paludification (the development of organic deposits or peatlands), which continue at present. Glacial Till - Morainal till of varying thickness was deposited as either ablation till or lodgment (basal) till as a result of glacial activity during the last ice age. The glacial SOIL PARENT MATERIALS debris was typically deposited as a morainal blanket of 1 to 2 m in thickness but with some veneer depositions (less than Based on their parent materials, soils are divided into two 1 m) and some areas of greater accumulation (greater than categories or groups: mineral soils and organic soils. 2 m). As Rampton et al. (1984) state “even though they Mineral soils consist predominantly of mineral matter, or consist dominantly of till, in many places they comprise a natural inorganic compounds as found in sands, silts, clays complex of ablation till, lodgment till, glaciofluvial deposits, and rock fragments of gravels, cobbles, stones and boulders. glaciolacustrine deposits, colluvium, and weathered Essentially they have formed in unconsolidated bedrock bedrock.” material that, in the case of central and northern New Brunswick, has usually been displaced, as previously Lodgment tills are dense and compact due to the pressure mentioned. Organic soils consist of peat deposits that applied by the weight of the glacial ice that plastered them contain more than 30% organic matter and are typically in place and subsequently overrode them as the glaciers greater than 40 cm thick, but often exceed 2 m in total advanced. Ablation till is that material carried on top of or accumulation. within the glacier and is generally stonier and usually not compacted. It is released from the glacier in the ablation zone, the area where melting occurs at a greater rate than Mineral Soils accumulation. As the ice melts, material is released from the glacier where it may accumulate to a thickness of many Residual - Soils formed from, or resting on, consolidated metres, creating an ablation moraine. In general, true rock of the same kind as that from which it was formed and ablation tills tend to be thicker than lodgment tills. Ablation in the same location are called residual soils. The materials till generally exceeds 5 m in thickness (Rampton et al. consist of unconsolidated or partly weathered bedrock that 1984), however, areas of negligible coverage are also has developed as a result of in situ physical, chemical and common. Thin ablation deposits are considered to be the biological activities. Due to a similarity in appearance and result of rapid retreat of the glacial ice, not allowing for any composition, residual materials are often difficult to significant accumulation of ablation debris. Most lodgment 12 tills have some capping of ablation material, albeit very thin. depending upon the amount of water working to which they Slowly retreating or stationary debris-rich ice sheets resulted have been subjected. Their particle size ranges from in thicker ribbed, hummocky and rolling ablational till coarse-loamy to sandy-skeletal. Although many deposits. glaciofluvial deposits occur along present-day drainage channels, other, such as eskers, which have formed in Differentiation of ablational from lodgment till materials is tunnels and channels within the glacier ice, are notorious for almost impossible where the ablational capping over traversing landscapes with little regard to existing lodgment till is thin and soil formation has obliterated the topography. Because of water working actions, glaciofluvial interface. Identification is made more difficult where the coarse fragments are strongly rounded. The coarse-textured, ablation and lodgment tills are alike in texture and colour. highly permeable nature of glaciofluvial sediments means Similar difficulties in identification occur where tills are that most soils developed on these materials are well shallow and soil forming processes have been active drained, unless drainage is impeded topographically. throughout the deposit thickness. Even in lodgment tills, Gravelly, cobbly and bouldery alluvial materials are found soil forming processes loosen the upper 50 cm of material. in up-stream locations. Finer-textured alluvial sediments Some materials deposited as ablation debris now have consisting of fine sands, silts and clays and organic materials relatively compact subsoils, a development that Rampton et form terraces and floodplains along lower stretches of al. (1984) attribute to postglacial processes. Representative streams and rivers. Alluvium is commonly underlain by ablational tills that are considered to be “noncompact” still glaciofluvial sediments. have subsoils which are denser than the surface soil due to the weight of overlying materials. No attempts were made Marine - Post glacial marine submergence resulted in sands to differentiate compact ablational till from compact of varying thicknesses being deposited on the tills and a lodgment till. Soil materials with similar physical and general reworking of surficial materials in the Maritime chemical properties were grouped together, regardless of Plain portion of the study area. These sandy deposits range original mode of deposition. up to several metres in thickness, but also commonly occur as thin veneers over either glacial tills or bedrock. Thick In areas of high bedrock relief, glacial erosion has resulted deposits of reworked marine, or possibly lacustrine clays, in most lodgment till deposits being relatively thin veneers. are also found well above present day sea levels. Since Texture, colour and coarse fragment lithology of lodgment many of these deposits contain remnants of glacial materials, tills closely resemble the underlying bedrock, or at least the they more aptly may be considered as “glacial marine”. A bedrock that is in an up-flow glacial direction, usually report by the Maritime Resource Management Service northwest. Ablation tills may have a more wide-ranging (1978) describes the depositional environment for materials lithological composition and weaker ties to the underlying on the Chaleur Coastal Plain as follows: “Marine deposits bedrock type. Excluding the northern half of the Acadian are associated with the invasion and recession of marine Peninsula where reddish brown tills are common, most tills waters on and from the land. During deglaciation, the are yellowish to olive brown or grey. earth’s crust was still depressed from the weight of the glacial ice sheet and the sea was able to encroach upon the Meltwaters from the glacier have often reworked the surface land surface. The marine submergence extended inland to of the till to give it a glaciofluvial appearance. This may 78 metres above the present sea level in the Jacquet River happen to such an extent that it is very difficult to area... The uplift was very gradual, thereby creating a differentiate between a highly reworked ablation till and a suitable depositional environment for extensive marine glaciofluvial deposit. sediments along the coast.... Much of the study area along the coast north of Peter’s River consists of a complex of For the purpose of mapping, tills with compact subsoils were raised beach ridges, strand lines and logoonal sediments. considered to be lodgment tills and tills with non-compact Each beach system represents a shoreline which has been subsoils were considered to be ablation tills. Lodgment and washed by the waves or tides of a sea undergoing a eustatic ablation tills were further categorized on the basis of soil decline in sea level relative to the uplifting land mass. The parent material particle size class, reaction, colour and material associated with these deposits is a well-graded, lithology. gravelly loam exhibiting continuous stratification, which indicates extensive washing and sorting.” Fluvial - All sediments, past and present, deposited by flowing water, are fluvial. This includes glaciofluvial Organic Soils materials that were moved by glaciers and subsequently sorted and deposited by streams flowing within and from the Three types of organic deposits have been identified and melting ice, forming outwash plains, deltas, kames, eskers, mapped. and kame terraces. Alluvial materials deposited by modern rivers and streams are also included in the “fluvial” Bog - Bogs consist of sphagnum and to a lesser extent forest designation. Glaciofluvial deposits are usually stratified peat materials. They have formed in an ombrotrophic sands and gravels and exhibit some degree of sorting, (nutrient poor) environment due to the slightly elevated 13 nature of the accumulation. This tends to disassociate them Different environmental conditions result in dissimilar soil from the nutrient-rich ground water of surrounding mineral formation. The differences in the types of soil formed is soils. These organic materials are extremely acid (pH less dependant upon the magnitude of variation in the soil than 4.5) and weakly to moderately decomposed (fibric to forming factor(s) involved. mesic). Bogs are associated with depressions where the water table is at or near the surface for the entire year. Most Climate is perhaps the most influential factor in determining deposits are virtually treeless, with the exception of some the degree of weathering and thus the degree of soil severely stunted conifers around the periphery. They are formation that occurs. The rate of chemical reaction doubles characterized by a ground vegetation cover of sphagnum for every 10oC rise in temperature (Brady, 1974). Soil mosses and ericaceous shrubs. Bog units mapped in this temperature is highly dependant upon soil moisture. survey are typically domed bogs on the Maritime Plain. Biochemical reactions and changes are sensitive to both soil temperature and moisture. Within the study area, annual Fen - Fens consist of peat materials derived primarily from precipitation (rain plus snow-water equivalent) averages sedges formed in a eutrophic (nutrient rich) environment. 1000 to 1200 mm. Under these levels of precipitation, soil This is due to the close association of the material with materials that have good drainage are readily leached of mineral-rich waters. Fen materials are medium acid to soluble and mobile materials which are either translocated neutral (pH 5.5 to 7.5) and moderately to strongly and redeposited within the profile, or lost entirely from the decomposed (mesic to humic). They are associated with a soil body. Podzolization, or the downward movement of Fe nutrient-rich watertable that persists seasonally at or very and Al and organic matter, is an end result. Annual air near the surface. Most deposits have a low to medium temperatures vary from a high of 5.2oC in the lowlands to a height shrub cover and sometimes a sparse layer of trees. low of 2.0oC in the central portion of the N. B. highlands. Stream fens are the most common type of fen found in the Lower temperatures result in reduced rates of chemical survey area. Most mapped fens have a surficial capping of reactions. Evapotranspiration is also lower and thus there is acidic sphagnum peat and are in a stage of transition towards higher "effective" precipitation, ie., more of the rainfall a bog environment. moves through the soil profile because less water is lost by evaporation from the soil or via the plant (transpiration). Swamp - These units are dominated by peat materials that Variations in soil solum development result. This usually consist of moderately to strongly decomposed (mesic to takes the form of increased accumulation of organic matter humic) forest peat. They have formed in a eutrophic in the upper B horizon. The climatic influence is also environment resulting from strong water movement from the indirectly expressed in its control over natural flora and margins with surrounding mineral soils. Forest peat fauna (organisms), which are in themselves contributing soil materials are medium acid to neutral (pH 5.5 to 7.5). They forming factors. Meso, or local, climate influences the way are associated with stream courses and depressions where soils develop, both directly as a result of temperature standing to gently flowing waters occur seasonally or persist variations and secondarily through type of vegetation. Local for long periods on the surface. The vegetative cover topography, steepness of the slope, aspect, exposure, usually consists of a thick forest growth of coniferous and position on slope and type of vegetation all modify deciduous trees. Swamps were mapped in the highland and mesoclimatic conditions (van Groenewoud, 1983) and thus upland areas of the survey area. impact on soil formation.

Living organisms play a significant role in soil profile SOIL DEVELOPMENT AND SOIL FORMING development. Natural vegetation in particular is a critical FACTORS factor in determining soil characteristics. Different types of organic debris (leaves, stems, branches, etc.) can vary Soil genesis or formation involves all the processes that are considerably in mineral element content. The litter from responsible for the development of soil. Although the deciduous trees is comparatively much higher in bases such individual processes are numerous, studies have shown that as calcium and potassium than is litter from coniferous trees. the kind of soil that develops is largely controlled by five The higher base status in deciduous litter usually results in major factors: climate (particularly temperature and a greater rate of decomposition in the forest duff layer. In precipitation); parent material (mode of deposition, texture, contrast to this, the organic acids from coniferous forest and mineralogical composition); topography or relief (in litter strongly leaches the upper mineral soil layers. relation to soil drainage and rates of soil erosion); living Windthrows, or the uprooting of trees, mixes the soil. organisms (especially natural vegetation, but also animal Although animal biomass in natural soil ecosystems is life); and time (the period over which the soil parent typically less than 1% of plant biomass (Buol et al, 1973), material has been subjected to soil formation). These animals create and foster change in soil conditions. In the factors were described in the preceding text under Part 1. adjoining counties of Carleton, Victoria and Madawaska, General Description of the Area. which are to the immediate west of the study area, Langmaid (1964) found alteration in surface horizonation of virgin Soils are very much products of their environments. forest soil profiles as a result of earthworm invasion. 14

Micro-organisms are involved in biochemical reactions. Topography also modifies the climatic influence and is a Even man plays a role in his use of the land. Conversion of determining factor in native vegetation cover type. forested land to farmland is a most dramatic change. The period or time that any given material is subjected to the Parent material has been recognized as a significant soil processes of weathering is another factor in soil formation forming factor since the inception of pedology. Many soil that cannot be over emphasized. Soils are routinely properties are inherited from the initial parent material. subjected to new cycles of soil development over both the Since most of our soils are relatively young in age, short term (ie. vegetative cover changes, erosion, etc.) and geologically speaking, weathering and soil formation have the long term (ie. land uplifting, world climatic changes, not drastically obliterated the inherited properties of the etc.). However, from a comparative point of view, time zero initial parent material. Different modes of deposition yield can be established at that point following the last major soil parent materials with different compositions and catastrophic event (Boul et al. 1973). In the Atlantic properties. Basal or lodgment tills that are so prevalent Region, glaciation was the last major catastrophic event. throughout the study area tend to yield compact, finer While some remnants of weathered bedrock in central New textured deposits than ablational tills. Glaciofluvial Brunswick are considered to be in excess of 1 to 1.5 million sediments are usually readily previous, sandy or sandy years old, for the most part, glacial sediments have only skeletal materials. The lithlogy of the bedrock materials been exposed to weathering for some 10,000 to 12,000 from which the regolith has been derived determines the years. Postglacial marine submergence in the lowland mineralogy of the soil. The potential fertility supplying portion of the area has resulted in slightly shorter periods of power of a particular rock type depends upon both its exposure, 8,000 to 10,000 years. Alluvial floodplain inherent nutrient content and its weatherability, or the rate at sedimentation is an ongoing process, as is paludification which nutrients can be released (Colpitts et al. 1995). Of all (organic soil accumulation). Materials are constantly being the mineral components the clay fraction is the most added to the surface of these deposits and soil development important because it is the most active in terms of physical, reflects these conditions. chemical and biological processes. Most of the clays in our soils are inherited from the soil parent material. Little From the foregoing discussion it is easy to see that the soil formation or alteration of clay minerals has taken place in forming factors are interdependent and interactive. They are the period since glaciation. Illite dominates, but most soils simultaneously at work, altering and continuously modifying have significant amounts of chlorite and small amounts of the soil profile. kaolinite and vermiculite-montmorillonite (Clayton et al. 1977). Where the initial parent material contained large amounts of free carbonates, the normal acid leaching process SOIL PROFILE is retarded until the free carbonates are leached from the soil. During this time, clay moves from the upper part of the The soil profile is a vertical cross section of the soil through profile and is redeposited in the B horizon. When leaching all its horizons and extending into the parent material. A has gone beyond this stage and the upper part of the profile soil horizon is a layer of soil approximately parallel to the is sufficiently acid, podzolization takes place. land surface that differs from adjacent genetically related layers in properties such as colour, structure, consistence, Topography or relief has been related to the following soil texture or chemical, biological and mineralogical properties (Buol et al, 1973): (1) depth of the solum; (2) composition. thickness and organic matter content of the A horizon; (3) relative wetness of the profile; (4) degree of horizon Organic layers are differentiated from mineral horizons and differentiation; (5) soil reaction; (6) temperature; and (7) layers on the basis of organic carbon. (Organic matter character of the initial (parent) material. To a large degree content is about 1.7 times the organic carbon content.) these effects are moisture related. The rugged topography Organic layers contain 17% or more organic carbon. Two of central and northwestern New Brunswick is conducive to groups of organic layers are recognized. O, organic layers more extensive areas of better drainage than in the flatter have developed mainly from mosses, rushes, and woody Maritime Plain region of northeastern New Brunswick, materials; and L-F-H, organic layers have developed where excess water tends to remain in the landscape for a primarily from leaves, twigs, and woody materials with only longer period of time. Soil profiles develop accordingly. a minor component of mosses. Organic horizons are found Locally, drainage variation across toposequences has in Organic soils and commonly at the surface of mineral significant impact on the degree and nature of soil soils. formation. Poorly drained soils have less distinct and duller coloured horizons than well-drained soils. Material types Mineral horizons and layers contain less than 17% organic are associated with different positions in the landscape. carbon. The master mineral soil horizons, from the mineral Depressional areas that are saturated with water for a large soil surface downward, are designated by the letters A, B, part of the year encourage the accumulation of organic soils; and C. The A and B horizons represent the upper and most alluvial soils occupy along flood plains; and so on. weathered part of the soil profile. Collectively, they are 15 referred to as the solum. The A horizon is formed at or near SYSTEM OF SOIL CLASSIFICATION the surface in the zone of removal of materials in solution and suspension, or maximum in situ accumulation of organic The soils are classified in accordance with criteria carbon. The B horizon is immediately below the A horizon. established by the Canadian System of Soil Classification It is usually characterized by either an enrichment in (Soil Classification Working Group 1998). Soil materials leached from the A horizon (ie. clay, iron, classification is based on a vertical section of the soil profile aluminum or organic matter) or some other form of referred to as the control section. The control section is alteration in colour and/or structure. The underlying C typically 1 m for mineral soils and 1.6 m for organic soils. horizon is the relatively unweathered parent material from The Canadian system is a hierarchical organization of which the soil has developed. It is comparatively unaffected categories that permit the consideration of soils at various by the pedogenic (soil-forming) processes operative in the levels of generality. The taxa are based upon soil properties A and B horizons. Lowercase suffixes are appended to the that can be observed and measured objectively in the field, master horizon designation to indicate the type of horizon. or, if necessary, in the laboratory. The system has a genetic Arabic numerals are used when further subdivision is bias in that soil properties that reflect genesis are favoured required. Roman numerals are prefixed to horizon and layer as differentiae in the higher categories. There are five designations to indicate parent material discontinuities in the different levels: profile. Bedrock (greater than 3 on Mohs' scale of hardness) is designated as R. Order. Taxa at the order level are based on properties of the pedon that reflect the nature of the soil environment and the Imperfectly drained mineral soils have the same type and effects of the dominant soil-forming processes. arrangement of horizons as their well-drained counterparts, but because they are periodically saturated, a condition Great group. Great groups are soil taxa formed by the called "mottling" develops. Mottling, or the occurrence of subdivision of each order. Thus each great group carries spots of different colours or shades interspersed within a with it the differentiating criteria of the order to which it matrix colour, is indicative of zones of alternating good belongs. In addition, taxa at the great group level are based (oxidized) and poor (reduced) aeration. In well drained sites on properties that reflect differences in the strengths of the soils are well oxidized and red, yellow and reddish dominant processes or a major contribution of a process in brown colours develop. Where oxygen is lacking, reduction addition to the dominant one. For example, in Luvic results in grays and blues. Poorly and very poorly drained Gleysols the dominant process is considered to be gleying, soils are waterlogged for a large part of the year, and so, but clay translocation is also a major process. because of the resulting reduced grayish-blue colours, are said to be "gleyed". Excessive moisture tends to retard Subgroup. Subgroups are formed by subdivisions of each profile development and expression. Horizonation is not great group. Therefore they carry the differentiating criteria nearly as evident as in well drained soils. of the order and the great group to which they belong. Subgroups are differentiated on the basis of the kind and A complete listing of all horizon nomenclature used in this arrangement of horizons that indicate: conformity to the report is provided in the Canadian System of Soil central concept of the great group, i.e. Orthic; intergrading Classification (Soil Classification Working Group 1998). toward soils of another order, e.g. Gleyed or Brunisolic; or additional special features within the control section, e.g. A profile that is under native vegetation and unmodified by Ortstein. man is considered a “virgin” profile. In a virgin profile the effects of soil formation are left relatively undisturbed or as Family. Taxa at the family level are formed by subdividing is. Most forest soils are considered as virgin sites, subgroups. Thus they carry the differentiating criteria of the regardless of whether or not they have been logged in the order, great group, and subgroup to which they belong. past. Under these conditions the naturally occurring Families within a subgroup are differentiated on the basis of sequences of soil horizons and layers are readily expressed parent material characteristics such as texture and and recognized. The exception to this is where road mineralogy, and soil climatic factors and soil reaction. construction and other soil displacing activities have taken place. In contrast to forest soil profiles, agricultural soils Series. Series are formed by subdivisions of families. show drastic variation in the surface layers as a result of Therefore they carry all the differentiating criteria of the cultivation. The organic surface layer, A horizon and upper order, great group, subgroup, and family to which they B horizon are mixed together into a relatively homogeneous belong. Series within a family are differentiated on the basis plow layer, which is designated as the Ap horizon. Man's of detailed features of the pedon. Pedons belonging to a activities not only alter the soil's physical and chemical series have similar kinds and arrangements of horizons composition, but also modify the soil forming factors whose colour, texture, structure, consistence, thickness, themselves and thus impact on future soil development. reaction, and composition fall within a narrow range. 16

SOIL ORDERS IN CENTRAL AND NORTHERN NEW soil solution ceases to move or movement becomes very BRUNSWICK slow. In the central and northern New Brunswick area, Luvisolic soil development is for the most part weakly Brunisolic Soils expressed. The typical Luvisolic characteristics of a Most Brunisolic soils are well to imperfectly drained and moderate to strong prismatic or blockly structured Bt have developed on either coarse textured glaciofluvial horizon and solum of high base saturation are not present. deposits, or medium textured old (ancient) alluvial Within the study area Luvisolic soil development is most sediments. They have sufficient profile development pronounced in materials of neutral reaction, ie. the Caribou, to exclude them from the Regosolic order, but lack the Carleton and Tracadie associations. Due to climatic degree or kind of horizonation specified for other orders. conditions, only members of the Gray Luvisolic great group Within the mapping area of central and northern New are found. The subgroups occurring within the study area Brunswick, most Brunisols can be considered to be weakly are: Orthic Gray Luvisols, Gleyed Gray Luvisols, developed Podzols. They tend to have a brownish-coloured Brunisolic Gray Luvisols, Gleyed Brunisolic Gray Luvisols, Bm horizon which has an accumulation of illuvial Al and Fe Podzolic Gray Luvisols (Fig. 6c), and Gleyed Podzolic compounds and organic matter under a whitish-gray eluvial Gray Luvisols. The Podzolic Gray Luvisols are Ae horizon. Significant areas of Dystric Brunisols occur "transitional" in that they have bisequal profile development under virgin conditions. Materials are acidic and lack any with a podzolic B horizon formed over the luvisolic Bt well developed mineral-organic surface horizon. Eluviated horizon. The Brunisolic Gray Luvisols and Gleyed Dystric Brunisol and Gleyed Eluviated Dystric Brunisol Brunisolic Gray Luvisols can be considered to be "juvenile" (Fig. 6a) subgroups are present. Some of the Gleyed counterparts of the Podzolic Gray Luvisols and Gleyed Eluviated Dystric Brunisols are poorly drained coarse Podzolic Gray Luvisols. textured glaciofluvial, marine or morainal till sediments. They have evidence of gleying but it is too weakly expressed Organic Soils to meet the specifications of Gleysolic soils. Organic soils are composed largely of organic materials, including soils commonly known as peats, mucks, bogs and Gleysolic Soils swamps. They occur in poorly and very poorly drained Soils of the Gleysolic order have features indicative of depressions and level areas saturated with water for periodic or prolonged saturation with water and reducing prolonged periods, and are derived from hydrophytic conditions. They are associated with either a high ground- vegetation (mosses, sedges, shrubs, etc.) that grow in such water table at some period of the year or temporary sites. Organic soils have at least 40 cm of organic material, saturation above a relatively impermeable layer. Gleysols with some having in excess of 5 m. Organic soils found in occupy poorly drained landscape positions, lower slopes, the study area fall into the Fibrisol, Mesisol and Humisol toes and depressions in rolling and hilly topography, and great groups. These subdivisions are based upon the degree depression to mid-slope and sometimes even upper slope of decomposition of the organic material. The following sites in level to gently undulating topography. Soil horizons subgroups occur: Typic Fibrisols (Fig. 6d), Mesic are subdued in appearance and may be difficult to Fibrisols, Terric Fibrisols, Humic Mesisols, Terric Mesisols, differentiate due to the gleyed and/or mottled conditions Terric Fibric Mesisols, Terric Humic Mesisols, Mesic throughout the profile. Hydrophytic vegetation and surface Humisols, Terric Humisols and Terric Mesic Humisols. peaty layers are commonly associated features, although not diagnostic. Gleysol, Humic Gleysol and Luvic Gleysol great Podzolic Soils groups occur. They are separated on the basis of the In central and northern New Brunswick most of the well to presence or absence of an Ah or Bt horizon. The following imperfectly drained mineral soils are members of the subgroup members were identified as occurring within the Podzolic order. See Table 1. This includes soils developed study area: Orthic Gleysols (Fig. 6b), Rego Gleysols, Fera in morainal till, marine, residual, glaciofluvial and ancient Gleysols, Orthic Humic Gleysols, Rego Humic Gleysols, alluvial parent materials. Podzolization is the dominant type Orthic Luvic Gleysols, Humic Luvic Gleysols and Fera of soil formation in the region. The prevailing cool to cold, Luvic Gleysols. With exception of organic soils, Gleysols humid to perhumid climatic conditions coupled with the have developed in every soil parent material type and almost influence of forest/heath vegetation, is conducive to all mapped soil associations. podzolic soil development. These soils are characterized by the following horizon sequence: The surface L, F and H, or Luvisolic Soils possibly Of or Om horizon, is underlain by a thin Well to imperfectly drained members of several soil discontinuous dark coloured Ah horizon and then by a light associations are classified as Luvisols. They have ashy coloured eluvial Ae horizon. The Ae horizon breaks developed in fine loamy morainal tills and clayey marine abruptly into a reddish brown to almost black B horizon that sediments. Luvisols are characterized by the presence of an grades into a slightly modified BC horizon and then into the illuvial Bt horizon in which silicate clay has accumulated. parent material “C”). The podzolic B contains illuvial Fe, Al Clay suspended in the soil solution is moved downward in and organic matter. It is the diagnostic horizon in terms of the soil profile from the surface layers to a depth were the morphological and chemical requirements. These and other 17

(a) (b) (c)

(d)

(e) (f)

Figure 6. Diagrammatic horizon patterns of various soil profiles.

technical criteria are detailed in the Canadian System of Soil subgroups occur: Orthic Humo-Ferric Podzols (Fig. 6e), Classification (Soil Classification Working Group 1998). Gleyed Humo-Ferric Podzols, Fragic Humo-Ferric Podzols, The Podzolic order is divided into great groups on the basis Luvisolic Humo-Ferric Podzols, Orthic Ferro-Humic of organic carbon content and related properties. Both Podzols and Gleyed Ferro-Humic Podzols. Some poorly Humo-Ferric and Ferro-Humic Podzols are present. Six drained soils have gley features but also a podzolic B 18

Table 1. Soil association members of the central and northern New Brunswick map area classified according to the Canadian System of Soil Classification (1998)

CSSC Subgroup(s) Mode of Rapidly to Mod. Well Imperfect Poor to Very Poor Soil Association Deposition Drained Drained Drained

Acadie Siding Paludification ------T.M, TFI.M, THU.M (T.H, T.F)

Barrieau-Buctouche Marine over O.HFP GL.HFP, GLE.DYB O.G, FE.G morainal till

Belldune River Marine O.HFP GL.HFP O.G, FE.G

Big Bald Mountain Residual O.HFP GL.HFP ----

Boston Brook Morainal till O.HFP GL.HFP O.G

Caribou Morainal till PZ.GL, LU.HFP GLPZ.GL, GLBR.GL O.LG, O.HG

Carleton Morainal till PZ.GL, LU.HFP (O.HFP) GLPZ.GL, GL.HFP O.LG, O.G

Catamaran Morainal till O.HFP GL.HFP O.G, FE.G

Gagetown Glaciofluvial O.HFP, E.DYB GL.HFP, GLE.DYB GL.HFP, GLE.DYB, O.G

Grand Falls Glaciofluvial O.HFP GL.HFP GL.HFP, GLE.DYB, O.G, R.G

Guimond River Glaciofluvial O.HFP, E.DYB GL.HFP, GLE.DYB GL.HFP, GLE.DYB, O.G

Holmesville Morainal till O.HFP GL.HFP O.G, FE.G

Interval Alluvium O.R, CU.R GL.R, GLCU.R R.G, R.HG

Jacquet River Morainal till O.FHP, O.HFP GL.HFP O.G, FE.G

Juniper Morainal till O.HFP GL.HFP O.G, FE.G, O.HG

Lavillette Paludification ------TY.F, ME.F

Long Lake Morainal till O.FHP, O.HFP GL.HFP O.G

Maliseet Alluvium (ancient) O.HFP GL.HFP, GLE.DYB GLE.DYB, O.G, R.HG

McGee Morainal till O.FHP, O.HFP GL.HFP O.G, R.G

Muniac Glaciofluvial O.HFP GL.HFP GL.HFP, GLE.DYB, O.G, R.HG

Nigadoo River Morainal till O.FHP, O.HFP GL.HFP O.G, FE.G

Parleeville Morainal till O.HFP GL.HFP GLE.DYB, O.G

Popple Depot Morainal till O.FHP, O.HFP GL.HFP O.G, FE.G

Reece Morainal till O.HFP, FR.HFP GL.HFP FE.G

Richibucto Marine O.HFP, E.DYB GL.HFP, GLE.DYB GLE.DYB, O.G

Riverbank Glaciofluvial or O.HFP GL.HFP GLE.DYB, O.G, FE.G Alluvial (ancient) 19

Table 1. Soil association members of the central and northern New Brunswick map area classified according to the Canadian System of Soil Classification (1998) cont’d

CSSC Subgroup(s) Mode of Rapidly to Mod. Well Imperfect Poor to Very Poor Soil Association Deposition Drained Drained Drained

Rogersville Morainal till O.HFP, FR.HFP, PZ.GL GL.HFP, GLPZ.GL O.LG, FR.LG

St. Quentin Paludification ------T.M, THU.M, T.H, TME.H (ME.H, HU.M)

Stony Brook Morainal till PZ.GL, LU.HFP GLPZ.GL, LU.HFP O.LG, FE.LG

Sunbury Morainal till O.HFP GL.HFP GL.HFP, GLE.DYB, O.G

Tetagouche Morainal till O.HFP, O.FHP GL.HFP O.G, FE.G

Tetagouche Falls Morainal till O.HFP, O.FHP GL.HFP O.G, FE.G

Thibault Morainal till O.HFP GL.HFP O.G, FE.G

Tracadie Marine or O.GL, BR.GL GL.GL, GLBR.GL O.LG Glaciolacustrine

Tuadook Morainal till O.FHP, O.HFP GL.HFP O.G, FE.G

Violette Morainal till O.HFP, PZ.GL GL.HFP, GLPZ.GL O.G, O.LG

Brunisols Organics E.DYB Eluviated Dystric Brunisol TY.F Typic Fibrisol GLE.DYB Gleyed Eluviated Dystric T.F Terric Fibrisol Brunisol ME.F Mesic Fibrisol HU.M Humic Mesisol Gleysols T.M Terric Mesisol O.G Orthic Gleysol TFI.M Terric Fibric Mesisol FE.G Fera Gleysol THU.M Terric Humic Mesisol R.G Rego Gleysol T.H Terric Humisol O.LG Orthic Luvic Gleysol ME.H Mesic Humisol FE.LG Fera Luvic Gleysol TME.H Terric Mesic Humisol HU.LG Humic Luvic Gleysol O.HG Orthic Humic Gleysol Podzols R.HG Rego Humic Gleysol O.FHP Orthic Ferro-Humic Podzol GL.FHP Gleyed Ferro-Humic Podzol Luvisols O.HFP Orthic Humo-Ferric Podzol O.GL Orthic Gray Luvisol GL.HFP Gleyed Humo-Ferric Podzol GL.GL Gleyed Gray Luvisol FR.HFP Fragic Humo-Ferric Podzol BR.GL Brunisolic Gray Luvisol LU.HFP Luvisolic Humo-Ferric Podzol GLBR.GL Gleyed Brunisolic Gray Luvisol PZ.GL Podzolic Gray Luvisol Regosols GLPZ.GL Gleyed Podzolic Gray Luvisol O.R Orthic Regosol GL.R Gleyed Regosol CU.R Cumulic Regosol GLCU.R Gleyed Cumulic Regosol

horizon. The podzolic B horizon takes precedence and the Regosolic Soils soils are classified as gleyed subgroup members of the Regosolic soils are weakly developed. The Regosolic soils Podzolic order. mapped in central and northern New Brunswick lack development of genetic horizons due to the youthfulness of the material in which they are forming, recent alluvium. 20

They are found along river and stream flood plains described in terms of taxonomic classes, the mapping units throughout the study area. The most pronounced soil are not the same as soil taxa. The purposes of soil development is in the surface layer where a thin organic-rich classification are: to provide a framework for the Ah horizon is often present. Soil development in the rest of formulation of hypotheses about soil genesis and the the profile is usually confined to changes in colour due to response of soil to management; to aide in extending mottling or gleying. Buried mineral-organic layers and knowledge of soils gained in one area to other areas having organic surface horizons may also be found. Only members similar soils; and to provide a basis for indicating the kinds of the Regosol great group occur. They are: Orthic of soils within mapping units (Canada Soil Survey Regosols, Gleyed Regosols, Cumulic Regosols (Fig. 6f) and Committee, 1978) Gleyed Cumulic Regosols. Collivial sites, with active soil deposition as a result of mass-wasting, usually at the base of The soils of the central and northern New Brunswick area steep slopes, may also have regosolic profiles. However, are mapped at the exploratory scale of 1:250,000. The soil these sites are localized and have been included with glacial association was used as the basic unit for soil mapping and till soils. description. The soil association is a grouping of soils that have developed on similar parent material under similar climatic conditions but vary in drainage due to topographic IMPACT OF AGRICULTURE ON SOIL relief. The soil association is a broadly enough defined unit CLASSIFICATION to encompass the variation and range of soils that are encountered within landscape units commensurate with the When land is brought into agricultural production the upper 1:250,000 scale of mapping. profile sequence of mineral and organic horizons are mixed together during cultivation to form an Ap horizon. Soil Soil associations may consists of several subgroups (Table solum horizons are, in whole or in part, incorporated into the 1). Where patterns of soil development are simple, the plow layer. Since soils are classified on the basis of mapping units may consist of one associate (member of an diagnostic horizons that are in the soil solum, the association) and possibly only one subgroup. These units classification of a virgin soil profile may be different than are relatively pure taxonomically speaking. In other areas that of its cultivated counterpart. Within the survey area the the complexity of the landscape is such that soils with depth of solum development averages 40 to 50 cm. The contrasting properties cannot be separated and must be more strongly developed horizons are usually in the upper included in the same unit. It is not possible to show the solum near the surface. On average the furrow slice, that geographic location of these different soils, but rather they portion of the soil turned or sliced by the plow, varies from are complexed on the map. These units consist of two or 20 to 25 cm in thickness. This can account for 40 to 65% of more associates. Since the Canadian System of Soil the average solum thickness. Classification is a national system designed to group different soils across the entire country (ie. the whole Cultivation of a soil can affect classification at the highest population of soils), it is understandable that in some regions taxa, the order and great group levels. Ferro-Humic Podzols the soils have properties that straddle the boundary line are often altered to Humo-Ferric Podzols, Humo-Ferric between two taxa. For example, the well drained associate Podzols to Sombric Brunisols, and Dystric Brunisols to of the McGee Association contains both Orthic Humo-Ferric either Sombric Brunisols or Regosols. Subgroup Podzols and Orthic Ferro-Humic Podzols. These soils have classifications are also affected. For example, Podzolic properties that are close to the taxonomic class boundary. Gray Luvisols often become Brunisolic Gray Luvisols when Drainage variations also result in differences in taxa at the cultivated. This type of variation in classification between higher levels of classification for soils that are located in cultivated and noncultivated conditions is dependent on the close proximity to each other. Well and imperfectly drained nature of development of the soil involved and the degree of Holmesville Association members are both Podzols while disturbance it is subjected to. Many cultivated soils retain their poorly drained counterparts are Gleysols. Intricate their pre-cultivated classification status, others do not. drainage patterns are common and therefore so are complex map units with two or more taxa.

RELATIONSHIP BETWEEN SOIL CLASSIFICATION AND SOIL MAPPING

Soil mapping is the identification, description and delineation on a map of contrasting segments of the landscape based on a set of established differentiating criteria. Soil mapping should not be confused with soil taxonomy or classification. Soil classification systems are methods of organizing information and ideas about soil in a logical and useful manner. Even though map units are 21

PART 3. SOIL MAPPING METHODOLOGY

OFFICE METHODS usually more than 2 m thick and frequently as much as 20 to 30 m thick; sandy skeletal, sandy or coarse loamy; level to Initial efforts consisted of compiling existing information on undulating or sloping terraces, kames, eskers, deltas and the physical resources of the study area that would be useful floodplains. to predict soil properties and distribution. Information was collected on climate, vegetation, geology, physiography, and 4. Marine sediments of clay, silt and sand that are well to geomorphology. This included bedrock and surficial moderately well sorted and stratified as a result of having geology maps, topographic maps, climatic parameter maps settled from suspension in salt or brackish water, or having (temperature, precipitation, etc.) and forest cover type maps. accumulated through shoreline processes such as wave action and longshore drift; ranging from thin discontinuous Previous soil mapping within the study area and soil survey veneers over bedrock or morainal deposits, to in excess of reports and maps from adjoining areas (See Fig. 1), were 50 m thick; sandy, coarse loamy or clayey; level to gently used extensively to establish a preliminary field mapping undulating. legend or key. A brief reconnaissance of the area was used to corroborate the validity of the legend. Discrepancies were 5. Colluvial sediments of nonsorted particle size classes rectified accordingly, additions were made were necessary, ranging from clay to boulders that are products of and the preliminary legend was finalized. mass-wasting and are the result of gravity-induced movement; usually less than 1 m thick, commonly overlying Photo interpretation played a major role in delineating the the Pleistocene till materials from which they have been various soil-landscape units. Aerial photographs taken derived; coarse loamy to fine loamy, with skeletal variations; between 1976 and 1981 at a scale of 1:63,360 were hilly, sloping or hummocky. NOTE: In the final compilation interpreted in terms of soil-landform patterns relevant to colluvial sediments were grouped with morainal deposits soils mapping at the exploratory (1:250,000) level of due to there similarities and intermixed distributions. intensity. Tentative delineations were made on the basis of major landforms. Topographic maps (1:50,000 scale with 6. Organic sediments consist of peat deposits containing 25 or 50 ft contour intervals) were used to check the more than 30% organic matter by weight that are derived accuracy of the delineation boundary lines and the from either sphagnum materials in an ombrotrophic landform-slope designations. Surficial and bedrock geology environment or sedge-forest materials in a eutrophic and photo interpretation were used to estimate soil parent environment; at least 40 cm thick, but in excess of 5 m in materials types. Aerial photographs were the basic tool used some deposits; fibric, mesic, or humic; domed, horizontal, to locate observation sites for ground truthing the predicted or bowl shaped. map polygons. 7. Rock consists of undifferentiated, indurated materials of The major landforms (defined as including both materials bedrock origin that are at or near the surface; the bedrock is and form) used to stratify the survey are were: at the surface or covered by less than 10 cm of regolith material, usually glacial drift; igneous, metamorphic or 1. Morainal sediments of compact or non-compact glacial sedimentary rock; hilly, ridged, sloping or rolling till (lodgment and ablational) consisting of a nonstratified, (associated with upper slope or crest positions). heterogeneous mixture of particle sizes ranging from sand, silt, and clay to gravels, cobbles, stones, and boulders; 10 cm to more than 10 m thick, but usually less than 3 m thick; sandy, coarse loamy or fine loamy, with skeletal variations; FIELD METHODS hilly, hummocky, ridged and sloping to rolling, undulating and level. The conventional or "free mapping" approach to soil-landscape information collection was employed. 2. Residual sediments of unconsolidated or partly weathered Relationships between soils and landforms were established bedrock developed in place from the underlying by observing the soils on strategic points in the landscape, consolidated rock; veneer (10 cm to 1 m thick); sandy such as crests, upper slopes, midslopes, lower slopes, skeletal; rolling. depressions, etc. Once these relationships were established the frequency of observations was reduced to a relatively 3. Fluvial sediments consisting of moderately to well sorted few strategic points to verify the soil type or association. and stratified rounded gravels (and sometime cobbles), These points were selected under stereoscopic examination sands, silts and occasionally clays deposited by flowing of aerial photographs. Accessibility limited the selection of water, both past and present (ie. glaciofluvials and alluvials); these points to locations along roadways, power lines, 22 railroad tracks, etc. Ground accessibility was adequate to Parameters in parentheses - material thickness, boulderiness traverse most map units. However, poor accessibility of a and rockiness - are only indicated in map symbols where few regions did dictate the use of a helicopter for additional relevant. field data collection. Field examination points were well distributed throughout the area with at least one observation The soil association is a natural grouping of soils based on point in 70 to 80% of the delineations. While intensity of similarities in climatic or physiographic factors and soil observations was heavily dependent on accessibility, it also parent material. In this context it is similar to the concept of varied with simplicity or complexity of the soil-landform the soil catena, in that it is a sequence of soils of about the relationships. In complex areas the number of field checks same age, derived from similar parent material, and under required to verify material compositions and distributions similar climatic conditions, but having unlike characteristics was greater than in areas of more uniform soil development. because of variations in relief and drainage. Thirty six soil associations are mapped. The soil associations are listed Field inspections provided ground-truth data to improve the alphabetically in the legend (Table 2) and described in terms quality and accuracy of the soil map. Information and of: mode of deposition, description of the soil parent boundaries for soil-landscape units were extrapolated from material (family particle size class, compactness, reaction, areas with ground inspections by interpretation of the aerial coarse fragment content, lithology), surface form and photographs. In most cases a pit was dug by shovel to physiographic region. This information is expanded upon in expose the soil profile. Road cuts, gravel/fill pits and other the report (Part 4). excavations were used to supplement profile data. Soil observations in mineral soils were made to a depth of 1 m, The remainder of the symbol is used to describe phases (ie. or to a lithic (bedrock) contact in shallow soils. Organic material thickness, drainage, surface expression, slope, soils were examined to a depth of 1.6 m, or to a mineral soil boulderiness, rockiness). Phases describe characteristics that contact, whichever was less. Each observation was described are specific to a given delineation. in terms of specific soil and site criteria. Descriptions and classifications were in accordance with procedures Material thickness indicates the average thickness of established in the Canadian System of Soil Classification regolith or soil material overlying solid bedrock. (Soil Classification Working Group 1998). Soil parameters included: horizon or layer designations, depths, colour, Drainage refers to the actual moisture content in excess of structure, consistence, mottles were present, reaction class, field capacity and the extent of the period during which such texture and coarse fragment type and content. Site excess water is present in the control section. For example, information consisted of: parent material mode of in well drained soils excess water flows downward readily deposition, surface expression, slope characteristics, into underlying pervious material, or laterally as subsurface drainage and moisture regime, erosion features, surface flow. The water source is precipitation. In contrast, in poorly stoniness, depth to bedrock, land use and vegetation. drained soils the water is removed so slowly in relation to supply that excess water is evident in the soil for a large part A number of representative soil profiles were described in of the time. Water sources are subsurface and/or detail and sampled for laboratory analysis to characterize the groundwater flow in addition to precipitation. Established soil in terms of selected physical and chemical properties. drainage classes (Expert Committee on Soil Survey, revised 1982) of excessive, well, moderately well, imperfect, poor and very poor are grouped into seven drainage categories. MAP SYMBOL Surface expression signifies a unique surface form The map symbol is the link between the soil map and the (assemblage of slopes) or pattern of forms that are repeated report. It is designed to convey information about the soils in nature. For example, rolling is a very regular sequence of and map units to the reader or user. Mapped soil and non- moderate slopes extending from rounded, sometimes soil portions of the landscape are delineated on the soil map. confined concave depressions to broad, rounded convexities These delineations or polygons are labelled on the map by producing a wavelike pattern of moderate relief. a symbol which is made up of letters and numbers representing classes of selected soil and landscape Slope quantifies the degree of inclination of the dominant properties. Descriptions or explanations for the various slopes within the map polygon. Slopes of similar magnitude components of the map symbol are provided in the map are grouped into seven classes expressed in percent slope. legend (Table 2). The map symbol used for the purpose of this survey is typically as follows: Boulderiness is defined as the percentage of the land surface occupied by stones greater than 1 m in diameter.

Soil Association(s) (Material Thickness) Drainage Rockiness indicates the percentage of the land surface Surface Expression Slope (Boulderiness) (Rockiness) occupied by bedrock exposures (or soil material less than 10 cm thick over bedrock). 23

Table 2. Soil mapping legend

Soil Associations and Land Types:

Mode of Physiographic Name Symbol Deposition Description of Soil Parent Material Surface Form Region

Acadie AS Paludification 40 to 160 cm of acidic, brown to dark brown, Flat, bowl Maritime Plain Siding mesic and humic sedge-sphagnum peats over or horizontal N. B. Highlands undifferentiated mineral soil deposits.

Barrieau- BB Marine over 20 to 100 cm of acidic, yellowish brown to Undulating to Maritime Plain Buctouche morainal till brown, sandy, noncompact marine sediments level blanket with less than 20% (but usually less than or veneer 5%) coarse fragments of mostly gray-green sandstones over acidic, yellowish brown to dark reddish brown, loamy compact till with 15 to 20% coarse fragments of mostly gray-green sandstone.

Belldune BR Marine Acidic, reddish brown to yellowish brown Undulating Chaleur Uplands River coarse loamy to sandy skeletal, noncompact, material with 15 to 50% coarse fragments of conglomerate, sandstone, siltstone, argillite and some limestone.

Big Bald BM Residual Acidic, yellowish brown, sandy skeletal, Hilly to rolling N .B. Highlands Mountain noncompact material with 15 to 50% coarse fragments veneer derived from feldspar rich granite weathered in situ.

Boston BO Morainal till Acidic, olive to olive brown, fine loamy Rolling to hilly Chaleur Uplands Brook (skeletal), noncompact, (but slightly firm), veneers and material with 10 to 30% coarse fragments of blankets argillite, slate and fine-grained sandstones.

Caribou CB Morainal till Neutral, olive to olive brown, fine loamy Undulating, Chaleur Uplands noncompact (but slightly firm in the Bt and rolling, hilly C) material with 10 to 30% coarse fragments of sloping calcareous shale, argillite and slate and blanket and some limestone. veneers

Carleton CR Morainal till Neutral, olive to yellowish brown, fine loamy, Rolling, undulating, Chaleur Uplands compact material with 10 to 30% coarse fragments hilly and sloping of calcareous shale, argillite and slate and blankets and veneers some calcite.

Catamaran CT Morainal till Acidic, yellowish brown to olive brown, Rolling, undulating, N. B. Highlands coarse loamy, compact material with 10 to 25% hilly and sloping coarse fragments of granite, schist, quartzite, blankets and veneers slate and sandstone.

Gagetown GG Fluvial Acidic, yellowish brown to brown, sandy Terraced, N. B. Highlands (Glaciofluvial) skeletal, noncompact sediments with 35 to 70% undulating Maritime Plain coarse fragments of mixed igneous and and hummocky metamorphic and miscellaneous sedimentary rocks.

Grand GF Fluvial Acidic, olive to olive brown, sandy skeletal Terraced N. B. Highlands Falls (Glaciofluvial) noncompact sediments with 35 to 70% and hummocky Chaleur Uplands fragments of noncalcareous slate, shale, Notre Dame Mtn quartzites and sandstones. 24

Table 2. Soil mapping legend cont’d

Mode of Physiographic Name Symbol Deposition Description of Soil Parent Material Surface Form Region

Guimond GM Fluvial Acidic, olive to yellowish brown, sandy Terraced, Maritime Plain River (Glaciofluvial) skeletal, noncompact sediments with 35 to 70% undulating coarse fragments of soft gray-green sandstone. and hummocky

Holmesville HM Morainal till Acidic, olive to olive brown, coarse loamy, Rolling, undulating Chaleur Uplands compact material with 10 to 30% coarse fragments and hilly blankets Notre Dame Mtn of quartzite and sandstones and miscellaneous and veneers N. B. Highlands argillite, slate and schist.

Interval IN Fluvial Acidic to neutral, olive to yellowish brown, Terraced and Maritime Plain (Alluvial) stratified coarse loamy and sandy, noncompact undulating to level N. B. Highlands sediments with very few coarse fragments of undifferentiated lithologies.

Jacquet JR Morainal till Acidic, yellowish brown, coarse loamy, Undulating to hilly N. B. Highlands River noncompact material with 20 to 40% coarse blankets and veneers Chaleur Uplands fragments of rhyolite and trachyte, with some basalt and miscellaneous slate and greywacke.

Juniper JU Morainal till Acidic, yellowish brown to brown, coarse loamy Rolling and N. B. Highlands to sandy (skeletal), noncompact material hilly veneers and with 20 to 50% coarse fragments of granite, grano- blankets or diorite, diorite, granite gneiss and undulating to miscellaneous volcanics. hummocky

Lavillette LV Paludification Acidic, brown to dark reddish brown, fibric Domed Maritime Plain (and minor mesic) sphagnum peats usually thicker than 1.6 m over undifferentiated mineral soil deposits.

Long Lake LL Morainal till Acidic, olive brown, coarse loamy, compact Rolling, hilly N. B. Highlands material with 20 to 40% coarse fragments of slate, and undulating Chaleur Uplands siltstone, argillite, schist and miscellaneous blankets and quartzite and greywacke. veneers

Maliseet MA Fluvial Acidic, olive to yellowish brown, stratified Level and Chaleur Uplands (Ancient alluvial) sandy to coarse loamy, noncompact sediments terraced Notre Dame Mtn with less than 10% coarse fragments of slate, shale miscellaneous quartzite and volcanics.

McGee MG Morainal till Acidic, olive to olive brown, coarse loamy Rolling, hilly N. B. Highlands (skeletal), noncompact material with 20 to 50% and sloping Chaleur Uplands coarse fragments of slate, argillite, schist, blankets and Notre Dame Mtn greywacke and quartzite. veneers

Muniac MU Fluvial Neutral, olive to olive brown, sandy skeletal Terraced Chaleur Uplands (Glaciofluvial) noncompact sediments with 35 to 70% and hummocky fragments of calcareous slate, shale, quartzites and sandstones.

Nigadoo NR Morainal till Acidic, yellowish brown, coarse loamy, compact Variable - undulating, Chaleur Uplands River material with 15 to 30% coarse fragments of rolling, hilly, ridged N. B. Highlands metagabbro and metabasalt, with some granites, and hummocky conglomerate and metagreywacke. veneers and blankets

Parleeville PA Morainal till Acidic, dark reddish brown, coarse loamy, Rolling and Chaleur Uplands noncompact material with 15 to 30% coarse undulating N. B. Highlands fragments of sandstone and conglomerate. blankets and veneers 25

Table 2. Soil mapping legend cont’d

Mode of Physiographic Name Symbol Deposition Description of Soil Parent Material Surface Form Region

Popple PD Morainal till Acidic, yellowish brown to olive brown, coarse Rolling, hilly N. B. Highlands Depot loamy (skeletal), compact material with 20 to 40% and sloping Chaleur Uplands coarse fragments of rhyolite and trachyte, with some veneers and basalt and miscellaneous slates and greywacke. blankets

Reece RE Morainal till Acidic, strong brown to dark yellowish brown, loamy, Undulating Maritime Plain compact material with 10 to 25% coarse fragments blankets and of soft gray-green sandstone and miscellaneous veneers remnants of highly weathered shale.

Richibucto RB Marine Acidic, yellowish brown to brown, sandy, non- Undulating and Maritime Plain compact sediments with less than 20% (but level veneers, usually less than 2%) coarse fragments of blankets and soft gray-green sandstone. thicker deposits

Riverbank RI Fluvial Acidic, yellowish brown to olive brown, sandy Terraced and Maritime Plain (Mixture of noncompact sediments with less than 20% (but level N. B. Highlands glaciofluvials usually less than 2%) coarse fragments of mixed and alluvials) igneous, metamorphic and minor amounts of sedimentary rock types.

Rogersville RS Morainal till Acidic, brown, fine loamy, compact material Undulating Maritime Plain with 10 to 25% coarse fragments of sandstone, blankets granites, gneiss, schists and some volcanics and miscellaneous remnants of highly weathered shale.

Salt Marsh SM Marine Undifferentiated marine deposits along Level Maritime Plain coast or tidal river, submerged at high tide Chaleur Uplands by salt water

Sand Dune SD Aeolian Low ridges of loose windblown sand along Ridged Maritime Plain the coast Chaleur Uplands

St. Quentin SQ Paludification Usually less than 160 cm of neutral, dark Flat, bowl Chaleur Uplands brown, forest-fen peats over undifferentiated and horizontal mineral soil deposits.

Stony SB Morainal till Acidic, red to reddish brown, fine loamy, Undulating and Maritime Plain Brook compact material with 10 to 25% coarse fragments level blankets of soft gray-green sandstone and miscellaneous and veneers remnants of highly weathered shale.

Sunbury SN Morainal till Acidic, yellowish brown to brown, coarse loamy Undulating Maritime Plain to sandy (skeletal), noncompact material with blankets and 15 to 35% coarse fragments of soft gray-green veneers sandstone.

Tetagouche TT Morainal till Acidic, strong brown, fine loamy, compact Undulating and Chaleur Uplands material with 10 to 25% coarse fragments of rolling with some metagabbro, metabasalt, metagreywacke and ridged and hilly conglomerate. blankets and veneers

Tetagouche TF Morainal till Acidic, strong brown, loamy, noncompact Rolling to hummocky Chaleur Uplands Falls material with 15 to 35% coarse fragments of or ridged and hilly N. B Highlands metagabbro, metabasalt, metagreywacke and veneers, blankets and conglomerate. deeper phases

Thibault TH Morainal till Neutral, light olive brown, coarse loamy, non- Rolling and hilly Chaleur Uplands compact material with 10 to 35% coarse fragments blankets and Notre Dame Mtn of weakly calcareous shale, slate, quartzite, veneers argillite and sandstone. 26

Table 2. Soil mapping legend cont’d

Mode of Physiographic Name Symbol Deposition Description of Soil Parent Material Surface Form Region

Tracadie TC Marine or Neutral, red to yellowish brown, clayey, Level and Maritime Plain glaciolacustrine compact sediments with less than 2% coarse undulating fragments of undifferentiated lithologies. blankets and deeper phases

Tuadook TU Morainal till Acidic, yellowish brown to brown, coarse loamy Rolling, hilly N. B. Highlands (skeletal), compact material with 15 to 35% coarse and sloping fragments of granite, granodiorite, diorite, blankets and granite gneiss and miscellaneous volcanics. veneers

Violette VO Morainal till Acidic, light olive brown, fine loamy, compact Rolling, undulating Chaleur Uplands material with 10 to 25% coarse fragments of and hilly veneers N. B. Highlands quartzite, sandstone and miscellaneous shale, and blankets argillite and slate.

Water WA - Small unnamed water bodies - All regions

Material Thickness: v - veneer, less than 1 m to bedrock. b - blanket, 1 to 2 m to bedrock. Where no material thickness is indicated it can be assumed to be greater than 2 m.

Drainage:

1 - excessively, well and/or moderately well drained (greater than 80% of the area) 2 - dominated ( greater than 40%) by excessively, well and/or moderately well drained with significant (20-40%) imperfectly drained 3 - dominated by excessively, well and/or moderately well drained with significant poorly drained 4 - dominated by imperfectly drained with significant excessively, well and/or moderately well drained 5 - dominated by imperfectly drained with significant poorly and/or very poorly drained 6 - dominated by poorly and/or very poorly drained with significant imperfectly drained 7 - poorly and/or very poorly drained

Surface Expression: h - hummocky: a complex sequence of slopes extending from somewhat rounded depressions or kettles of various sizes to irregular to conical knolls and knobs. Elevation differences are usually less than 100 m. I - inclined: a sloping, unidirectional surface with a general constant slope not broken by marked irregularities. l - level: a flat or gently sloping, unidirectional surface with a generally constant slope not broken by marked elevations and depressions. Slopes are generally less than 2%. m - rolling: a very regular sequence of moderate slopes extending from rounded, sometimes confined concave depressions to broad rounded convexities producing a wavelike pattern of moderate relief. Slope length is often 1.6 km or greater and gradients are greater than 5%. r - ridged: a long, narrow elevation of the surface, usually sharp crested with steep sides. s - sloping: an inclined multi-directional surface with variable slopes broken by marked irregularities. t - terraced: a scarp face and the horizontal or gently inclined surface (tread) above it. u - undulating: a very regular sequence of gentle slopes that extends from rounded, sometimes confined concavities to broad rounded convexities producing a wavelike pattern of low local relief. Slope length is generally less than 0.8 km and the dominant gradient of slopes is 2-5%. y - hilly: a very complex sequence of slopes extending from weakly to moderately incised depressions of various sizes to somewhat rounded crests and peaks. Elevation differences are usually greater than 100 m.

An asterisk following the surface expression (eg. m*, etc.) indicates that the landform is significantly dissected by steeply incised drainage channels. 27

Table 2. Soil mapping legend cont’d

Slope: Rockiness: Boulderiness:

Class % Slope % Surface Distance (m) % Surface Distance (m) 1 0-0.5 Class exposed between exposures Class exposed between exposures 2 0.5-2 R1 2-10 75+ B1 0.01-0.1 30-10 3 2-5 R2 10-25 25-75 B2 0.1-3 10-2 4 5-9 B3 3-15 2-1 5 9-15 B4 15-50 1-0.1 6 15-30 B5 50+ less than 0.1 7 30-45 8 45-70 9 70-100

All delineations with exactly the same symbol constitute a names have been used to indicate the kind of soil and/or non- map unit. Because of the open mapping legend approach soil materials present. Three land types were mapped - salt that is used in this soil survey, a majority of map units are marsh, sand dune and water bodies. Where a land type has unique. These tend to be the simpler map units. Map units been mapped, no additional information is provided on surface may contain one to three soil associations. Simple map units texture, slope, drainage, etc. consist of 100% of soils that have properties as defined for the designated soil association. Complex map units are used SOIL CORRELATION WITH ESTABLISHED SOIL to describe areas were a second and possibly third soil CONCEPTS association is significant in areal abundance, but so intricately mixed with the dominant soil association that it Soil correlation is the process of maintaining consistency in (they) can not be separated out at the 1:250,000 scale of naming and classifying soils. Over the years soil survey has mapping. In complex map units consisting of two soil gradually defined and categorized many of the different soils associations, the first or dominant soil association accounts found in New Brunswick. The central and northern New for 70% of the area and the second or significant soil Brunswick area shares a common boundary with seven association for 30%. In complex map units consisting of regional reconnaissance soil survey areas (Fig. 1). Other three soil associations, the first soil association accounts for detailed or reconnaissance soil survey mapping has also been 50% of the area, the second soil association for 30% of the conducted within the study area. There is a need to correlate area and the third soil association for 20% of the area. the soils mapped in these previous studies to the soil legend Inclusions are areas of unspecified soil or nonsoil bodies used in this report. Table 3 is a summary of the relationships that occur within delineated map units. Typically up to 15% among the soil associations used in the Exploratory Soil of a mapped polygon may consist of inclusions of different Survey of Central and Northern New Brunswick and soil materials. established soil series from other survey areas in the province.

The degree of detail that is required or intended ultimately In most of the earlier mapping programs the soil series was the determines the minimum size area that should be depicted taxonomic element employed to describe the mapping units. on the soil map. At a mapping scale of 1:250,000, a map The soil series provides more precise information about the area of 0.5 cm2 represents 156 ha of land. This is the soil mapping unit than does the soil association. This was smallest area that should be identified on the map, however, appropriate because the scale of mapping of these earlier in a few instances, areas smaller than this with highly surveys was of a more detailed nature (ie, larger scale). The contrasting soil and landscape differences, were mapped. concept of the soil series has evolved over the years, it is dynamic. Soil mapping in the Fredericton-Gagetown and In total, 685 soil polygons were mapped with an average Woodstock areas during the late 1930's employed a concept of polygon size of 4060 ha, a minimum polygon size of 37 ha the soil series that was somewhat analogous to a geological and a maximum polygon size of 43,236 ha. formation based on origin of material, lithology, weathering and colour, and subdivided into textural classes. This concept Land Types has changed greatly over the years to the present day where the soil series has precisely defined limits in terms of colour, Natural and man-made units in the landscape that are either texture, structure, consistence, thickness and degree of highly variable in content, have little or no natural soil, or are expression of horizons and of the solum, abundance of coarse excessively wet, are referred to as land types. Connotative fragments, depth to bedrock, depth to free carbonates, pH, and 28 lithology, for mineral soils; and parent material botanical and land segments that are similar in geomorphic position, origin, abundance of logs and stumps, calcareousness, bulk landform, and soil properties. It is an amalgamation of density, mineral content, soil development, and mineralogy of similar catenary associations. For example, as defined in this the terric layer, for organic soils. A few of the later date report, the Juniper Association consists of the Juniper catena reconnaissance-detailed surveys (ie. Rogersville-Richibucto, (Juniper, Jummet Brook, and McKiel series) and the Irving Chipman-Minto-Harcourt) utilized an association-catena type catena (Irving, Goodfellow and Halls Brook series). Both concept whereby each of the associates (association drainage catenas have developed in coarse loamy stony ablation or water members) is basically equivalent to the soil series. Because of reworked till parent materials derived from gray and red drainage difference, the soil series that form a catenary granites, with some basalts, felsites and volcanics in a rolling sequence can be quite dissimilar in soil profile horizons and to hilly or sloping landform. The soils and landscape other properties. However, these soil series are closely properties that are used to differentiate the two catenas are not associated under field conditions and so the catenary mappable at the exploratory level of investigation and so they association is a very practical grouping for mapping the soils have been combined into one association, Juniper. The soil of a region. By convention, the catena-association name is properties for the "new" Juniper Association have ranges that taken from the name of the most rapidly drained member of the are broad enough to include both of the former catenas. In drainage sequence. Referring to soils on a catenary basis was other instances the soil association consists of only one also seen as a means of reducing the number of soil names catenary association ie. the Interval catena (Interval, Waasis involved. A Cyr soil is simply referred to as a poorly drained and East Canaan series). Here the association definition is a Grand Falls, a Blackville soil as an imperfectly drained Stony generalized catenary association description, expanded as Brook, and so on. required to include variations found during mapping.

The soil association concept employed in the central and northern New Brunswick survey area is more broadly defined than the catenary association. It is a grouping of related soils

Table 3. Correlation of soil associations mapped in central and northern New Brunswick with established soil series as listed in "Soils of New Brunswick: A First Approximation" (Fahmy et al. 1986)

Established New Brunswick Soil Series Rapidly to Mod Well Imperfectly Poorly to Very Poorly Soil Association Drained Drained Drained

Acadie Siding Acadie Siding* Chelmsford*

Barrieau-Buctouche Barrieau* Cote d'Or Shediac Bretagneville* St. Charles* Buctouche* Michaud Neguac

Belldune River Belldune River* Durham Centre* Green Point*

Big Bald Mountain Big Bald Mountain*

Boston Brook Boston Brook* Skin Gulch Yellow Brook

Caribou Caribou* Carlingford Washburn Jardine* Nickle Mills Five Fingers Undine* Harquail* Quisibis* Dube Big Spring

Carleton Carleton* Canterbury Canterbury (Washburn) Kedgwick* Siegas* Salmon Bourgoin 29

Table 3. Correlation of soil associations mapped in central and northern New Brunswick with established soil series as listed in "Soils of New Brunswick: A First Approximation" (Fahmy et al. 1986) cont’d

Established New Brunswick Soil Series Rapidly to Mod Well Imperfectly Poorly to Very Poorly Soil Association Drained Drained Drained

Catamaran Catamaran*

Gagetown Gagetown* Geary Penobsquis

Grand Falls Grand Falls* Sirois Cyr

Guimond River Guimond River* St. Olivier St. Theodule Cocagne* Lord and Foy*

Holmesville Holmesville* Johnville Poitras

Interval Interval* Waasis East Canaan

Jacquet River Jacquet River*

Juniper Juniper* Jummet Brook McKiel Irving* Goodfellow Halls Brook

Lavillette Lavillette* Legaceville*

Long Lake Long Lake* Blue Mountain Colter Mountain Serpentine* Adder Jenkins Britt Brook* Portage Lake Babbit Brook

Maliseet Maliseet* Wapske Wapske Flemming* Martial Kelly Benedict*

McGee McGee* Nason Trafton Glassville* Temiscouata Foreston

Muniac Muniac* Ennishore Cyr

Nigadoo River Nigadoo River*

Parleeville Parleeville* Midland Midland

Popple Depot Popple Depot*

Reece Reece* Chipman Pangburn

Richibucto Richibucto* Cap Lumiere Nevers Road Kouchibouguac* Potters Mills Vautour Bay-du-Vin* Napan Fontaine Chockpish* Caissie* Galloway* Smelt Brook Briggs Brook Babineau* Escuminac* Baie-Ste.-Anne Miscou Island*

Riverbank Riverbank* Oromocto Nevers Road

Rogersville Rogersville* Acadieville Rosaireville 30

Established New Brunswick Soil Series Rapidly to Mod Well Imperfectly Poorly to Very Poorly Soil Association Drained Drained Drained

St. Quentin St. Quentin*

Stony Brook Stony Brook* Blackville Shinnickburn Harcourt* Coal Branch Grangeville St. Gabriel* North Forks North Forks

Sunbury Sunbury* Hoyt Cork Big Hole* Beaver Lake Fair Isle* Black Brook

Tetagouche Tetagouche*

Tetagouche Falls Tetagouche Falls*

Thibault Thibault* Guercheville Lauzier Monquart*

Tracadie Tracadie* Bouleau Sheila Mount Hope* Boland Cambridge Fundy* Canobie

Tuadook Tuadook* Redstone Lewis

Violette Violette*

* Catenary association name. 31

PART 4. SOIL ASSOCIATION IDENTIFICATION KEY AND GENERAL DESCRIPTION

KEY TO SOIL ASSOCIATION PARENT vegetative cover, and related associations and how they are MATERIALS differentiated. Profile and/or landscape photographs are included for some of the dominant soil associations. Summary A key to the soil association parent materials in the central and tabular information is provided at the end of each soil northern New Brunswick map area is presented in Table 4. association description. The soils are systematically keyed out using chemical, physical, morphological and genetic properties and characteristics of the parent material. The sequence of Acadie Siding Association parameters utilized includes, in mineral soils: mode of deposition, particle size class, consistence, reaction class, The Acadie Siding Association is made up of soils which are colour, and coarse fragment lithology; and in organic soils: composed of organic materials. They consist of relatively thin botanical origin, degree of decomposition, reaction class, peatland deposits, averaging 0.4 to 1.6 m in thickness, with colour and thickness. The key provides a means to identify an weakly to well-decomposed sphagnum and sedge plant association, or of differentiating one association from another. remains. Acadie Siding soils have developed as a result of the It is also an orderly arrangement of the distinguishing features "gradual build-up" process (Tarnocai, 1981). This process of a group of soils that facilitates the classification and involves the invasion of poorly drained areas by hydrophytic determination of relationships. Soils are grouped into similar vegetation, particularly mosses and sedges. As plant debris classes according to diagnostic characteristics. For example, accumulates above the level of the surrounding nutrient rich Reece, Stony Brook, Tetagouche, and Violette are all mineral ground water, the deposition becomes more and more acidic soils developed on glacial till deposits of fine loamy, compact, and "nutrient poor", or ombrotrophic. Essentially, they are flat, acidic material. These soil associations are differentiated from basin or bowl bogs (Tarnocai 1981) that have developed on each other on the basis of more detailed characteristics, ie. soil horizontal or channel fens. Acadie Siding soils occur mostly colour and coarse fragment lithology. A more general in the Maritime Plain portion of the survey area (Fig. 7) on grouping of soils would be that of all mineral soils developed level to undulating landscapes with slopes of less than 5%. in marine sediments. This includes; Richibucto, a sandy Some scattered deposits are also found in the New Brunswick noncompact acidic material; Belledune River, a coarse loamy Highlands. Although they only account for 45,435 ha, to sandy skeletal noncompact acidic material; and Tracadie, a representing less than 1.63% of the survey area, Acadie Siding clayey compact neutral material. The Reece-Stony Brook- soils commonly occur as unmapped inclusions in other organic Tetagouche-Violette grouping can be considered a fourth level soils map units, or with very poorly drained mineral soils. grouping (composition, mode of deposition, particle size-consistence, reaction), whereas the Richibucto-Belledune River-Tracadie grouping is a second level grouping (composition, mode of deposition).

SOIL ASSOCIATION GENERAL DESCRIPTION

A general description of each soil association is provided in the following text. These descriptions include information on soil, landscape and related attributes. A map of the survey area shows the location of polygons where the soil association has been mapped. The soil profile is discussed in terms of horizon sequence and classification in the Canadian System of Soil Classification (Canada Soil Survey Committee 1978), texture, consistence, structure, colour, coarse fragment content (G, gravels; C, cobbles; S, stones), reaction, moisture holding capacity, available rooting zone, internal drainage, mottling, gleying and inherent fertility. General landscape conditions are discussed. These include; slope, surface expression, Figure 7. Location of mapped Acadie Siding soils. elevation, material thickness, depth to bedrock, mode of deposition, stoniness, boulderiness and drainage (catena Acadie Siding peatlands usually have level or flat surfaces that members, site drainage, runoff). Information is also provided are not raised above the surrounding terrain. Although peat on location (ie. physiographic region, etc.) and extent, depths are relatively uniform, they decrease in depth from the 32

Table 4. Key to soil association parent materials in the central and northern New Brunswick map area

I. Mineral soils. A. Soils developed on glacial till. 1. Sandy, non-compact. a. Acidic. I. Yellowish brown to brown; coarse fragments - granites, granodiorites, diorites, granite gneiss and miscellaneous volcanics; frequently skeletal...... Juniper ii. Yellowish brown to brown; coarse fragments - soft grey-green sandstone; frequently skeletal...... Sunbury 2. Coarse loamy, non-compact. a. Acidic. I. Olive to olive brown; coarse fragments - slate, argillite, schist, greywacke and quartzite; frequently skeletal...... McGee ii Yellowish brown; coarse fragments - rhyolite, trachyte, basalt and miscellaneous slates and greywacke...... Jacket River iii Yellowish brown to brown; coarse fragments - granites, granodiorites, diorites, granite gneiss and miscellaneous volcanics; frequently skeletal...... Juniper iv. Yellowish brown to brown; coarse fragments - soft grey-green sandstone; frequently skeletal...... Sunbury v. Dark reddish brown; coarse fragments - sandstone and conglomerate...... Parleeville b. Neutral. I. Light olive brown; coarse fragments - weakly calcareous shales, slates, quartzites, argillites and sandstones...... Thibault 3. Coarse loamy, compact. a. Acidic. I. Olive brown; coarse fragments - slate, siltstone, argillite, schists and miscellaneous quartzite and greywacke; frequently skeletal...... Long Lake ii. Yellowish brown to olive brown; coarse fragments - quartzite, sandstone and miscellaneous argillite, slate and schists...... Holmesville iii. Yellowish brown to olive brown; coarse fragments - granites, schists and quartzites...... Catamaran iv. Yellowish brown to olive brown; coarse fragments - rhyolite, trachyte, basalt and miscellaneous slates and greywacke; frequently skeletal...... Popple Depot v. Yellowish brown; coarse fragments - metagabbro and meta basalt with some granites, conglomerate and metagreywacke...... Nigadoo River vi. Yellowish brown to brown; coarse fragments - granites, granodiorites, diorites, granite gneiss and miscellaneous volcanics; occasionally skeletal...... Tuadook 4. Loamy, non-compact a. Acidic. I. Strong brown; coarse fragments - metagabbro and meta basalt with some granites, conglomerate and metagreywacke...... Tetagouche Falls 5. Fine loamy, non-compact a. Acidic. I. Olive to olive brown; coarse fragments - argillites, slates and fine grained sandstones...... Boston Brook b. Neutral. I. Olive to olive brown; coarse fragments - calcareous shale, argillite and slate and some limestone...... Caribou 6. Fine loamy, compact a. Acidic. I. Light olive brown; coarse fragments - quartzite, sandstone and miscellaneous shale, argillite and slate...... Viloette ii. Yellowish brown to brown; coarse fragments - soft gray-green sandstone and miscellaneous remnants of shale...... Reece iii. Brown; coarse fragments - sandstones, granites, gneiss, schists, and some volcanics and miscellaneous remnants of highly weathered shale ...... Rogersville iv. Strong brown; coarse fragments - metagabbro and meta basalt with some granites, conglomerate and metagreywacke...... Tetagouche v. Red to reddish brown; coarse fragments - soft gray-green sandstone and miscellaneous remnants of shale...... Stony Brook b. Neutral. I. Olive to yellowish brown; coarse fragments - calcareous shale, argillite and slate and some calcite...... Carleton B. Soils developed in residual materials. 1. Sandy skeletal, non-compact a. Acidic. I. Yellowish brown; coarse fragments - granite...... Big Bald Mountain 33

Table 4. Key to soil association parent materials in the central and northern New Brunswick map area cont’d

C. Soils developed in fluvial sediments. 1. Sandy skeletal, non-compact. a. Acidic. I. Olive to olive brown; coarse fragments - noncalcareous slate, shale, quartzite and sandstone...... Grand Falls ii. Olive to yellowish brown; coarse fragments - soft gray-green sandstone...... Guimond River iii. Yellowish brown to brown; coarse fragments - mixed igneous, metamorphic and miscellaneous sedimentary...... Gagetown b. Neutral. I. Olive to olive brown; coarse fragments - calcareous slate, shale, quartzite and sandstone...... Muniac 2. Sandy, non-compact. a. Acidic. I. Yellowish brown to olive brown; coarse fragments - mixed...... Riverbank 3. Sandy to coarse loamy, non-compact. a. Acidic. I. Olive to yellowish brown; coarse fragments - slate, shale and miscellaneous quartzite and volcanics...... Maliseet 4. Coarse loamy, non-compact. a. Acidic to neutral. I. Olive to yellowish brown; coarse fragments - none; floods...... Interval D. Soils developed in marine sediments. 1. Sandy, non-compact. a. Acidic. I. Yellowish brown to brown; coarse fragments - soft gray-green sandstone...... Richibucto 2. Coarse loamy to sandy skeletal, non-compact. a. Acidic. I. Reddish brown to yellowish brown; coarse fragments -conglomerate, sandstone, siltstone, argillite and some limestone...... Belldune River 3. Clayey, compact. a. Neutral. I. Red to yellowish brown; coarse fragments - very few, mixed...... Tracadie E. Soils developed in marine or fluvial sediments over glacial till deposits. 1. Sandy, noncompact over loamy, compact. a. Acidic over acidic. I. Yellowish brown to brown; coarse fragments - very few, undifferentiated over yellowish brown to dark reddish brown; coarse fragments - undifferentiated...... Barrieau-Buctouche II. Organic soils. A. Soils developed in sphagnum peat. 1. Dominantly fibric. a. Acidic. I. Brown to dark reddish brown; usually greater than 160 cm thick...... Lavillette B. Soils developed in sedge-sphagnum peat. 1. Dominantly mesic and humic. a. Acidic. I. Brown to dark brown; usually less than 160 cm thick...... Acadie Siding C. Soils developed in forest-fen peat. 1. Dominantly mesic and humic. a. Neutral. I. Dark brown; usually less than 160 cm thick...... St. Quentin 34 centre of the deposit outwards. Inclusion of areas with which varies from mesic to humic, also plays a major role in thicknesses of more than 1.6 m may occur. Pronounced the classification of Acadie Siding soils. Where the control surface patterns are usually lacking with the exception of the section of the profile is dominated by well-decomposed presence of intermittent to semi-permanent drainage courses. sedge-sphagnum peats, the soil is classified as a Humisol. Most deposits are topographically confined in depression-like Inclusions of areas of deeper deposition (i.e., nonterric) usually areas. consist of thicker layers of both fibric and mesic-humic peats, which are classified as Typic Mesic Fibrisols or Typic Fibric Vegetative cover is dominated by sphagnum mosses and Mesisols. ericaceous shrubs, with varying amounts of sedges and reeds. Most deposits are treeless or treed with stunted dwarf black Acadie Siding soils are associated with other organic soils, as spruce and tamarack in the centre, but with increasing cover at well as with poorly and very poorly drained members of some the margins. Those sites that are more strongly minerotrophic mineral soils. Lavillette is a common organic soil associate. (nutrient-rich) have increased concentrations of sedges, Lavillette soils differ from Acadie Siding soils in that they grasses, reeds, and even herbs. They also have denser tree consist of deep, non-terric, weakly decomposed, fibric cover. materials found on well-developed, domed or raised bogs. Lavillette soils usually have a distinctive circular surface Peat stratigraphy usually consists of a surface layer 20 to 100 pattern not present on Acadie Siding soils. Very poorly or cm thick of fibric (weakly decomposed) sphagnum peats with poorly drained Barrieau-Buctouche, Richibucto, Reece, Stony some shrubby materials, over a layer of mesic (moderately Brook and Sunbury mineral soils are also close associates. decomposed) and/or humic (well-decomposed) Acadie Siding soils have been mapped less frequently with sedge-sphagnum to sedge peat. This material extends to the Catamaran, Juniper, Long Lake and Tuadook mineral soils. terric (mineral) contact. The underlying mineral material is Acadie Siding soils are differentiated from mineral soils based variable, usually being whatever is the predominate material in on the depth of organic material present. To be classed as the surrounding area. Acadie Siding, a soil must have at least 40 cm of dominantly mesic or humic organic material or 60 cm of dominantly fibric The surface peat is brown to dark reddish brown, acidic (pH organic material, otherwise it is included with the appropriate in H2O of less than 4.5), low in bulk density (less than 0.1 mineral soil association. g/cm3), moderately rapid to rapidly permeable (saturated hydraulic conductivity of 10 to 15 cm/hr), and highly fibrous Acadie Siding soils are considered to have no immediate with a class 1 to class 4 rating on the von Post scale of decom- potential for forest or agricultural crops. Costs associated with position. Properties of the subsurface peat differ, mostly as a development and management are considered to be excessive. result of its more advanced state of decomposition and different botanical origin. The subsurface peat is brown to Summary of general characteristics of the Acadie Siding Association dark brown, acidic (pH in H2O of less than 4.5), moderate to 3 Map Symbol : AS high in bulk density (approximately 0.15 g/cm ), moderately Physiographic Region(s) : Maritime Plain, N. B. Highlands to very slowly permeable (saturated hydraulic conductivity of Elevation : < 150 m 1.0 to less than 0.1 cm/hr), and moderate to low in rubbed fibre Extent : 45,435 ha content with a class 5 to class 8 rating on the von Post scale of Percentage of Mapped Area : 1.63% Parent Material Type : Organic decomposition. Mode of Origin : Basin or bowl bogs Material Thickness : 0.4-1.6 m over mineral soil Drainage is very poor. Water table levels are at or near the Soil Colour : Brown to dark brown surface throughout the year resulting in ponding. Ground Degree of Decomposition : Moderately to very strongly decomposed Botanical Composition : Sphagnum and sedge peat water is acidic to neutral and of low to moderate nutrient Inherent Fertility : Very low status. Topography (slope) : Flat (<1%) in an undulating landscape (<5%) Acadie Siding soils are dominantly Terric Mesisols, Terric Drainage (dominant) : Very poor Classification (typical) : Terric Mesisol Fibric Mesisols or Terric Humic Mesisols, but with significant Terric Humisol and Terric Fibrisol components. Total thickness of the organic material ranges from 40 to 160 cm over the mineral soil (terric) contact. Variation in clas- Layer Friable upper Subsoil Subsoil sification depends upon the relative thicknesses of the fibric soil material material #1 material #2 and humic layers in the profile. The fibric influence is largely determined by the thickness of the surficial layer of weakly Depth (cm) 0 - 60 60 - 120 > 120 decomposed (fibric) sphagnum material. Where fibric Von Post rating 1 - 4 5 - 8 - materials dominate the control section, the profile is classified as some form of Fibrisol, depending upon the significance and % Wood 10 10 - degree of decomposition of other layers present. The degree of decomposition of the underlying sedge-sphagnum material, 35

Texture Class - - Sandy clay into place in successive layers and compacted by the weight of loam glacier ice. It is a heterogeneous mixture of particle sizes ranging from silts and clays to stones and boulders. % Sand - - 60 Subsequent to this was the deposition of well sorted sandy % Silt - - 16 marine or marine reworked glaciofluvial sediments. These are weakly stratified sands, primarily medium to fine grained, but % Clay - - 24 with some fine gravels. The combined thickness of both materials is usually 1 to 3 m, with most soils being mapped as % Coarse - - 20 angular Fragments G/C blankets. Barrieau-Buctouche soils occupy level to gently undulating landforms. Surface expression conforms to the pH (H2O) < 4.5 < 4.5 4.5 configuration of the underlying bedrock. Most slopes are BD (g/cm3) < 0.10 0.15 1.90 between 0.5 and 3%. Steeper gradients are site specific or occur along stream and river valleys. Well to moderately well Ksat (cm/hr) 10 - 15 1.0 - < 0.1 0.1 drained sites support stands of black spruce and balsam fir with some jack pine and grey birch on the drier sites. Black spruce, AWHC (cm/cm) 0.10 0.20 < 0.10 balsam fir, cedar, red maple and some yellow birch are typical of ill-drained conditions.

The Barrieau-Buctouche association consists of well to Barrieau-Buctouche Association moderately well drained Orthic Humo-Ferric Podzols (Fig. 9), imperfectly drained Gleyed Humo-Ferric Podzols and Gleyed The Barrieau-Buctouche association is made up of soils that Eluviated Dystric Brunisols, and poorly to very poorly drained have developed in deposits consisting of acidic, sandy, marine Orthic Gleysols and Fera Gleysols. Although the B horizon in or marine modified glacial outwash sediments overlying well to imperfectly drained profiles appears morphologically acidic, compact, fine loamy, morainal till materials. It to be a Bf horizon, chemical analysis reveals that it just barely occupies the transition zone between Richibucto soils and exceeds the minimum requirements for sodium pyrophosphate Stony Brook-Reece soils. Mapping of these types of transition extractable Fe plus Al. Poorly drained soils lack the podzolic zones between material types is usually impossible at a scale B horizon. They have evidence of gleying that satisfies the of 1:250,000. In most instances they are ill-defined areas specifications of the Gleysolic order. Where hydrous iron along map unit boundaries. However, as a result of postglacial oxide has accumulated forming a Bgf horizon they are Fera marine submergence, significant areas of the lowland plain Gleysols, otherwise poorly to very poorly drained (Fig. 8) have a thin veneer (less than 1 m thick) of marine Barrieau-Buctouche soils are classified as Orthic Gleysols. sediments overlying the glacial till. Barrieau-Buctouche soils Internal drainage is impeded by the presence of the underlying are found at elevations of less than 50 m above sea level. They compact, very slowly permeable (less than 0.1 cm/hr) glacial occupy approximately 40,054 ha, or about 1.44% of the map till subsoil. Textural voids in the coarse textured sandy marine area. surface sediments are conducive to rapid flow rates of in excess of 15 cm/hr. This hydraulic discontinuity between the surface and subsoil promotes internal lateral flow, with downslope seepage of water. Perched water tables often result, with a saturated zone at and just immediately above the interface. Available water storage capacity is moderately low (less than 0.15 cm/cm) throughout the profile . With exception of the upper solum where slightly finer texture and the presence of organic matter enhance moisture retention, the coarser nature of the marine sand is not conducive to water storage. On the other hand the glacial till subsoil is low in available water storage capacity because of its limited total porosity. Well to moderately well drained Barrieau-Buctouche soils occupy crest and upper slope positions where precipitation is the sole source of water. Excess precipitation is laterally removed from the site as subsurface flow. Given similar topographic conditions, well drained sites usually occur where marine sediments are thicker (50 to 100 cm), and moderately well drained where thinner cappings are present (less than 50 cm). Imperfectly and poorly to very poorly Figure 8. Location of mapped Barrieau-Buctouche soils. drained sites are strongly influenced by inflow (seepage) from surrounding uplands. Prolonged saturation is due to both The underlying glacial till is basal or lodgment till, plastered perched and true groundwater tables. The undulating 36 configuration of the underlying till is conducive to localized interface of the two materials. The textural profile consists of perched water tables which are created by spring snowmelt and sandy loam to loamy sand marine sediments over loam to clay rejuvenated during the summer months by precipitation and loam or sandy clay loam glacial till material. The marine seepage. The association is dominated by imperfect drainage. sediments are usually relatively free of coarse fragments (less than 5%). Those coarse fragments that do occur are rounded gravels derived from soft, gray-green Pennsylvanian sandstone. The till materials have from 15 to 20% flat to subangular cobbles and gravels of similar sandstone lithology. Some remnant shale and siltstone chips are also present, but for the most part the original clasts have disintegrated and been incorporated into the soil matrix. Surface stones are insignificant. Barrieau-Buctouche soils are low in natural

fertility and acidic throughout, pH(H2O) 4.0 to 5.5. The solum is very friable, weak platy (Ae) or weak granular (B). Subsoil marine sediments are usually loose and structureless or single grain. The underlying till is firm to compact and pseudoplaty to weak medium subangular blocky or massive.

Barrieau-Buctouche soils have developed in two tiered deposits of marine sediments over glacial till. They are therefore intimately associated with soils that have developed on either of their component parts, i.e., Richibucto sandy marine soils, or Stony Brook and Reece fine loamy till soils. The Richibucto association lacks the underlying till component. The Stony Brook and Reece associations lack the surficial mantle of marine sediments. Tracadie marine clays and Guimond River glaciofluvial gravels are other water- deposited soils that have been mapped with Barrieau- Buctouche. Very poorly drained Barrieau-Buctouche soils have also been mapped with Lavillette organic soils and Salt Marsh land types.

In terms of land use and biological production, the outstanding features of the Barrieau-Buctouche association are the presence of the relatively coarse fragment free sandy marine veneer and the dense, compact, relatively impermeable nature of the underlying till which limits moisture movement and root penetration. Barrieau-Buctouche soils are also low in natural Figure 9. Well drained Barrieau-Buctouche soil profile. fertility. While natural or inherent fertility of the soil is to a large degree a function of soil mineralogy, it also relates to soil Soil formation averages 35 to 45 cm in depth. Depending nutrient retention. Coarser-textured soils that are low in clay upon thickness of the marine mantle, this development may be content tend to be more easily leached of nutrients than finer- confined to the marine sediments, or may affect both materials. textured soils. Forest production, which is dependent on In well to moderately well drained profiles the common natural fertility, is limited by these low levels of nutrients. horizon sequence is either : LFH, Ae, Bf, BC, C, and IIC ; or LFH, Ae, Bf, IIBC, and IIC. The profile is typically podzolic Summary of general characteristics of the Barrieau-Buctouche Association in appearance with a thin LFH layer over an ash coloured Map Symbol : BB eluvial A horizon that has an abrupt lower boundary to a Physiographic Region(s) : Maritime Plain reddish brown to yellowish brown Bf. Where present the C Elevation : <50 m horizon is yellowish brown to brown. The underlying IIC Extent : 40,054 ha horizon is either yellowish brown to brown, or red to reddish Percentage of Mapped Area : 1.44% Parent Material Type : Mineral brown. Imperfectly drained sites are not always podzols and so Mode of Origin : Marine or outwash over compact glacial there may be either a Bfgj or Bmgj horizon. There is also till usually a thin leached horizon, Aegj, immediately above the Material Thickness : 1-3 m second material. This layer is the result of lateral leaching. Soil Colour : Yellowish brown to brown over yellowish brown to reddish brown Poorly drained profiles consist of LFH or O , Aeg, Bg or Bgf Family Particle Size Class : Sandy over loamy and II Cg horizons. The surface organic layer is usually Petrology (parent material) : Grey-green sandstone over grey-green thicker and strong mottling and/or gleying occurs along the sandstone plus red shale 37

Inherent Fertility : Low Topography (slope) : Level to undulating (0-3%) Drainage (dominant) : Imperfect Classification (typical) : Gleyed Humo-Ferric Podzol

Layer Friable upper Subsoil Subsoil soil material material #1 material #2

Depth (cm) 0 - 40 40 - 65 65 - 100+

Texture Class Loamy sand Sand Sandy clay loam

% Sand 85 93 53

% Silt 8 4 25

% Clay 7 3 22

% Coarse 0 5 rounded G 20 subangular Fragments G/C

pH (H2O) 4.5 - 5.0 5.0 5.0 - 5.5

BD (g/cm3) 1.15 1.40 1.90 Figure 10. Location of mapped Belledune River soils.

Ksat (cm/hr) 45 50 0.1

AWHC < 0.15 0.10 < 0.10 Well drained Belledune River association soils are Orthic (cm/cm) Humo-Ferric Podzols (Fig. 11). Podzolization is strongly expressed, even in sites that are less than well drained. Imperfectly drained sites are Gleyed Humo-Ferric Podzols. Poorly drained sites are Orthic Gleysols or Fera Gleysols. Belledune River Association Internal drainage is good . The profile consists of a moderately rapidly permeable solum over a moderately permeable subsoil. The Belledune River association consists of soils developed in Saturated hydraulic conductivity values are greater than 2.5 moderately thick (greater than 2 m) deposits of strong to cm/hr throughout the profile and greater than 5 cm/hr in the medium acidic, coarse loamy to sandy skeletal, non-compact, solum. Available water storage capacity ranges from 0.20 to marine sediments with coarse fragments of conglomerate, 0.10 cm/cm, the higher values being in the solum where finer sandstone, siltstone and some argillite and limestone. textures and organic matter contents enhance moisture Belledune River soils occur only on the lowlands portion of the retention. Precipitation is the sole source of water supply on New Brunswick Highlands adjacent to Chaleur Bay (Fig. 10). well drained sites. Excess water flows downward into the They are situated at elevations of less than to 50 m above sea underlying subsoil. Imperfectly and poorly drained sites are level. Belledune River marine sediments are underlain by the results of high groundwater tables. either glacial till, or lie directly on the bedrock. Belledune River soils occupy approximately 27,854 ha or 1.00% of the Solum development in Belledune River soils varies from 35 to map area. 55 cm in thickness. The common horizon sequence is: LFH, Ae, Bf, BC and C on well to moderately well drained sites; Belledune River soil parent materials are marine depositions LFH, Ae, Bfgj, BCgj or BCg and Cg on imperfectly drained dominated by sand and silt. They were deposited in a brackish, sites; and LFH or O, Aeg, Bg or Bgf and Cg on poorly or very shallow water environment during postglacial marine poorly drained sites. Although Belledune River soils have submergence and subsequently exposed when water levels formed in marine sediments, soil forming processes have receded. Most land surfaces are gently undulating, with slopes obliterated any evidence of material stratification in the solum. of 2 to 5%. Belledune River material consists of weakly Soil textures grade from a sandy loam to loam or silt loam stratified marine sediments with coarse fragments and soil solum into a sandy loam to loamy sand subsoil. Coarse particles poorly sorted according to size or weight. Because of fragment content ranges from 15 to 50%. Coarse fragments this, they are frequently referred to as being “dirty” sand and are mostly subrounded to rounded gravels with some cobbles. gravel deposits. Belledune River soils may have enough They are derived from conglomerate, sandstone, siltstone and scattered surface stones to be a slight hindrance to cultivation. some argillite and limestone. These rock types result in a soil Forest vegetative cover consists of species such as black that is moderately fertile. The profile is acidic throughout, spruce, cedar, tamarack, red maple, trembling aspen and alder. ranging from a pH(H2O) of 5.0 to 6.0 . The parent material is reddish to dark brown. The mineral soil profile consists of a 38 pinkish gray, friable, weak, fine platy Ae horizon over a strong Summary of general characteristics of the Belledune River Association brown, very friable, weak to moderate, fine granular Bf Map Symbol : BR horizon which merges gradually into the friable, very weak, Physiographic Region(s) : Chaleur Uplands subangular blocky BC and then C. Mottles and grayish gley Elevation : <50 m colours modify the profile morphology in imperfectly and Extent : 27,854 ha poorly drained sites. Only under the very wettest of conditions Percentage of Mapped Area : 1.00% Parent Material Type : Mineral is the general podzolic sequence not present. Mode of Origin : Marine Material Thickness : > 2 m Soil Colour : Reddish brown to yellowish brown Family Particle Size Class : Coarse loamy to sandy Petrology (parent material) : Conglomerate, sandstone siltstone, argillite and some limestone Inherent Fertility : Medium Topography (slope) : Undulating (2-5%) Drainage (dominant) : Imperfect Classification (typical) : Gleyed Humo-Ferric Podzol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 45 45 - 100+

Texture Class Sandy loam, loam, Sandy loam to loamy silt loam sand

% Sand 55 60

% Silt 28 30

% Clay 17 10

% Coarse 20 rounded G 50 rounded G/C Fragments

pH (H2O) 5.0 5.5

BD (g/cm3) 1.30 1.55

Ksat (cm/hr) 10 2.5

AWHC (cm/cm) 0.20 0.10

Figure 11. Well drained Belledune River soil profile. Big Bald Mountain Association

Belledune River association soils are often associated with The Big Bald Mountain association consists of soils that have other water deposited materials - Tracadie and Gagetown. developed in thin veneers of acidic, sandy skeletal residual Tracadie soils have developed in coarse fragment-free clayey material that has weathered in place from the consolidated marine sediments and are readily differentiated from Belledune granite bedrock on which it lies. Big Bald Mountain soils were River soils. Gagetown soils have developed in yellowish first mapped in the vicinity of Big Bald Mountain in the brown glaciofluvial gravels. Central Highlands physiographic region (Fig. 12). They are also found in other areas of the Central Highlands where Good internal drainage, adequate water and nutrient holding granitic bedrock occurs. Big Bald Mountain soils are mapped capacities in the surface soil and medium natural fertility make at elevations of 400 to 600 m above sea level, and cover Belledune River soils productive for both agricultural and approximately 15,394 ha, or about 0.55% of the map area. forestry crops. The major limitation to land use is the predominance of imperfectly and poorly drained conditions. Big Bald Mountain soils are considered to have develop in situ However, with moderate permeability in the subsoil, Belledune from the underlying feldspar rich granitic bedrock. Physical River soils should be very responsive to tile drainage. Natural and chemical transformations have taken place in the surface drainage conditions will be more of a limitation to forestry of the parent bedrock which has disintegrated and decomposed crops. into rock fragments and soil debris. This type of accumulation 39

glaciers. The landforms have a strongly rolling to hilly surface expression dominated by moderate to very strong slopes of 9 to 45%. Vegetation consists mainly of stunted, scattered jackpine and spruce. Wild blueberry, interspersed with other ericaceous shrubs, is the dominant ground cover.

The Big Bald Mountain association is dominated by well to rapidly drained Orthic Humo-Ferric Podzols (Fig. 14). The profile consists of a bleached ashy Ae horizon followed by a dark to strong brown B horizon in which both colour value and chroma decrease with increase in depth. The C horizon is dark yellowish brown. Imperfectly to somewhat poorly drained sites occur as inclusions. They consist of Gleyed Humo-Ferric Podzols.

Figure 12. Location of mapped Big Bald Mountain soils. of angular coarse-grained fragments resulting from the granular disintegration of granite (and other crystalline rocks) is referred to as "grus". The granite bedrock of the Big Bald Mountain association is estimated to consist of 40% potassium feldspar, 25% plagioclase, 30% quartz and 5% biotite, chloride and hornblende. Weathered bedrock or grus is usually less than 1 m thick, except for the soils at the foot of slopes which are deeper. Tors, peculiarly shaped isolated rock masses or pinnacles, are present on some summits (Fig. 13). They are deeply weathered, with rings 1 to 2 m wide, of colluvial grus accumulating around their bases. Figure 14. Well drained Big Bald Mountain soil profile.

Precipitation is the sole source of water on well to rapidly drained sites. The soils have a high infiltration capacity and excess water flows downward rapidly through the porous profile at an estimated rate of 10 cm/hr or greater. The bedrock, which becomes more consolidated with depth, impedes downward flow to some degree, causing horizontal water flow under conditions of extreme rainfall or rapid snowmelt. Available water storage capacity is estimated to be less than 0.15 cm/cm in the solum and less than 0.10 cm/cm in the C horizon. Increased capacity to retain moisture in the solum is attributed to its higher clay and organic matter contents and lower coarse fragment content than the patent material. Moisture deficits on Big Bald Mountain soils influence forest fire patterns, encouraging repeated burnings, thus determining the vegetative cover type. Imperfectly to Figure 13. Big Bald Mountain soil association landscape somewhat poorly drained sites occupy depressions and showing “tors”. drainage channels in lower site positions. They are supplied with water by groundwater flow and seepage (along the Gibbsite, considered to be the end product of the weathering soil-bedrock interface) from adjacent uplands. sequence of soil minerals, has been found in Big Bald Mountain soil parent material. The presence of tors and Soil development averages 30 to 45 cm in depth. The common gibbsite coupled with a general lack of evidence of glacial horizon sequence consists of: Om, Ae, Bf, BC, C, and R. A activity prompted Wang et. al. (1981) to conclude that these weakly developed ortstein layer may occur in the Bf horizon. soils and landforms are of pre-Wisconsin or even Ortstein is an irreversible hardpan that is bonded by Fe, Al and pre-Pleistocene age. It is hypotheorized that the area was organic matter complexes. It is discontinuous, occurring in frozen, protected by ice, and consequently undisturbed by the less than 20% of the soil associations horizontal extent. Profile 40 texture is sandy loam to loamy sand. Clay content seldom Layer Friable upper soil Subsoil material Bedrock exceeds 10%. Coarse fragment content increases with depth material from 10 to 20% in the solum to in excess of 60% in the parent material C horizon). Most coarse fragments are angular fine Depth (cm) 0 - 35 35 - 70 > 70 gravels but the occasional cobble or stone sized fragment of Texture Sandy loam Loamy sand - consolidated bedrock is also found in the profile. The land Class surface is slightly to moderately stony where differential frost heaving has brought bedrock fragments to the soil surface. All % Sand 70 85 - coarse fragments have been derived from the underlying % Silt 23 7 - granitic bedrock. Bedrock exposures and areas of very thin soil (less than 10 cm thick) cover up to 25% of the land surface % Clay 7 8 - of some map polygons. They are scattered patches on crest % Coarse 15 angular G 50 angular G/C - and upper slope positions. Big Bald Mountain soils are very Fragments low in natural fertility and acidic, pH (H2O) of 4.5 to 5.5, pH (H O) 4.5 5.0 - throughout. The soil is very friable to friable, very weak, fine 2 to coarse, subangular blocky in the solum, and firm, pseudo BD (g/cm3) 1.10 1.45 - platy in the C horizon. Much of the original bedrock structure is retained in the profile, becoming more pronounced with Ksat (cm/hr) > 10 10 - depth. Where patches of ortstein occur the Bf horizon is firm AWHC < 0.15 < 0.10 - and massive. (cm/cm)

Juniper is the soil most commonly mapped in association with Big Bald Mountain. Juniper is coarse loamy to sandy and is derived from primarily granitic sources. Its till mode of Boston Brook Association deposition, however, makes it easy to separate the two soils. Juniper soils are a heterogeneous mixture of glacial debris The Boston Brook association consists of soils that have ranging from silts and clays to boulders. Lithologically they developed in acidic, fine loamy, noncompact morainal till are also more diverse with diorites, granodiorites, granite derived from argillites, slates and fine-grained sandstones. gneiss, volcanics and miscellaneous sedimentary and Deposits range from less than 1 m thick (veneers) to in excess metamorphic coarse fragments in addition to the feldspar rich of 3 m. Boston Brook soils occur in the Chaleur Uplands granites. Big Bald Mountain is also found adjacent to units of portion of the study area (Fig. 15) at elevations between 300 Long Lake and McGee soils, both of which are glacial till and 500 m above sea level. They occupy approximately 2,877 soils. The Long Lake and McGee associations have distinctly ha, representing some 0.10% of the map area. different lithological origins, having been derived from argillaceous sedimentary and metamorphic rock types such as Boston Brook soil parent material is an ablational till, and as shale, argillite, slate, greywacke and quartzite. such is typically noncompact, however, some firmness may occur in the subsoil. The somewhat firm consistence of the Big Bald Mountain soils are shallow to bedrock and very low subsoil can be attributed to the composition of the parent in natural fertility and available moisture storage capacity. material in that it is fine loamy and acidic. The acidic nature These limitations coupled with adverse topographic conditions, of the subsoil does not promote soil forming physical and ie. excess slope, and a harsh climate, make Big Bald Mountain biochemical processes that favour the development and soils unsuitable for agriculture. These factors also limit the stabilization of soil structure. soils potential for forestry. Boston Brook soils consist of fine loamy sediments with Summary of general characteristics of the Big Bald Mountain Association subangular and flat to subrounded coarse fragments derived Map Symbol : BM from the underlying slate, argillite, sandstone or quartzite Physiographic Region(s) : N. B. Highlands bedrock. Surface stoniness ranges from moderate to very Elevation : 400-600 m stony, with up to 15% of the land surface occupied by coarse Extent : 15,394 ha fragments in some cases. Well drained Boston Brook soils Percentage of Mapped Area : 0.55% Parent Material Type : Mineral have developed under a mixed hardwood-softwood forest Mode of Origin : Residual cover type consisting of yellow birch, cedar, spruce, balsam Material Thickness : < 1 m fir, sugar maple, beech, white birch, white pine, red oak and Soil Colour : Yellowish brown striped maple. Poorly to very poorly drained members are Family Particle Size Class : Sandy skeletal Petrology (parent material) : Granite dominated by cedar, black spruce, balsam fir, white birch, red Inherent Fertility : Very low maple, speckled alder and willows. Topography (slope) : Strongly rolling to hilly (9-45%) Drainage (dominant) : Well Classification (typical) : Orthic Humo-Ferric Podzol 41

brownish gray coloured Ae horizon which breaks abruptly into the B horizon. A thin brown to dark brown Bhf horizon varies from 3 to 8 cm in thickness. The Bhf horizon merges with a yellowish brown Bf horizon which gradually grades into the oxidized light olive brown parent material. At 30 to 40 cm the podzolic B horizon grades into a BC horizon which grades into the unaltered parent material or C horizon. Imperfectly drained soils have similar profile horizons but are modified by periodic saturation. They are mottled in the B and C horizons. Poorly to very poorly drained horizon sequences typically consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The forest duff layer is thicker in poorly and very poorly drained conditions than found in well drained counterparts, varying from 5 to 15 cm, but occasionally as thick as 30 cm. The Boston Brook textural profile consists of a loam to clay loam, usually increasing in clay content with depth and also as drainage becomes poorer. Profile coarse fragment content varies from 10 to 30%, with a preponderance of subangular to somewhat subrounded gravels and cobbles. Boston Brook soils are medium in inherent fertility and acidic throughout,

Figure 15. Location of mapped Boston Brook soils. with pH(H2O) values of 4.0 to 5.5. A friable to very friable, weak to moderate, fine to medium, granular or subangular blocky solum overlies a slightly firm weak, medium The Boston Brook association is dominated by well to subangular blocky subsoil. moderately well drained Orthic Humo-Ferric Podzols. Imperfectly drained sites are classified as Gleyed Humo-Ferric Boston Brook soils are associated with soils of the Caribou, Podzols, indicating varying oxidizing/reducing conditions due Holmesville and Violette associations., and occasionally with to periodic saturation. Poorly to very poorly drained sites are the Tetagouche and Tetagouche Falls associations The typically Orthic Gleysols but may have some inclusions of Caribou association is differentiated from Boston Brook on the Fera Gleysols. Imperfect and poorly to very poorly drained basis of subsoil reaction. Boston Brook parent materials are sites occur along drainage channels and in depressions in areas acidic while Caribou parent materials are near neutral. Coarse dominated by moderately well drained soils, or more fragment lithologies also differ between the two soils, extensively in areas that are level or only gently undulating. however, in many other features they are similar owing to their Boston Brook soils have moderate to somewhat slow internal both having developed on fine loamy noncompact till drainage. The upper solum usually has moderate permeability materials. Boston Brook is differentiated from Holmesville (approximately 5 cm/hr saturated hydraulic conductivity), but and Violette on the basis of subsoil compaction. Boston Brook the subsoil only has moderately slow permeability (0.5 to 2.0 soils are only somewhat compact in the subsoil while both cm/hr). Available moisture storage capacity exceeds 0.20 Holmesville and Violette soils are strongly compacted, cm/cm throughout the profile with highest levels in the upper especially Violette soils. Holmesville soils have coarser solum. Decreased pore size in the lower solum reduces the textured subsoils than Boston Brook soils. Violette soils have availability of retained moisture. In well to moderately well similar fine loamy subsoils, and near identical lithologies, drained sites precipitation is the dominant source of water. making their separation from Boston Brook soils one of Lateral flow or seepage is not a problem, occurring only on subsoil compaction. very steeply sloping landscapes where bedrock restricts vertical flow, or when water inputs due to either precipitation The Boston Brook association is considered marginally or snowmelt exceed the subsoil permeability. Poorly to very suitable for agriculture in its existing state. The major poorly drained sites occur because of high groundwater levels limitation to agricultural development is coarse fragment and to a lesser extent because of the inflow of seepage from content. Stones and cobbles may impede agricultural adjacent uplands, or both. The underlying bedrock is acidic production, but when overcome, Boston Brook soils should be and so seepage waters are not exceptionally rich in nutrients, moderately suitable for most crops. They have good nutrient although still somewhat beneficial to plant growth. and water holding capacities and the subsoil is not typically a structural limitation. From a forestry perspective these soils Soil development is relatively thin, with solums ranging from are capable of supporting a wide range of commercial species 35 to 55 cm. The common horizon sequence on well drained since they are moderate in natural fertility. sites is LFH, Ae, Bhf, Bf, BC and C. O horizons may occur under coniferous forests where mosses dominate the ground Summary of general characteristics of the Boston Brook Association vegetation. The organic layer is 3 to 10 cm thick, becoming Map Symbol : BO more humified with depth. It overlies a thin (2 to 5 cm), light Physiographic Region(s) : Chaleur Uplands 42

Elevation : 300-500 m 9%, but slopes of 15 to 45% may occur along stream channels Extent : 2,877 ha that are deeply incised into the bedrock. Landform surface Percentage of Mapped Area : 0.10% Parent Material Type : Mineral expressions are more characteristic and indicative of a basal till Mode of Origin : Glacial till, noncompact mode of deposition. This is further corroborated by the Material Thickness : < 3 m localized nature of the till debris. Most of the soil parent Soil Colour : Olive to olive brown material has been derived from the bedrock upon which it is Family Particle Size Class : Fine loamy Petrology (parent material) : Argillite, slate and fine-grained sandstone presently resting, with only minimal displacement. Similarity Inherent Fertility : Medium to the underlying bedrock often makes it difficult to determine Topography (slope) : Undulating to hilly or ridged (2-70%) if the subsoil is till or residual (weathered in situ) material. Drainage (dominant) : Well to moderately well The friable to only somewhat firm consistence of the subsoil Classification (typical) : Orthic Humo-Ferric Podzol may be attributed to the composition of the parent material. The presence of available bases (ie. calcium from the calcitic bedrock debris) promotes physical and biochemical processes Layer Friable upper soil Subsoil material in soil formation that favour the development and stabilization material of soil structure.

Depth (cm) 0 - 45 45 - 100+

Texture Class Loam Clay loam

% Sand 35 30

% Silt 40 39

% Clay 25 31

% Coarse 15 subangular G/C 25 subangualar G/C Fragments

pH (H2O) 4.5 - 5.0 5.0 - 5.5

BD (g/cm3) 1.30 1.60

Ksat (cm/hr) 5 0.5 - 2

AWHC (cm/cm) >.20 0.20

Figure 16. Location of mapped Caribou soils. Caribou Association Regardless of mode of deposition, the physical and chemical attributes of Caribou soils are quite uniform. They consist of The Caribou association consists of soils that have developed noncompact, fine loamy sediments with sharp, angular, flat in neutral to weakly calcareous, fine loamy, noncompact coarse fragments derived from the underlying weakly morainal till derived from calcareous shale, argillite and slate, calcareous shale-slate. Surface stoniness ranges from slightly and occasionally some limestone. Deposits range from less to moderately stony, with less than 3% of the land surface than 1 m thick (veneers) to some deposits in excess of 3 m occupied by coarse fragments. Well drained Caribou soils have thick. The transition from regolith to bedrock may be gradual, developed under a mixed hardwood-softwood forest cover type with some in situ weathering of the underlying vertically consisting of red and sugar maple, beech, white birch, dipping calcitic shale (slate) bedrock. Caribou soils occur in mountain ash, red oak, trembling aspen, white pine, balsam fir the Chaleur Uplands portion of the study area (Fig. 16) at and black and white spruce. Poorly to very poorly drained elevations between 300 and 500 m above sea level. They members are dominated by black spruce, balsam fir, white occupy approximately 82,212 ha, representing some 2.95% cedar, tamarack, red maple, trembling aspen, black ash, and of the map area. speckled alder. Caribou soil parent material is noncompact, and as such has The Caribou association is dominated by well to moderately been considered to be ablational till. However, it is quite well drained Podzolic Gray Luvisols and Luvisolic conceivable that much of the material was in fact deposited as Humo-Ferric Podzols. This represents bisequal soil basal till, laid down below the glacier as it advanced. This horizonation ie. two sequences of an eluvial horizon and its hypothesis is substantiated by several conditions. Most related illuvial horizon. The upper sequence of horizons is Caribou soils occur on the gently rolling to undulating plateau typical of a podzol with development of a Bf horizon. The between St. Quentin and the Restigouche River. They lower sequence of horizons is typical of a luvisol, with a commonly occupy ridges with broad tops and slopes of 3 to distinct increase in clay content forming a Bt horizon. Depth 43 to the Bt horizon determines whether the soil is classified as Luvisolic or Podzolic. During soil formation acid leaching removed free carbonates from the upper solum. Wetting and drying cycles then lead to the dispersal of the very fine clay component which was translocated with the downward movement of water. Carbonates in the lower profile caused the clays to flocculate, thus accumulating into a Bt horizon. Thin to moderately thick clay films are present in voids and root channels and on most vertical and horizontal ped faces. Imperfectly drained sites are classified as either Gleyed Podzolic Gray Luvisols or Gleyed Brunisolic Gray Luvisols, indicating weaker soil development than is found in the well to moderately well drained sites. Poorly to very poorly drained sites are Orthic Luvic Gleysols and Orthic Humic Gleysols. They usually occur along drainage channels and in depressions as predictable inclusions in areas dominated by well to moderately well drained soils. Caribou soils have moderate internal drainage. Based on pore size distribution, the upper solum is estimated to have a moderate to moderately rapid permeability (2.5 to 10 cm/hr saturated hydraulic conductivity) and the lower solum (Bt horizon) and subsoil moderately slow permeability (0.5 to 2.0 cm/hr). Available moisture storage capacity exceeds 0.20 cm/cm throughout the profile. In well to moderately well drained sites precipitation is the dominant source of water. Rainfall exceeds evaporation resulting in excess water which flows downward through the profile. Lateral flow occurs only on very steep gradients during periods of extreme wetness (spring snowmelt, heavy rainfall, etc.). Poorly to very poorly drained sites occur because of high groundwater levels and to a lesser extent because of inflow of seepage from adjacent uplands, or both. The underlying bedrock is a vertically standing weathered shale-slate (Fig.17) Figure 17. Well drained Caribou soil profile, veneer phase. that accommodates some downward movement of water. where the dominant features are the thick Ah and lack of clay Soil development is quite thick, with solums ranging from 60 migration; or some combination of the two sequences. The to in excess of 100 cm. This greater than normal thickness of Caribou textural profile consists of a silt loam to loam upper solum development can be attributed to the illuviation of clay. solum that grades into a clay loam to silty clay loam in the Bt Profile development is greatest in the well to moderately well and C horizons. The clay content peaks in the Bt horizon. drained sites. The common horizon sequence is LFH, Ah, Ae1, Clay mineralogy of the podzolic portion of the profile is Bf, Ae2, Bt and C. The Ae1 horizon is usually thin and often dominated by vermiculite. Mica dominates the Bt and C discontinuous. Faunal activity has created a moder-mull type horizons (Arno et. al ca 1964). Percent silt plus clay averages of forest humus form that may reach depths of 5 to 10 cm, at 60 to 75%. Poorly drained depression sites have heavier the expense of the LFH and Ae horizons. However, conditions textures because of inwashed fines from seepage and overland also exist in which the Ah horizon may be almost completely flow. Coarse fragment content within the profile averages 10 absent. The organic rich Ah is dark brown to black while the to 30%, usually increasing with depth. Lithic or veneer phases Ae horizon is white to light grey. The Bf horizon is may have increased coarse fragment contents especially characteristically strong brown to brownish yellow, becoming nearing the bedrock interface. The rock fragments are flat, paler with depth. Parent material colours range from olive to angular gravels (channers) of soft weathered shale-slate olive brown. Imperfectly drained Caribou soils have similar derived from the underlying calcitic bedrock. Most fragments horizonation to their well drained counterparts. The major are completely leached of carbonates, especially in the upper difference morphologically is the presence of mottles and gley profile. The soil parent material has been derived from rock features due to periodic reducing conditions. Chemically, Fe types that weather rapidly and are moderately rich in bases. and Al accumulation in the upper B horizon is less than in the Inherent fertility is therefore high in comparison to other soil well drained member. The upper B horizon in imperfectly associations but at the same time "wanting" because of natural drained soils ranges from a Bf to a Bm (or Bfj). In poorly to leaching due to rainfall. From an agricultural perspective very poorly drained profiles the common horizon sequence is nutrient retention is good. There is a gradual increase in soil either LFH or O, Aeg, Btg and Cg where there is a significant reaction down the profile. The upper solum is acidic while the amount of clay translocation; or, LFH or O, Ah, Bg and Cg lower solum is neutral grading into a weakly calcareous parent 44 material between 1 and 2 m from the mineral soil surface. Summary of general characteristics of the Caribou Association Shallow to bedrock phases are acidic throughout. Sites that Map Symbol : CB receive seepage are often enhanced with soluble bases that Physiographic Region(s) : Chaleur Uplands have been leached from adjacent upland soils and bedrock Elevation : 300-500 m formations. Impeded drainage also results in less acid Extent : 82,212 ha leaching. For this reason depressions are often higher in Percentage of Mapped Area : 2.95% Parent Material Type : Mineral exchangeable bases (more nutrient rich) and thus have a higher Mode of Origin : Glacial till, noncompact pH. Caribou soils are characterized by their noncompactness Material Thickness : < 3 m and well developed structures. The upper solum is usually Soil Colour : Olive to olive brown friable to very friable, moderate to strong, medium, granular. Family Particle Size Class : Fine loamy Petrology (parent material) : Calcareous shale, argillite, slate and some The Bt is friable to slightly firm with a moderate, medium, limestone subangular blocky structure. The subsoil is somewhat firm in Inherent Fertility : High situ but is very friable when removed. Topography (slope) : Undulating and rolling to hilly or sloping (3-45%) Drainage (dominant) : Well to moderately well Caribou soils are primarily associated with soils of the Classification (typical) : Podzolic Gray Luvisol Carleton and Thibault associations, and to a lesser degree with the Boston Brook, Violette and Holmesville associations. Caribou, Carleton and Thibault soils have all developed on parent materials derived from calcareous to weakly calcareous Layer Friable upper soil Subsoil material rock types. Thibault soils are coarser-textured and often material referred to as "the coarse loamy phase of the Caribou Depth (cm) 0 - 50 50 - 100+ association". However, while well drained Caribou soils have bisequal profile development with podzolic features over Texture Class Silt loam Clay loam luvisolic features, Thibault association soils lack any sign of % Sand 30 35 luvisolic features. The Carleton association is similar to the Caribou association in that both soils are fine loamy and have % Silt 45 33 developed from parent materials derived from the same lithological rock types. They differ in subsoil compaction. % Clay 25 32 Carleton soils are compact, Caribou soils are non-compact. In % Coarse 10 flat/angular G 25 flat/angular G some instances where the subsoils are only weakly compact, Fragments separation of these two associations may be difficult. The pH (H O) 5.3 6.0 - 7.0+ Caribou association is differentiated from the Boston Brook, 2 Violette and Holmesville soils on the basis of coarse fragment BD (g/cm3) 1.20 1.55 lithology, particle size class, reaction, and/or subsoil consistence. Caribou is derived almost completely from Ksat (cm/hr) 2.5 - 10 0.5 - 2 calcareous shale-argillite-slate. Boston Brook, Violette and AWHC (cm/cm) 0.25 0.20 Holmesville are derived from acidic lithological rock types such as quartzite, sandstone, argillite and slate. Both Holmesville and Violette have developed on lodgment tills and as such have dense compact subsoils. Holmesville soils are Carleton Association also coarse loamy in comparison to the fine loamy Caribou. Like Caribou soils, Boston Brook soils are fine loamy and non- The Carleton association consists of soils that have developed compact in the subsoil. But Boston Brook soils have more in neutral to weakly calcareous, fine loamy, compact morainal angular cobble-sized coarse fragments, the coarse fragments till derived from calcareous shale, argillite and slate, and are of acidic metasedimentary rock types, the subsoil pH is occasionally some limestone. Deposits are typically less than more acidic and the subsoil consistence is more firm (compact) 2 m thick (veneers and blankets) over bedrock. In veneer and less structured. phases, the transition from regolith to bedrock may be gradual, with some in situ weathering of the underlying calcareous The Caribou association is considered highly suitable for bedrock. Carleton soils occur mostly in the Chaleur Uplands agriculture where surface relief is sufficient for external portion of the study area (Fig. 18) at elevations between 300 drainage, but not excessively steep. The soil has a deep (50 cm and 500 m above sea level. They occupy approximately plus) available rooting zone with excellent nutrient and water 85,211 ha, representing some 3.06% of the map area. retention capacities. The soils are easily worked and retain most of their structural integrity. From a forestry perspective Carleton soil parent material is compact, and as such has been these soils are capable of supporting a wide range of considered to be a lodgment or basal till, laid down below the commercial species. They are comparatively high in natural glacier as it advanced. Most of the soil parent material has fertility. been derived from the bedrock upon which it is presently resting, with only minimal displacement. While the subsoil is 45 considered to be firm, it is not excessively so. The firm to fine clay component which was translocated with the somewhat friable subsoil consistence is attributed to the downward movement of water. Carbonates in the lower composition of the parent material. It is gravelly, which tends profile caused the clays to flocculate, thus accumulating into a to reduce its compatibility and it is also higher in pH. The Bt horizon. Thin to moderately thick clay films are present in presence of available bases (ie. calcium from the calcareous- voids and root channels and on most vertical and horizontal rich bedrock debris) promotes physical and biochemical soil ped faces. Imperfectly drained sites are classified as gleyed forming processes that favour the development and variants of their well-drained counterparts, Gleyed Podzolic stabilization of soil structure. Gray Luvisols and Gleyed Humo-Ferric Podzols. They may also be Gleyed Brunisolic Gray Luvisols, indicating weaker soil development than is found in the well to moderately well drained sites. Poorly to very poorly drained sites are Orthic Luvic Gleysols and Orthic Gleysols. They usually occur along drainage channels and in depressions, interspersed in areas dominated by well to moderately well drained soils. Carleton soils have slow internal drainage. The upper solum is estimated to have moderate to moderately rapid permeability (2.5 to 10 cm/hr saturated hydraulic conductivity), but the lower solum (Bt horizon) and subsoil have slow permeability (0.1 to 0.5 cm/hr). Available moisture storage capacity ranges from 0.25 cm/cm in the upper solum to less than 0.15 cm/cm in the subsoil. The subsoils are dense and compact, but not excessively so. Bulk densities of 1.70 to 1.80 g/cm3 are common. In well to moderately well drained sites precipitation is the dominant source of water. Downward movement of excess moisture through the profile is impeded by the subsoil. Lateral flow or seepage is common, especially on sloping topography after heavy rains or following snowmelt. Imperfectly and poorly to very poorly drained areas have Figure 18. Location of mapped Carleton soils. developed because of a combination of topographic position, lack of gradient, subsoil compaction, seepage and high Carleton soils consist of compact, fine loamy sediments with groundwater table. an abundance of gravel-sized subangular and subrounded to sharp, angular, flat coarse fragments derived from the Soil development is quite thick, with solums ranging from 60 underlying weakly calcareous bedrock. Surface stoniness to in excess of 80 cm. This greater than normal thickness of ranges from slightly to moderately stony, with less than 3% of solum development can be attributed to the illuviation of clay. the land surface occupied by coarse fragments. Well drained Profile development is greatest in the well to moderately well Carleton soils have developed under a mixed drained sites. The common horizon sequence is LFH, Ah, Ae1, hardwood-softwood forest cover type consisting of red and Bf, Ae2, Bt and C. The Ae1 horizon is usually thin and often sugar maple, beech, birch, mountain ash, red oak, trembling discontinuous. Faunal activity has created a moder-mull type aspen, white pine, balsam fir and black and white spruce. of forest humus form that may reach depths of 5 to 10 cm, at Poorly to very poorly drained members are dominated by the expense of the LFH and Ae horizons. However, conditions black spruce, balsam fir, white cedar, tamarack, red maple, also exist in which the Ah horizon may be almost completely trembling aspen, black ash, and speckled alder. absent. The organic rich Ah is dark brown to black while the Ae horizon is white to light grey. The Bf horizon is The Carleton association is dominated by well to moderately characteristically strong brown to brownish yellow, becoming well drained Podzolic Gray Luvisols (Fig. 19) and Luvisolic paler with depth. Where clay translocation is weakly Humo-Ferric Podzols, but with some Orthic Humo-Ferric expressed, the Bt horizon may not be present. The transition Podzols. The Podzolic Luvisols and the Luvisolic Podzols have to parent material is then designated as a BC horizon. Parent overlying sequences of eluvial/illuvial horizons. The upper material colours range from olive to olive brown. Imperfectly sequence of horizons is typical of a podzol with development drained Carleton soils have similar horizonation to their well of a Bf horizon. The lower sequence of horizons is typical of drained counterparts. The major differences morphologically a luvisol, with a distinct increase in clay content forming a Bt are the presence of mottles and gley features due to periodic horizon. Depth to the Bt horizon determines whether the soil reducing conditions. Chemically, Fe and Al accumulation in is classified as a Luvisolic or Podzolic intergrade, and where the upper B horizon is less than in the well drained member. Bt horizon formation is weak (more acidic sites), the profile is The upper B horizon in imperfectly drained soils ranges from classified solely as a Podzol. During soil formation acid a Bf to a Bm (or Bfj). In poorly to very poorly drained profiles leaching removed free carbonates from the upper solum. the common horizon sequence is either LFH or O, Aeg, Btg Wetting and drying cycles then lead to the dispersal of the very and Cg where there is a significant amount of clay 46 translocation; or, LFH or O, Ah, Aeg, Bg and Cg where clay and slate while the Carleton association soils have been migration is less pronounced. The Carleton textural profile derived from calcareous-rich rock types. Holmesville is coarse consists of a loam to silt loam upper solum that grades into a loamy in comparison to the fine loamy Carleton, but Violette loam to clay loam or silty clay loam in the Bt and C horizons. is similarly fine loamy in composition and as such very similar The clay content peaks in the Bt horizon. Poorly drained to the Carleton soil. In addition to different lithologies, subsoil depressional sites have heavier textures because of inwashed reaction and density are also used to separate the two fines from seepage and overland flow. Coarse fragment associations. Violette is acidic and more compact in the content within the profile averages 10 to 30%, usually subsoil than Carleton. Violette also has more cobble-sized increasing in abundance with depth. Lithic or veneer phases subangular coarse fragments throughout the profile. may have increased coarse fragment contents especially nearing the bedrock interface. Most fragments are completely leached of carbonates, especially in the upper profile. The soil parent material has been derived from rock types that weather rapidly and are moderately rich in bases. Inherent fertility is therefore high in comparison to other soil associations but at the same time subjected to natural leaching due to rainfall. From an agricultural perspective nutrient retention is good. There is a gradual increase in soil reaction with depth. The upper solum is acidic while the lower solum is neutral grading into a weakly calcareous parent material between 1 and 2 m from the mineral soil surface. Shallow to bedrock phases are acidic throughout. “There are slight variations in texture, pH and degree of leaching in the Carleton association. The degree of leaching usually increases and the pH decreases as the texture becomes lighter. It is also generally found that a well- drained porous soil on top of ridges and knolls is more acidic and more leached then the average Carleton soil. Down the slope the reaction of the soil gradually increases and the degree of leaching decreases. This gradual change down the slope is partly connected with the parent material of the soil. The parent material of the Carleton series contains considerable lime, which on weathering, is liberated into the soil and subsequently washed down to the lower levels. This raises the pH of the lower lying soils and consequently restricts the leaching process.” (Stobbe 1940). Sites that receive seepage are thus enhanced with soluble bases that have been leached from adjacent upland soils and bedrock formations, resulting in increased fertility. The upper solum is usually friable to very friable, moderate to strong, medium, granular. The Bt is firm, but with a moderate, medium, subangular blocky structure. The subsoil increases in density with depth. Figure 19. Well drained Carleton soil profile. Carleton soils are associated with other soils that have developed on parent materials derived from calcareous to The Carleton association is considered highly suitable for weakly calcareous rock types - the Thibault and Caribou agriculture where surface relief is sufficient for external associations. Both of these soils have developed on drainage but not excessively steep. The soil has a relatively noncompact ablational tills and as such lack the compact deep (50 cm plus) available rooting zone with excellent subsoil found in the Carleton soils. The Thibault soils are also nutrient and water retention capacities. The soils are easily coarser textured than the Carleton soil. The Caribou worked and retain most of their structural integrity. From a association is similar to the Carleton association in that both forestry perspective these soils are capable of supporting a soils are fine loamy and have developed from parent materials wide range of commercial species. They are comparatively derived from the same lithological rock types. They differ in high in natural fertility. subsoil compaction. Carleton soils are compact, Caribou soils are noncompact. In some instances where the subsoils are only Summary of general characteristics of the Carleton Association weakly compact, separation of these two associations may be Map Symbol : CR difficult. Carleton soils have also been mapped with Violette Physiographic Region(s) : Chaleur Uplands and Holmesville soils. Both Violette and Holmesville soils Elevation : 300-500 m have been derived from acidic quartzite, sandstone, argillite Extent : 85,211 ha 47

Percentage of Mapped Area : 3.06% Parent Material Type : Mineral Mode of Origin : Glacial till, compact Material Thickness : < 2 m Soil Colour : Olive to yellowish brown Family Particle Size Class : Fine loamy Petrology (parent material) : Calcareous shale, argillite, slate and some calcite Inherent Fertility : High Topography (slope) : Rolling and undulating to hilly or sloping (2-100%) Drainage (dominant) : Well to moderately well Classification (typical) : Podzolic Gray Luvisol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 50 50 - 100+

Texture Class Loam Loam - clay loam Figure 20. Location of mapped Catamaran soils. % Sand 40 40

% Silt 40 29 thicker than the average depth of soil development can the two materials be positively identified. These represent very small % Clay 20 31 areas, being the exception rather than the rule. In most profiles the solum is underlain by a dense compact lodgment till % Coarse 15 subangular G/C 25 subangular G/C Fragments subsoil (Fig. 21). Because of the relatively thin nature of these deposits, the surface expression generally reflects the

pH (H2O) 5.0 - 5.5 6.0+ topography of the underlying bedrock. Landforms consist BD (g/cm3) 1.20 1.75 largely of blankets and to a lesser extent veneers over an undulating to rolling (2 to 15% slope) and sometimes hilly, Ksat (cm/hr) 2.5 - 10 0.1 - 0.5 inclined or sloping (9 to 45% slope) bedrock. Relief is a function of distance from the Maritime Plain, with more AWHC (cm/cm) 0.25 < 0.15 strongly expressed topographic conditions occurring in the central portions of the Highlands. Although the regolith is thin, the material is uniform in thickness. Seldom are there significant bedrock outcrops (ie. exposures covering more than Catamaran Association 2% of the surface) to warrant consideration. Well drained Catamaran soils support mixed softwood-hardwood stands of The Catamaran association consists of soils that have balsam fir, black spruce, red spruce, white birch, yellow birch, developed in moderately thin (most less than 2 m thick) red oak and sugar and red maple. Forest cover on poorly deposits of acidic, coarse loamy compact morainal till. This drained sites is comprised of balsam fir, black spruce, cedar, association has been used to describe soils that occur mostly in red maple, tamarack and some yellow birch. an area along the eastern boundary of the New Brunswick Central Highlands physiographic region (Fig. 20), where the Drainage of Catamaran soils ranges from good to poor, but glacial till has been derived from a mixture of Devonian well and imperfectly drained associates dominate. They are granites and Ordovician and Silurian greywacke, schists, classified as Orthic Humo-Ferric Podzols (Fig. 21) and Gleyed quartzite, slates and sandstones. Elevations range from 120 to Humo-Ferric Podzols, respectively. Most profiles show some 400 m above sea level. Other occurrences of Catamaran soils tendency of intergrading towards soils of the Ferro-Humic are found north of Fredericton and west of Bathurst. In total Podzol great group, with a thin (less than 10 cm thick) Bhf in these soils occupy approximately 133,044 ha or 4.77% of the the upper B horizon. Higher effective precipitation due to total map area. cooler temperatures results in environmental conditions in central New Brunswick that are conducive to organic matter Catamaran parent material has been deposited as ground accumulation in the B horizon and thus the formation of a Bhf. moraine, basal till plastered in place during glacial advance and Poorly drained Catamaran soils are classified mainly as Orthic subsequently covered with a thin discontinuous mantle of or Fera Gleysols, and occasionally as Orthic Humic Podzols. ablational till upon glacial retreat. Both materials are of Internal drainage is somewhat impeded by the subsoil which similar composition. Mixing actions of soil formation have has an estimated slow permeability rate of 0.1 to 0.5 cm/hr. obliterated most evidence of the ablational capping. Only in Available water storage capacity is estimated at 0.15 to 0.25 areas where the noncompact ablational material is significantly 48

are slow. The F horizon dominates over the H horizon. The light grayish coloured Ae overlies the dark reddish brown coloured Bhf which in turn changes abruptly to a 10 to 25 cm thick, yellowish brown coloured Bf horizon. The Bf horizon grades through a transitional BC horizon into a compact C horizon. The C horizon often has fragipan formation, which when moist, is difficult to differentiate from the compact parent material. When dry, the fragic material is brittle and slakes in water. Well drained profiles with fragipan development are classified as Fragic Humo-Ferric Podzols. However, most of the fragipan in Catamaran soils is weakly expressed and limited in areal extent. Imperfectly drained members of the Catamaran association have a similar sequence of horizons, but display distinct or prominent mottling, especially along the contact of the dense, compact subsoil. Gleying becomes more prominent in lower site positions. Poorly to very poorly drained Catamaran soils have profiles consisting of LFH or O, Aeg, Bg or Bgf, and Cg. The predominance of coniferous forest vegetation on these sites encourages mosses and the accumulation of thicker organic layers. Lithic phases of Catamaran occur randomly in well, imperfectly and even some poorly drained locations, wherever bedrock is near the surface. With the exception of being somewhat abbreviated, profile characteristics are similar to the aforementioned.

The Catamaran texture profile consists of a loam to sandy loam throughout, with 8 to 18% clay content. Weathering within the solum may result in a slightly finer texture in the upper profile than in the subsoil, however, this variation is still within the Figure 21. Moderately well drained Catamaran soil profile. loam-sandy loam grouping. Profile coarse fragment content ranges from 10 to 25% with subangular cobbles and gravels cm/cm in the solum and less than 0.15 cm/cm in the subsoil. the dominant size class. Most Catamaran land surfaces are Well to moderately well drained Catamaran soils have moderately to very stony with stone-sized clasts occupying 2 developed in areas where steeper topography permits adequate to 15% of the area. Usually these soils are also moderately to site drainage. They occupy crest to mid-slope positions in very cobbly with surface coverage similar to that of the stones. rolling landscapes, but may also occupy lower slope positions Surface boulders are present but not in significant quantities to in hilly, inclined and strongly sloping areas. Precipitation is warrant designation. Catamaran soils are low to medium in the dominant water source but additions by subsurface flow are natural fertility. The granitic parent rocks weather slowly and also significant in moderately well drained sites. Excess water yield relatively infertile soil material. The non-granitic flows both downward through the underlying parent material component tends to weather more rapidly and yield more and laterally as subsurface flow. Seepage along the subsoil nutrient-rich soil. Soil reaction increases with depth but both contact is common during periods of excess moisture. ie. after the solum and subsoil are acidic, falling within a pH(H2O) heavy rainfalls and following snowmelt. Poorly drained range of 4.0 to 5.5. The solum is weak to moderate, fine to Catamaran soils occur on level to gently undulating terrain medium, granular to subangular blocky structured and very characterized by slow runoff, or in depressions and along friable. It provides a 40 to 50 cm potential rooting zone. The drainage ways in areas with more relief (rolling, hilly and parent material is firm to very firm, compact, and slightly sloping topography). Groundwater flow and subsurface flow cemented in the upper C horizon. The C horizon is usually are the major water sources. Imperfectly drained sites are pseudoplaty in situ but breaks to medium subangular blocky frequently the result of a temporarily perched water table when extracted. where precipitation and lateral flow exceed downward permeability and evapotranspiration. Catamaran soils found along the Plaster Rock-Renous highway occupy a bedrock zone that separates the Long Lake-McGee Solum thickness ranges from 40 to 50 cm. On well drained association parent materials to the northwest, the Juniper sites the common horizon sequence is LFH, Ae, Bhf, Bf, BC association parent material to the west and the Reece and C or Cx. The upper horizons, LFH, Ae, and Bhf are all association parent material to the east. Juniper soils are readily relatively thin (3 to 10 cm) but distinct in appearance. differentiated from Catamaran soils on the basis of a number Mineralization and humification processes in the organic layer of properties, the most obvious being subsoil consistence, 49 coarse fragment content and lithology. Juniper soils have a Ksat (cm/hr) 2.5 - 10 0.1 - 0.5 noncompact subsoil, 20 to 50% coarse fragment content and granitic lithology. Catamaran soils have a compact subsoil, 10 AWHC (cm/cm) 0.15 - 0.25 < 0.15 to 25% coarse fragment content and mixed granitic-metamorphic lithology. Reece soils are similar in morphology but are fine loamy (greater than 18% clay content) whereas Catamaran soils are coarse loamy (less than 18% clay Gagetown Association content). Reece soils are also derived from sandstone and shale bedrock types. Long Lake soils are closest to the The Gagetown Association consists of soils developed in thick Catamaran association in terms of physical, chemical and deposits (some in excess of 20 m) of noncalcareous, sandy morphological properties. Long Lake soils are coarse-loamy skeletal, glaciofluvial material with mixed igneous and with compact subsoils, but they are derived from slate, metamorphic coarse fragment rock types. There soils occur in siltstone, argillite, schist and miscellaneous quartzite and small tracts scattered throughout the central New Brunswick greywacke. Highlands and coastal Maritime Plain regions of the survey area (Fig. 22). Gagetown association soils cover Biological production on Catamaran soils is affected by low to approximately 44,150 ha or 1.58% of the map area. medium inherent fertility, surface stoniness, depth to a root/water restricting layer, climate, and to a lesser degree wetness and topography. These limitations more severely handicap agriculture than forestry. Agricultural potential is marginal. Catamaran soils should prove adequate to support moderately productive stands of forest tree species climatically suited to the region.

Summary of general characteristics of the Catamaran Association

Map Symbol : CT Physiographic Region(s) : N. B. Highlands Elevation : 120-400 m Extent : 133,044 ha Percentage of Mapped Area : 4.77% Parent Material Type : Mineral Mode of Origin : Glacial till, compact Material Thickness : < 2 m Soil Colour : Yellowish brown to olive brown Family Particle Size Class : Coarse loamy Petrology (parent material) : Granite, schist, quartzite, slate and sandstone Figure 22. Location of mapped Gagetown soils. Inherent Fertility : Medium Topography (slope) : Rolling and undulating to hilly or sloping (2-45%) Gagetown soils are found on eskers, kames, kame terraces and Drainage (dominant) : Well to moderately well deltas, kame and kettle complexes, outwash plains and fans Classification (typical) : Orthic Humo-Ferric Podzol and valley trains. Surface expressions vary from gently undulating plains with less than 5% slopes to hummocky, terraced or sloping landscapes with slopes ranging from 2 or 3% to in excess of 45%. Steep complex slopes are the rule Layer Friable upper soil Subsoil material material rather than the exception. Many of these depositions are associated with present day river valleys along the Nepisiguit, Depth (cm) 0 - 45 45 - 100+ Tetagouche, Miramichi and Nackawic Rivers and their Texture Class Loam - sandy loam Sandy loam tributaries. Other deposits traverse the landscape, showing little or no conformity to existing relief or topography. These % Sand 50 60 were englacial stream flow sediments which were left behind upon glacial retreat. Most sediments consist of well % Silt 35 30 stratified sands and gravels with some cobbles. Bedding is % Clay 15 10 commonly skewed from the horizontal and particle size distribution may vary abruptly and significantly from one layer % Coarse 15 subangular C/G 20 subangular C/G Fragments to the next. Most of the finer materials (silts and clays) have been washed out during deposition. Boulders and stones

pH (H2O) 4.5 - 5.0 5.0 - 5.5 occasionally occur, both on the surface and within the soil profile, the result of ice-rafted debris. However, most units are BD (g/cm3) 1.20 1.80 nonstony. Gagetown soils usually support forest stands of 50 predominantly softwoods, jack pine and black spruce, with LFH, Ae, Bf or Bm, BC and C. Imperfectly to poorly drained some grey birch on the drier sites. Wetter sites along river profiles have: LFH or O, Ae, Bfgj or Bmgj, BCgj or BCg and bottoms encourage stands of black spruce, red maple and white Cg ; and very poorly drained profiles: LFH or O, Aeg, Bg and birch. Cg. The surface horizons of Gagetown soils are relatively devoid of the stratification or layering so prevalent and The Gagetown Association is dominated by well to rapidly characteristic of the parent material. The non-stratified nature drained Orthic Humo-Ferric Podzols (Fig. 23) and Eluviated of these upper horizons can be attributed to pedogenic Dystric Brunisols. Significant areas of gleyed phases of the activities of soil mixing by microorganisms, frost action and aforementioned subgroups occupy imperfectly and poorly tree windthrow. Pedogenic weathering has also resulted in drained sites, with some Orthic Gleysols on very poorly increased levels of silt and clay (fines) in the solum. The drained locations. On well to rapidly drained sites the sole Gagetown texture profile usually grades from a gravelly loamy source of water is precipitation. Excess rainfall quickly sand to sandy loam solum into a gravelly to very gravelly dissipates since the underlying material is very rapidly loamy sand to sand subsoil. Coarse fragment content varies permeable (usually greater than 25 cm/hr). These soils have a from occasionally less than 20% in the solum to more than low to very low available water storage capacity, 0.10 cm/cm 70% in the C horizon or parent material, usually increasing or less. In imperfectly and poorly drained sites excess water is with depth. Most coarse fragments are rounded or subrounded the result of a high ground water table. Off drainage occurs in gravels, 0.2 to 7.5 cm in diameter, however some larger depressions and lower terrace site positions along some stream cobbles may occur. The coarse fragments are derived from and river valleys. granites, granite gneiss, schists, quartzite, basalt and related lithologies. Gagetown soils are very low in natural fertility.

They are also acidic throughout the profile, with pH(H2O) ranging from 4.0 to 5.5. In well drained soils the parent material colour is yellowish brown to brown. The solum consists of a light gray Ae horizon and a yellowish brown to strong brown and occasionally even reddish brown Bf or Bm horizon. Imperfectly and poorly drained members have either distinct or prominent mottling. Poorly and very poorly drained members are gleyed with gray to olive gray colours of low chroma. The subsoils are loose and single grain, while the sola are for the most part very friable, very weak, fine to medium granular. In exception to this is the presence of ortstein, a hardpan that occurs sporadically throughout Gagetown soils. Iron, aluminum and organic complexes are the cementing agents that result in massive to slightly platy, irreversible Bfc horizons. Ortsteins usually form 10 to 15 cm below the mineral soil surface. The upper boundary of the ortstein is abrupt and cementation decreases near the lower boundary some 10 to 45 cm below. Ortstein is most strongly expressed under poorly drained conditions, however, even here it is discontinuous. Massive blocks of cemented ortstein materials are frequently observed in gravel pits where Gagetown soil parent materials are being extracted.

The Gagetown catena has formed in glaciofluvial material derived primarily from igneous and highly metamorphosed rocks. It is found in areas dominated by soils formed from similar rock types, such as the Juniper, Catamaran, Popple Depot and Tuadook Associations. However, these are till soils and readily distinguished from Gagetown. Catamaran, Popple Depot and Tuadook are nonstratified deposits with angular Figure 23. Rapidly drained Gagetown soil profile. coarse fragments, finer textures and have compacted subsoils. Juniper, an ablational till, is similar to Gagetown owing to its The solum of Gagetown Association soils varies from 35 to 45 mode of deposition. Depending upon the degree of water- cm in thickness. Solum thickness is related to the prevailing working during deposition, some Juniper soils may closely moisture regime. Well to somewhat imperfectly drained soils resemble Gagetown soils. The modal Juniper soil is readily have the thickest development, followed by rapidly differentiated from Gagetown on the basis of its non-stratified, (excessively) and then poorly to very poorly drained soils. The heterogeneous nature and the presence of more angular coarse common horizon sequence in well to rapidly drained soils is: fragment shapes. Gagetown soils also occupy the same type of 51 landforms as a number of other associations formed in fluvial BD (g/cm3) 1.20 1.55 sediments - Grand Falls, Riverbank, Interval and Maliseet. Geographically, the Gagetown association is most closely Ksat (cm/hr) > 25 > 25 associated with the Riverbank and Interval associations. AWHC (cm/cm) < 0.10 < 0.05 Differentiation among associations formed in fluvial sediments is made on the basis of particle size or coarse fragment lithology. The Interval and Maliseet associations are coarse loamy; the Riverbank association is sandy; and the Grand Falls Association Grand Falls association is sandy skeletal but with noncalreous shale, quartzite, slate and sandstone coarse fragments. In The Grand Falls Association consists of soils developed in comparison, the Gagetown association is sandy skeletal and thick deposits (often in excess of 20 m) of acidic, sandy has granite, granite gneiss, basalt and some quartzite coarse skeletal, glaciofluvial material with noncalcareous slate, shale, fragments. quartzite and sandstone coarse fragments. The glaciofluvial material is underlain by glacial till or bedrock. These soils All uses of Gagetown soils for biological production, be it occur in small tracts scattered throughout the Chaleur Uplands agriculture or forestry, are limited by the soils low water and New Brunswick Highlands regions of the survey area (Fig. holding capacity and fertility related problems - low inherent 24). Grand Falls association soils cover approximately 24,264 fertility and low fertility retention. Forest tree species selection ha or 0.87% of the map area. must be done with these limitations in mind. Imperfect to very poorly drained members also have added problems of excessive wetness, typically due to topographic position. However, Gagetown soils are readily drained by tile drainage systems. Gagetown soil parent material is an excellent source of aggregate for road building, construction and related uses. It is extracted for local use from numerous sites.

Summary of general characteristics of the Gagetown Association

Map Symbol : GG Physiographic Region(s) : N. B. Highlands, Maritime Plain Elevation : up to 300 m Extent : 44,150 ha Percentage of Mapped Area : 1.58% Parent Material Type : Mineral Mode of Origin : Fluvial (glaciofluvial) Material Thickness : Up to 20 m Soil Colour : Yellowish brown to brown Family Particle Size Class : Sandy skeletal Petrology (parent material) : Mixed igneous and metamorphic and some sedimentary Inherent Fertility : Low Figure 24. Location of mapped Grand Falls soils. Topography (slope) : Terraced, undulating and hummocky (2- 45%) Drainage (dominant) : Rapid Grand Falls soils were deposited as river terraces, outwash Classification (typical) : Orthic Humo-Ferric Podzol plains or kames or eskers. The topography is either hummocky ie, knob-and-kettle; terraced, with horizontal or gently inclined terraces separated by steeply sloping scarp faces; or undulating. The knob-and-kettle topography consists Layer Friable upper soil Subsoil material of a disordered assemblage of knolls or "knobs" interspersed material with irregular depressions or "kettles" that are commonly Depth (cm) 0 - 40 40 - 100+ poorly drained or even swamps or ponds. The terraces are long, narrow surfaces running parallel to streams and rivers, Texture Class Loamy sand Loamy sand - sand marking a former water level. The esker deposits are long, % Sand 80 85 narrow, low, sinuous, steep-sided ridges or mounds. Most of the Grand Falls soils mapped are located along present day % Silt 10 10 drainage systems, however, some minor deposits are known to % Clay 10 5 occur in isolated areas far removed from any existing waterways. These have been deposited by streams within % Coarse 25 rounded G 60 rounded G glacial ice and then subsequently laid down upon glacial Fragments retreat, thus showing little or no conformance to local relief. Most sediments consists of well stratified sands and gravels pH (H2O) 4.5 - 5.0 5.0 - 5.5 52 with some cobbles. The soil and rock fragments are smooth to in excess of 70% in some strata (layers) in the parent and rounded. The layers or strata vary in thickness and material. Percentage coarse fragment content varies from one composition, a reflection of the changing environmental stratum to another. Most coarse fragments are round-edged, conditions during which they were deposited. Although some flat, elongated gravels or channers, 0.2 to 15 cm long. These erratic surface boulders and stones may be found, Grand Falls channers are derived from slate, shale, quartzite, sandstone and soils are considered to be nonstony. The major forest species related lithologies. The characteristic channer shape is an on well to rapidly drained sites are black spruce, balsam fir and inherited feature from these rock types. Grand Falls soils are white and yellow birch. Poorly to very poorly drained lower low in natural fertility. Profiles are acidic throughout, with slopes and depressions support communities of black spruce, pH(H2O) values ranging from 4.0 to 5.5. In well drained soils balsam fir, red maple and white birch. the parent material colour is olive brown. The solum consists of a relatively thin (1-5 cm) LFH horizon over a light to The Grand Falls Association is dominated by well to rapidly pinkish gray Ae which is underlain by a brownish or reddish drained Orthic Humo-Ferric Podzols (Fig. 25). Gleyed yellow to strong brown coloured Bf. Imperfectly drained soils Humo-Ferric Podzols occupy imperfectly drained sites, and have iron mottling of high chroma and value in the lower B Gleyed Humo-Ferric Podzols, Gleyed Eluviated Dystric and C horizons. Poorly drained soils are characterized by gray Brunisols, Orthic Gleysols and Rego Gleysols occur on poorly colours and prominent mottling indicative of intense reducing to very poorly drained sites. The subsoil parent material is conditions. Matrix chromas are generally 2 or less. The very rapidly permeable (usually greater than 25 cm/hr) and so subsoils are loose and single grain, while the sola are very on elevated, rapidly to well drained sites, excess precipitation friable to friable, with weak, fine to medium, granular structure readily flows downward through the profile. These soils have in the B horizon and weak, fine, platy structure in the A low available water storage capacity within the control section, horizon. Cementation of the B horizon occurs in some profiles. averaging 0.10 cm/cm or less. The available water storage This is the result of ortstein or hardpan formation. It is capacity decreases with depth, a reflection of coarser soil discontinuous and very sporadic in its occurrence. materials and increased gravel content. Upper solum water holding capacities are enhanced by their finer textures and the presence of organic matter. Precipitation is the sole source of water on these sites. Off-drainage (imperfect, poor and very poor drainage) is the result of high ground water tables and groundwater flow. Most Grand Falls soils are either dry (well to excessively drained) or wet (poorly to very poorly drained). Areas of imperfect drainage are restricted to subdominant components of map units of the above mentioned drainage categories.

The depth of the solum of Grand Falls Association soils varies from 35 to 55 cm. Thickest solum development is found on well to imperfectly drained sites. Sites with moisture regimes at the extremes, either excessively dry or excessively wet, tend to have shallower solum development. The common horizon sequence in well to rapidly drained soils is: LFH, Ae, Bf, BC and C. At higher elevations where there is greater effective precipitation, increased accumulation of organic matter in the upper podzolic B horizon leads to the formation of a thin Bhf horizon. Imperfectly drained profiles have: LFH, Ae, Bfgj, BCgj and Cg horizons, indicating the presence of distinct or prominent mottles. Poorly to very poorly drained soils have horizons sequences of: LFH, Ae, Bmgj or Bfjgj and Cg; LFH or O, Aeg, Bg and Cg; or LFH or O and Cg as drainage gets progressively worse. The stratification so characteristic of the soil parent material is not present in the solum. Mixing actions of soil organisms, frost churning and tree uprooting (windthrow) have altered the upper soil profile, obliterating any of its original stratification. The Grand Falls texture profile usually grades from a gravelly sandy loam to loamy sand, and occasionally even loam, solum into a gravelly to very gravelly loamy sand to sand subsoil. In poorly drained Figure 25. Rapidly drained Grand Falls soil profile. sites inwashed fines (siltation) may make the surface material slightly heavier. Coarse fragment content increases with depth Grand Falls soils are found in areas dominated by soils formed 53 from shale, slate, quartzite and sandstone, such as the Ksat (cm/hr) > 25 > 25 Holmesville, Long Lake and McGee associations. However, these are till soils and readily distinguished from Grand Falls AWHC (cm/cm) < 0.10 < 0.05 soils. These till soils are nonstratified deposits with angular coarse fragments (cobbles, gravels, and stones), finer textures and have friable to very firm subsoils. Grand Falls soils occupy the same type of landscapes as do a number of other Guimond River Association soils formed on fluvial sediments: Gagetown, Interval and Maliseet. They are differentiated on the basis of soil particle The Guimond River Association consists of soils developed in size class and coarse fragment lithology. Interval and Maliseet relatively thick deposits (sometimes in excess of 10 m) of are coarse loamy nonskeletal materials. Gagetown is sandy acidic, sandy skeletal, glaciofluvial material with coarse skeletal, but dominated by igneous coarse fragments. fragments of soft sandstone. The glaciofluvial sediments are underlain by either bedrock, or a thin mantle of glacial till over Biological production on Grand Falls soils is limited because the bedrock. Guimond River soils are found only on the of low fertility retention and low water holding capacity. Finer- lowlands or Maritime Plain (Fig. 26). All deposits occur at low textured surface soil in some deposits helps but does not altitude, less than 100 m above sea level, and so were subjected completely alleviate this problem. Retention characteristics of to a short (approximately 2000 years) period of post glacial the subsoil are still problematic. Excessive wetness is an marine submergence. They occupy approximately 2169 ha or additional problem on poorly drained sites. Grand Falls soil 0.08% of the map area. Occurrences are scattered and small parent material is an excellent source of aggregate for road in size. building, construction and related uses. It is extracted for local use from numerous sites.

Summary of general characteristics of the Grand Falls Association

Map Symbol : GF Physiographic Region(s) : N. B. Highlands, Chaleur Uplands, Notre Dame Mountains Elevation : 300-600 m Extent : 24,264 ha Percentage of Mapped Area : 0.87% Parent Material Type : Mineral Mode of Origin : Fluvial (glaciofluvial) Material Thickness : Up to 20 m Soil Colour : Olive to olive brown Family Particle Size Class : Sandy skeletal Petrology (parent material) : Noncalcareous slate, shale, quartzites and sandstones Inherent Fertility : Low Topography (slope) : Terraced and hummocky to undulating and rolling (0.5-15%) Drainage (dominant) : Rapid Classification (typical) : Orthic Humo-Ferric Podzol

Figure 26. Location of mapped Guimond River soils.

Layer Friable upper soil Subsoil material Guimond River soils were deposited as river terraces, outwash material plains, eskers, beach ridges and related landscapes. Typically Depth (cm) 0 - 45 45 - 100+ they are found close to flowing water, but not necessarily. Englacial sediments deposited during glacial retreat do not Texture Class Sandy loam - loamy Loamy sand - sand always conform to present day relief. Landform surface sand expressions vary from gently undulating with slopes of less % Sand 75 90 than 5%, to sloping terraced configurations with complex, irregular slopes of up to 30%. Valley fills of Guimond River % Silt 15 5 materials are common. The sediments consist of well stratified sands and gravels with some cobbles. Water working has % Clay 10 5 resulted in most soil and gravel fragments being smoothed and % Coarse 35 rounded, flat, 60 rounded, flat, well rounded. Changing conditions during the time of Fragments elongated G elongated G deposition is reflected in an alternation of sediment beds that show no regular sequence and considerable variation in pH (H2O) 4.5 - 5.0 5.0 - 5.5 thickness and texture. Guimond River soils are nonstony, with BD (g/cm3) 1.20 1.50 the exception of the occasional ice rafted erratic stone or 54 boulder. Well to rapidly drained sites support stands dominated non-sandstone components from the highlands may be present. by jack pine and black spruce, with minor inclusions of red The gray-green sandstone is relatively soft ( less than 4 Mohs pine and stunted white birch. Ill-drained sites in depressions scale), medium to fine-grained, and contains 60 to 85% or along drainage channels have forest stands of black spruce, feldspars and 5 to 10% biotite and muscovite. Guimond River balsam fir, red maple and some birch and alder. soils are very low in natural fertility and acidic throughout the

profile, with pH(H2O) values of 4.0 to 5.5. In well to rapidly The Guimond River association is dominated by well to drained soils the parent material is olive to yellowish brown. rapidly drained Orthic Humo-Ferric Podzols and Eluviated The solum consists of a light grayish coloured eluvial Ae Dystric Brunisols. Imperfectly to poorly drained sites are horizon with an abrupt boundary to a reddish brown to classified as gleyed phases of the aforementioned subgroups. yellowish brown B horizon that becomes progressively Very poorly drained soils are frequently classified as Orthic yellower in hue as it grades into the BC and C horizons. Gleysols. The entire depth of the soil (greater than 100 cm) Mottles and grayish gley colours are found in imperfectly and consists of a very rapidly permeable material with saturated poorly drained conditions, but for the most part the general hydraulic conductivities of 25 cm/hr and faster. Coarse texture podzolic or brunisolic horizon sequence is maintained. The results in a low available water storage capacity of 0.10 cm/cm subsoil is loose and single grain while the solum is usually or less. The available water storage capacity is highest in the very friable, very weak, fine to medium granular. Ortstein, an solum where textures are slightly finer and less gravelly, and irreversible hardpan, occurs sporadically in the B horizon of organic matter is present in significant quantities. Precipitation Guimond River soils. Iron, aluminum and organic matter is the sole source of water on well to rapidly drained sites. In complexes cement the sand grains together into a very firm, poorly drained sites precipitation supplements groundwater compact, massive but discontinuous layer. Ortstein is most flow, which is the dominant factor determining drainage. In strongly expressed under poorly drained conditions. the catenary sequence the transition from rapidly drained to poorly drained soils is abrupt, occurring over a relatively short The Guimond River association is found on the eastern coastal horizontal distance. Imperfectly drained soils are usually only plain portion of the study area, interspersed between units of subdominant components of map units dominated by either Reece, Stony Brook and Sunbury till soils. The Reece and well to rapidly drained soils or poorly to very poorly drained Stony Brook soils are compact lodgment tills and readily soils. distinguished from the Guimond River association. Sunbury soils are similar lithologically in that their coarse fragments are Solum development in Guimond River soils varies from 30 to derived from soft sandstone. But Sunbury soils are finer 50 cm in depth, where it gradually merges into the textured in the parent material and consist of nonstratified unweathered regolith or subsoil. Well-aerated conditions glacial drift with angular and flaggy coarse fragments. promote thicker sola than in poorly drained sites. This may be Guimond River soils are most closely associated with somewhat negated on rapidly drained sites that are excessively Richibucto soils. Both were deposited by water and they droughty. Moisture deficiencies lead to reduced rates of soil occupy similar landscapes positions. However, Richibucto genesis. Poorly drained soils may have more than 20 cm of soils are non-skeletal; they are relatively coarse fragment-free organic debris accumulation on the surface. The common sandy materials. horizon sequence is: in well to rapidly drained soils, LFH, Ae, Bf or Bm, BC and C; in imperfectly to poorly drained soils, Very low water holding and nutrient retention capacities effect LFH or O, Ae, Bfgj or Bmgj, BCg and Cg; and in very poorly all uses of Guimond River soils for biological production of drained soils, LFH or O, Aeg, Bg and Cg. forest and agricultural crops. Forest tree species selection in particular must be made with these limitations in mind. Postglacial marine submergence (wave washing, sediment Guimond River parent material is a source of aggregate used deposition and erosion) and soil forming processes have for buildings, road construction and related activities. Quality created solum conditions that vary from the subsoil. The is a problem with these materials. The sandstone clasts are solum is nonstratified and finer textured and less gravelly than considered to be unsound. The gravels are soft and rapidly the subsoil. Marine submergence was brief and consisted more break down into their initial components, ie. sand, making of an estuarial environment of brackish water rather than salt them lower quality gravel sources. water. Some sediments may have been deposited subaqueously. However, chemical alterations as a result of this Summary of general characteristics of the Guimond River Association marine inundation have long since been leached out. The Map Symbol : GM Guimond River texture profile consists of gravelly to Physiographic Region(s) : Maritime Plain nongravelly sandy loam to loamy sand A and B horizons over Elevation : < 100 m a gravelly to very gravelly loamy sand to sand subsoil. Coarse Extent : 2169 ha fragment content increases with depth. It ranges from 35 to Percentage of Mapped Area : 0.08% Parent Material Type : Mineral 70%. Most coarse fragments are rounded gravels, 0.2 to 7.5 Mode of Origin : Fluvial (glaciofluvial), possibly marine- cm in diameter. They are derived from the gray-green modified Pennsylvanian sandstone that underlies the coastal plain. Material Thickness : Up to 10 m Minor inclusions of red Pennsylvanian sandstone and some Soil Colour : Olive to yellowish brown 55

Family Particle Size Class : Sandy skeletal Petrology (parent material) : Soft gray-green sandstone Inherent Fertility : Very low Topography (slope) : Undulating (0.5-5%) Drainage (dominant) : Rapid Classification (typical) : Orthic Humo-Ferric Podzol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 40 40 - 100+

Texture Class Sandy loam - loamy Loamy sand - sand sand

% Sand 80 90

% Silt 10 5

% Clay 10 5 Figure 27. Location of mapped Holmesville soils.

% Coarse 30 rounded G 60 rounded G surface area occupied by coarse fragments. Frost action may Fragments concentrate profile cobbles on the mineral soil surface under

pH (H2O) 4.5 - 5.0 5.0 - 5.5 the forest floor in imperfectly and poorly drained sites. Boulders are not common. Holmesville landforms are BD (g/cm3) 1.20 1.50 dominated by undulating, rolling and occasionally hilly surface Ksat (cm/hr) > 25 > 25 expressions with slopes varying from 2 to 45%, but mostly in the 2 to 15% range. Holmesville soils occur on bedrock AWHC (cm/cm) < 0.10 < 0.05 controlled topography with most map units averaging only 1 to 2 m of soil material. Veneer phases are associated with areas of steeper topography and bedrock outcrops that occur are usually associated with these areas. Well drained soils of Holmesville Association the Holmesville association support forest communities of sugar maple, beech, yellow birch, red oak, red and white The Holmesville association consists of soils that have spruce, balsam fir, red maple, white pine, trembling aspen, pin developed in relatively thin (1 to 3 m thick) deposits of acidic, cherry, striped maple and mountain maple. On poorly to very coarse loamy, compact morainal till sediments derived from poorly drained sites the tree vegetation consists of black quartzite and sandstones with miscellaneous argillite, slate spruce, cedar, speckled alder and balsam fir, with some red and schists. They occur in the Chaleur Uplands, Central maple and tamarack. Highlands and Notre Dame Mountains physiographic regions of the study area (Fig. 27) at elevations of 300 to 600 m above Holmesville soils are dominated by well drained Orthic sea level. Holmesville soils occupy approximately 72,592 ha, Humo-Ferric Podzols (Fig. 28). Well drained conditions or 2.60% of the map sheet. dominate where more steeply sloping hilly and rolling landscapes occur. In these landforms poorly and imperfectly The soil parent material has been deposited as ground moraine, drained conditions are confined to relatively narrow drainage plastered in place under the weight of advancing glacial ice. channels. More significant hectarages of imperfectly and However, it is possible that the loose material in which the poorly drained Holmesville soils occur as Gleyed Humo-Ferric solum formed is a thin layer of ablational till, derived from the Podzols and Orthic Gleysols, respectively, in areas of same bedrock sources, deposited on top of the ground moraine undulating to gently rolling topography. Internal drainage is by melting ice during glacial retreat. As a result, there are restricted by a slowly to moderately slowly permeable subsoil varying depths of the loose material overlying the compact till. with an estimated saturated hydraulic conductivity value of 0.1 Composition strongly reflects the incorporation of local to 1.0 cm/hr. Available water storage capacity ranges from bedrock formations. The till is a heterogeneous mixture of 0.25 to less than 0.15 cm/cm, decreasing with depth because of angular to subrounded shaped particle sizes ranging from silts reduced total porosity in the compact subsoil. Well drained and clays to cobbles and stones. Coarse fragment shapes are a sites are supplied with water solely via precipitation. function of the parent bedrock but have been somewhat Downward movement of excess moisture through the profile rounded by basal till grinding actions. Contents typically vary is impeded by the subsoil, resulting in lateral flow or seepage, from 10 to 30% with a high percentage of gravels and cobbles. particularly in the spring after snowmelt. Imperfectly and Holmesville soils are generally not too stony to prevent their poorly to very poorly drained areas have developed because of use for agriculture, with usually less than 3% of the land a combination of topographic position, lack of gradient, subsoil 56 compaction, seepage and high groundwater table. lack a podzolic B horizon. They consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The forest duff layer is thicker in the poorly and very poorly drained conditions than found in well drained counterparts, varying from 5 to 15 cm, but is occasionally as thick as 30 cm. The Holmesville textural profile consists of a loam to sandy loam (8 to 18% clay) throughout. Profile coarse fragment content varies from 10 to 30%, with a preponderance of subangular to somewhat subrounded gravels and cobbles. Holmesville soils are medium in inherent fertility and acidic throughout, with

pH(H2O) values of 4.0 to 5.5. The friable to very friable, weak to moderate, fine to medium, granular or subangular blocky solum overlies a firm to very firm, massive to medium platy subsoil. The subsoil shatters readily upon extraction.

The Holmesville association is most commonly found with members of the Long Lake and McGee associations. The three soils have been derived from materials of similar lithological origin, mostly metasedimentary rock types. Holmesville and Long Lake are also alike in many other physical, chemical and morphological features, both having developed in coarse loamy basal till materials. Differentiation is primarily based on lithology. Long Lake soil parent materials have been derived from strongly metamorphosed quartzite, slates and some volcanics. Subsoil consistence is the primary differentiating criteria between McGee and Holmesville. Holmesville subsoils have firm to very firm consistence, high bulk density (greater than 1.75 gm/cm3) and voids consisting predominantly of micro pores. McGee subsoils are friable (to slightly firm), lower in bulk density (usually less than 1.60 gm/cm3) and have a higher proportion of macro pores. Holmesville soils have also been mapped in association with Boston Brook, Caribou, Carleton, Jacquet River and Thibault soils. Figure 28. Well drained Holmesville soil profile, cultivated. Excluding problems due to wetness in imperfectly and poorly Soil development varies from 35 to 65 cm in thickness. The drained locations, the dominant features affecting agricultural common horizon sequence on well drained sites is LFH, Ae, land use are related to topography (excessive slope), coarse Bhf, Bf, BC and C. O horizons may occur under coniferous fragment content (both surface and profile) and the presence of forests where mosses dominate the ground vegetation. The a subsoil restricting layer which impedes root penetration and organic layer is 2 to 10 cm thick, becoming more water percolation. Medium inherent fertility means that humified with depth. It overlies a thin (5 to 10 cm), white, Holmesville are productive forest soils suited to a wide range ashy coloured Ae horizon which breaks abruptly into the B of tree species. Holmesville are typical of soil development in horizon. The upper strong brown to dark reddish brown Bhf New Brunswick and have been selected as the provincial soil horizon varies from 2 to 5 cm in thickness. It merges with the (Fig. 29). brown to yellowish brown Bf horizon which gradually grades into the oxidized olive to grayish brown parent material. Morphological appearance may be deceptive. Significant amounts of translocated iron and aluminum are often present Figure 29. Provincial soil in horizons that display little colour change from the parent badge. The Holmesville soil material. At 35 to 45 cm the podzolic B horizon grades into a was proclaimed the New BC horizon which grades into the unaltered parent material or Brunswick provincial soil on C horizon between 35 and 65 cm from the mineral soil surface. February 13, 1997. Imperfectly drained soils have similar profile horizons but are modified by periodic saturation. They are mottled in the B and C horizons, especially a thin zone immediately above the compact subsoil where water is perched. The Ae horizon is often irregular or broken because of tree uprooting due to windthrow. Poorly to very poorly drained horizon sequences 57

Summary of general characteristics of the Holmesville Association sea level to 700 m. However, at the exploratory level of mapping it is not possible to identify these as individual units. Map Symbol : HM Physiographic Region(s) : Chaleur Uplands, Notre Dame Mountains, They are considered as predictable inclusions within other N. B. Highlands related map units. The only areas of significant size are found Elevation : 300-600 m along the Nashwaak, Keswick and Southwest Miramichi Extent : 72,592 ha Rivers where river channel meandering has resulted in flood Percentage of Mapped Area : 2.60% Parent Material Type : Mineral plains of up to 1 km in width (Fig. 30). These are within the Mode of Origin : Glacial till, compact Lowlands and Central Highlands physiographic regions. In Material Thickness : 1-3 m total, Interval soils account for 4,871 ha, or 0.17% of the map Soil Colour : Olive to olive brown area. Family Particle Size Class : Coarse loamy Petrology (parent material) : Quartz and sandstone with miscellaneous argillite, slate and schist Inherent Fertility : Medium Topography (slope) : Rolling and undulating to hilly or sloping (2-100%) Drainage (dominant) : Well to moderately well Classification (typical) : Orthic Humo-Ferric Podzol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 50 50 - 100+

Texture Class Loam - sandy loam Loam - sandy loam

% Sand 50 50

% Silt 35 35

% Clay 15 15

% Coarse 15 subangular G/C 25 subangular G/C Fragments Figure 30. Location of mapped Interval soils. pH (H2O) 4.5 - 5.0 5.0 - 5.5

BD (g/cm3) 1.10 1.75 Interval alluvial terraces, flood plains and stream bottoms have flat to very gently undulating surface expressions with Ksat (cm/hr) 2.5 - 10 0.1 - 1.0 generally less than 2% slope (Fig. 31). They are located only AWHC (cm/cm) 0.20 - 0.25 < 0.15 slightly above mean annual river elevation. Alluviation is an ongoing process. Increments of soil are added during flooding. Depending upon site location this may be an annual event or may only occur under extreme conditions (ie. once in every 10 Interval Association or 20 year flood). Because of this gradual buildup or accumulation of sediments, most Interval soils are rich in The Interval association consists of soils that have developed organic matter. Plant roots and surface litter are constantly in acid to neutral, coarse loamy to sandy alluvial sediments of being buried by the addition of new sediments (Fig. 32). variable thickness. Alluvium is deposited during relatively Floodwaters are also rich in organic matter. The natural recent geologic time by running water (rivers, streams, etc.) as vegetation on these valley floor locations is distinctly different sorted or semi-sorted clays, silts, sands and gravels in stream from that associated with adjacent uplands. They are beds and flood plains. It is derived from the till and bedrock dominated by nutrient demanding and/or water tolerant that underlies its upstream area of origin. The size of particles deciduous tree species such as elm, ash, red maple, willow and carried by the water is among other factors determined by alder and various native grasses and herbaceous plants. stream flow velocities and currents. Settling occurs where stream velocity is decreased. Depositions are thus varied The Interval association is dominated by imperfectly drained within the profile (layered) as well as from site to site. Interval Gleyed Regosols and Gleyed Cumulic Regosols. Soil sediments are mostly silts and fine sands, although some horizonation is too weakly expressed to meet the requirements coarser-textured materials are found immediately adjacent to of any order other than the Regosolic Order because of the the channel. They occur as narrow flood plains and terraces youthfulness of the material. These are immature soils. They along most stream courses. Small tracts of Interval soil are have little or no soil horizon development. The common scattered throughout the study area at elevations ranging from horizon sequence consists of an LF and thin (less than 10 cm 58 thick) Ah over a Cgj. A B horizon less than 5 cm thick may with each successive deposition during flooding. Many of the underlie the Ah. Sites with only intermittent flooding and sediments consist of nutrient rich materials eroded from upland deposition of material have buried Ah horizons resulting in soils. Texture and organic matter contents are also conducive profile horizon sequences of LF, Ah, Cgj, Ahb, Cgj, Ahb, Cgj to nutrient retention. Soil reaction ranges from pH(H2O) 5.0 etc. Well to moderately well drained Interval soils are to 6.5. Most variation is between profiles. The parent material classified as orthic subgroups of their imperfectly drained colour is olive to yellowish brown in well to moderately well counterparts. Most of these profiles still have some faint drained soils. Thin, irregularly spaced layers of dark coloured, orange mottling. Poorly and very poorly drained associates are buried Ah horizon may occur. The surface Ah is dark gray to Rego Gleysols and Rego Humic Gleysols with common dark brown. Gray shades dominate poorly to very poorly horizon sequences of LFH or O, Cg; and LFH or O, Ah, Cg; drained sites. The soil profile is weak to moderate, medium respectively. Buried horizons may also occur. All catena granular to fine subangular blocky and friable to very friable members are subjected to flooding. The severity of flooding throughout. No compacted or otherwise root restricting layers varies with site position. During the spring floods the soils are exist. usually saturated with water or entirely submerged. As river levels recede, surplus moisture seeps through the profile. Where water is trapped in enclosed depressional areas the drying out period is extended to several weeks. Interval soils are usually readily permeable within the profile (saturated hydraulic conductivity of greater than 2.5 cm/hr). Underlying substrata of both coarse (sand and gravel) and fine (clay) materials may impede water movement. The available water holding capacity averages 0.20 to 0.30 cm/cm for the entire depth of the profile. Imperfectly drained soils are supplied with water from numerous sources: precipitation, seepage from adjacent uplands, and groundwater flow. Well to moderately well drained sites occupy slightly elevated positions and are not effected by subsurface and groundwater flow to the same extent as imperfectly drained sites. Poorly to very poorly drained sites are the result of high groundwater tables and inflow of seepage waters. They are found in low-lying depressions and are subjected to ponding after heavy rainfall or whenever river levels rise.

Figure 32. Imperfectly drained Interval soil profile.

Interval soils are associated with other fluvial soils that occupy Figure 31. Interval soil association landscape. similar geographic positions. They have been mapped with Gagetown, Grand Falls and Riverbank soils. The Gagetown The Interval textural profile consists of a relatively uniform silt and Grand Falls associations are sandy skeletal (ie. gravels) loam to fine sandy loam or fine loamy sand throughout (Fig. and the Riverbank association is sandy. All three have well 32). The majority of soil particles fall within the silt to fine developed horizonation. Interval soils are readily sand diameter range, 0.002 to 0.25 mm. Stratification is distinguished by their lack of soil development and silty common in the lower profile. Substrate may be quite variable texture. (clays to gravels) depending upon past stream conditions. Interval sediments are free of coarse fragments and surface Well to moderately well drained Interval soils are particularly stones. They are high in natural fertility, probably the most suited to agriculture. They are stone free and friable fertile soils of the region. The fertility is renewed or enhanced throughout, making them easy to work. Available moisture 59 storage capacity is high and they retain nutrients well. Surface Jacquet River Association conditions are level to gently undulating. Their chief limitations are that they are subject to flooding and that their The Jacquet River association consists of soils that have scattered distribution and small extent make them developed in moderately thin (mostly less than 2 m) deposits economically unimportant from a regional perspective. of acidic, coarse loamy non-compact morainal till derived from Flooding and subsequent saturation delays planting until late mixed rhyolite and trachytes with some basalt and in the spring. Poorly drained areas are difficult to drain miscellaneous slates and greywackes. It occurs scattered because of their low-lying locations with groundwater levels across the New Brunswick Central Highlands physiographic near the surface. Development of many Interval soils is region. Some Jacquet River soils are also mapped in the possible on a field by field basis, but under other circumstances Chaleur Uplands (Fig. 33). Elevations range from 120 to 700 they require community efforts for such projects as dykes and m above sea level. In total these soils occupy approximately main drains. From a wood production point of view, Interval 69,047 ha or 2.48% of the total map area. soils are really of little significance, other than that they occupy riparian zones that are protected. However, it is this riparian zone nature that makes Interval soils extremely important in terms of surface water quality protection and wildlife habitat. Interval soil material is often treated as an extractable commodity. It is "mined" and sold as topsoil for lawns, gardens and other uses.

Summary of general characteristics of the Interval Association

Map Symbol : IN Physiographic Region(s) : Maritime Plain, N. B. Highlands Elevation : up to 700 m Extent : 4871 ha Percentage of Mapped Area : 0.17% Parent Material Type : Mineral Mode of Origin : Fluvial (alluvium) Material Thickness : 1-4 m Soil Colour : Olive to yellowish brown Family Particle Size Class : Coarse loamy Petrology (parent material) : Undifferentiated Inherent Fertility : High Topography (slope) : Undulating or terraced (0.5-5%) Figure 33. Location of mapped Jacquet River soils. Drainage (dominant) : Imperfect Classification (typical) : Gleyed Regosols Jacquet River parent material is a non-compact till and as such has been deposited either as an ablational till or possibly as a lodgment till that has been reworked by water. Regardless of Layer Friable upper soil Subsoil material origin, it is friable throughout both solum and subsoil. material However, as a result of the overburden, the subsoil does tend Depth (cm) 0 - 30 30 - 100+ to be somewhat more dense. Because of the relatively thin nature of these deposits, surface topography is generally a Texture Class Silt loam - fine Silt loam - fine sandy reflection of the topography of the underlying bedrock. The sandy loam loam exception to this is where Jacquet River is mapped as % Sand 30 25 hummocky. Here the till is often slightly thicker and tends to mask the underlying bedrock configuration. Most Jacquet % Silt 55 60 River landforms consist of a mixture of veneers and blankets % Clay 15 15 on either undulating and rolling or hilly, ridged and sloping bedrock formations. Slopes range from 0.5 to 100%. Bedrock % Coarse 0 0 outcrops are common on the more rugged landscapes (hilly, Fragments sloping) that have steeper slopes. Here exposures occupy

pH (H2O) 5.5 - 6.0 6.0 - 6.5 anywhere from 2 to 50% of the map unit area. Well drained Jacquet River soils support mixed softwood-hardwood stands BD (g/cm3) 1.10 1.20 of balsam fir, black spruce, red spruce, white birch, yellow Ksat (cm/hr) > 2.5 > 2.5 birch, and sugar and red maple. Forest cover on poorly drained sites is comprised of balsam fir, black spruce, cedar, red maple, AWHC (cm/cm) 0.20 - 0.30 0.20 - 0.25 tamarack and some yellow birch.

Jacquet River soils are dominated by well drained Orthic Ferro-Humic Podzols with some Orthic Humo-Ferric Podzols. 60

Climatic conditions in central New Brunswick are conducive falling within a pH(H2O) range of 4.0 to 5.0. The solum is to the development of Ferro-Humic Podzols. Ferro-humic moderate, fine to medium, granular to subangular blocky podzolization is more strongly expressed under the harsher structured and very friable. The parent material is friable to climates of the central portion of the Highlands. slightly firm. Mesoenvironmental differences due to the type of vegetation and thus the type of litter are also important in determining Jacquet River soils have been mapped with other till soils - variation in solum formation within a map unit. Well drained Popple Depot, Catamaran, Tetagouche Falls, Thibault and conditions dominate steeply sloping hilly, ridged and sloping McGee. Of these, Popple Depot is the most frequent associate. landscapes. In these landforms poorly and imperfectly drained Popple Depot soils have developed in parent materials of conditions are confined to relatively narrow drainage channels. similar lithology to Jacquet River soils. However, Popple Most of the hectarage of imperfectly drained Gleyed Depot soils have a compact subsoil. Catamaran soils also have Humo-Ferric Podzols and poorly to very poorly drained Orthic compact subsoils. Tetagouche Falls, Thibault and McGee soils Gleysols and Fera Gleysols occur in areas of undulating have developed in non-compact ablational till materials as have topography. Internal drainage is moderate to rapid (saturated Jacquet River soils. They are differentiated on the basis of hydraulic conductivity of 5 to 15 cm/hr) in the solum but coarse fragment lithologies. Tetagouche Falls is most similar, becomes moderate (2 to 3 cm/hr) in the subsoil. Available having igneous rock types, but they are richer-yielding mafic water storage capacity ranges from 0.25 to less than 0.15 volcanic rocks. Thibault and McGee soils are derived from cm/cm, decreasing with depth from surface to subsoil. Well sedimentary and metasedimentary lithologies. Jacquet River drained sites are supplied with water solely via precipitation. soils are also occasionally mapped with Big Bald Mountain, Imperfectly and poorly to very poorly drained areas have Holmesville, Juniper, Nigadoo River and Long Lake soils. developed because of a combination of topographic position, lack of gradient, and high groundwater table. Biological production on Jacquet River soils is affected by low inherent fertility, surface stoniness, climate, topography and to Solum thickness ranges from 35 to 55 cm. On well drained a lesser degree wetness. These limitations more severely sites the common horizon sequence is LFH, Ae, Bhf, Bf, BC handicap agriculture than forestry. Agricultural potential is and C. The upper horizons, LFH, Ae, and Bhf are all relatively marginal. Jacquet River soils should prove adequate to support thin (3 to 12 cm or slightly thicker) but distinct in appearance. moderately productive stands of forest tree species climatically Mineralization and humification processes in the organic layer suited to the region. are slow. The F horizon dominates over the H horizon. The light grayish coloured Ae overlies the dark reddish brown Summary of general characteristics of the Jacquet River Association coloured Bhf which in turn changes abruptly to a 10 to 25 cm Map Symbol : JR thick, yellowish brown coloured Bf horizon. The Bf horizon Physiographic Region(s) : N.B. Highlands, Chaleur Uplands grades through a transitional BC horizon into the C horizon. Elevation : 120-700 m Bedrock exposures occur in better drained more steeply Extent : 69,047 ha sloping sites with truncated profiles. Imperfectly drained Percentage of Mapped Area : 2.48% Parent Material Type : Mineral members of the Jacquet River association have a similar Mode of Origin : Glacial till, noncompact sequence of horizons, but display distinct or prominent Material Thickness : <2 m mottling in the subsoil. Gleying becomes more prominent in Soil Colour : Yellowish brown level to depressional site positions. Poorly to very poorly Family Particle Size Class : Coarse loamy Petrology (parent material) : Rhyolite and trachyte with some basalt, drained Jacquet River soils have profiles consisting of LFH or slate and greywacke O, Aeg, Bg or Bgf, and Cg horizons. The predominance of Inherent Fertility : Low coniferous forest vegetation on these sites encourages mosses Topography (slope) : Undulating, rolling and hummocky to and the accumulation of thicker organic layers. ridged, sloping and hilly (2-100%) Drainage (dominant) : Well Classification (typical) : Orthic Ferro-Humic Podzol and Orthic The Jacquet River texture profile consists of a sandy loam to Humo-Ferric Podzol loam throughout, with 8 to 18% clay content. Weathering within the solum may result in a slightly finer texture in the upper profile than in the subsoil , however, this variation is still within the sandy loam-loam grouping. Profile coarse fragment Layer Friable upper soil Subsoil material content ranges from 20 to 40%, with subangular stones, material cobbles and gravels and even some boulders. Most Jacquet Depth (cm) 0 - 45 45 - 100+ River land surfaces are moderately to very stony with stones occupying 2 to 15% of the surface area. Usually these soils are Texture Class Loam - sandy loam Loam - sandy loam also moderately to very cobbly with surface coverage similar % Sand 45 60 to that of the stones. Surface boulders are present but not in significant quantities. Jacquet River soils are low in natural % Silt 40 25 fertility. The parent rocks weather slowly and yield relatively % Clay 15 15 infertile soil material. Both the solum and subsoil are acidic 61

% Coarse 20 subangular 30 subangular S/C/G different landforms. Thin layers of Juniper till cover broad Fragments S/C/G expanses. Rampton et. al. (1984) attributed these deposits to the down wasting of dead ice which was isolated from the pH (H O) 4.5 - 5.0 4.5 - 5.0 2 main glacier as it thinned out over areas of high relief. BD (g/cm3) 1.10 1.55 Associated landforms generally consist of sloping or hilly veneers or undulating to strongly rolling blankets over Ksat (cm/hr) 5 - 15 2 - 3 similarly configured bedrock. Slopes range from 3 to 45%. Rock outcrops are common in elevated crest, upper slope or AWHC (cm/cm) 0.20 < 0.15 summit positions or along incised stream channels. Lithic phases (less than 1 m to bedrock) may have a component of residual material. The underlying bedrock is usually Devonian granite, which is also the main constituent of the Juniper till Juniper Association parent material. Glacial ice has also displaced some of these sediments to the southeast where the underlying bedrocks are The Juniper association consists of soils that have developed Silurian or Ordovician argillaceous sedimentary rock types. in thin (less than 1 m) to relatively thick (greater than 5 m) Thicker deposits of Juniper soil (some exceeding 10 m) occur deposits of acidic, coarse loamy to sandy, frequently skeletal, in valley bottoms where glacial ice was thicker and supplied noncompact morainal till derived from granite, granodiorite, more debris during melting. Associated landforms are usually diorite, granite gneiss and miscellaneous volcanics. These hummocky with short irregular slopes of 5 to 15%, but some soils occur over large blocks of land in the Central Highlands areas may be undulating to rolling in surface expression. These along the western boundary of the map area from Coldstream units are characterized by numerous randomly oriented north to Serpentine Lake (Fig.34). Elevations range from 300 drainage channels, streams, ponds and lakes. All Juniper soils to 700 m above sea level. Juniper soils cover approximately are stony and usually bouldery (Fig. 35). The valley bottom 219,273 ha, or 7.87% of the survey area. deposits are particularly bouldery on the surface with some units mapped as having boulder pavement where more than 50% of the surface area is occupied by boulders. Well drained sites support stands of red and black spruce, balsam fir, sugar and red maple, beech, yellow and white birch and some white pine. Species segregation occurs on the basis of aspect and slope position with the more tolerant species occupying the cooler lower slope and north-facing slope positions. Imperfect to poorly drained soils have forest vegetation consisting of balsam fir, black spruce, red maple, cedar, tamarack and alder.

Figure 34. Location of mapped Juniper soils.

The soils of the Juniper association have developed on ablational till materials. These ablational tills have resulted from the down wasting of glacial ice that was rich in debris. Juniper sediments are usually more stony, less compact and coarser textured than surrounding lodgment till. The materials Figure 35. Juniper soil association landscape and surface accumulated in place as the ice melted. No compacting forces stones/boulders. were involved in their deposition. Interstitial fines were flushed from the matrix by running water resulting in coarser Juniper soils have excellent internal drainage. The parent textures and accentuating the stone content. Periglacial frost material is open and porous with 30 to 40% total pore space, action also concentrated stones on the surface. Ice-contact well of which approximately one third are macro pores that permit to poorly sorted deposits such as kames and eskers are a moderate to moderately rapid (2.5 to 10 cm/hr) saturated common inclusions. Juniper soils occupy a number of hydraulic conductivity. Available water storage capacity is 62

0.10 to 0.20 cm/cm in the solum but is always less than 0.15 cm/cm and commonly less than 0.10 cm/cm in the subsoil. Better water retention capabilities in the solum are due to increased content of colloidal materials, ie. clays and fine silts due to weathering, and humus as a result of decaying plant debris. Upland Juniper soils are dominated by well drained Orthic Humo-Ferric Podzols. A thin Bhf horizon is usually present and in some cases is sufficiently developed (greater than 10 cm thick) to classify the profile as an Orthic Ferro-Humic Podzol. On well drained sites precipitation is the sole source of water. Excess water flows downward through the underlying pervious subsoil and out of the control section. In lithic phases lateral subsurface flow may occur for short durations as water moves down slope along the bedrock contact. Imperfectly and poorly to very poorly drained sites are usually found in valley bottom deposits. Imperfectly drained associates are Gleyed Humo-Ferric Podzols. Poorly to very poorly drained associates are Orthic Gleysols, Fera Gleysols or Othic Humic Gleysols. Groundwater flow is the major water source. Precipitation and subsurface flow are less important. Poorly to very poorly drained sites are confined to depressions, drainage channels and other low-lying areas. In hummocky topography there is often a sequence of well drained knolls and poorly drained depressions. Imperfectly drained conditions occur on the periphery of depressions, in lower slope positions and locally where hillslope seepage is fed by springs.

Profile development averages 40 to 55 cm in depth (Fig.36). The common horizon sequence in well drained profiles is LFH or O, Ae, Bhf, Bf, BC and C. Moss dominated O horizons usually occur in sites under coniferous forest cover. Mixed Figure 36. Well drained Juniper soil profile. wood conditions promote development of a thinner LFH horizon sequence. The organic layer varies from 5 to 10 cm in However, silt plus clay content in the upper profile is thickness but may exceed 15 cm in localized areas, especially considerably greater than in the subsoil because of ongoing where the organic debris is acidic softwood and moss litter. physical and chemical weathering processes. Poorly drained The mineral soil profile consists of a leached ashy coloured Ae depressional sites also have inwashed silts and clays from horizon of 5 to 15 cm over a thin (less than 5 cm thick) dark adjacent uplands and so their surface soil textures are often reddish brown coloured Bhf. The underlying Bf horizon is significantly finer than their subsoil texture. Clay content strong brown to yellowish brown. It becomes progressively averages less than 15% throughout most profiles. The silt:sand paler with depth grading through the BC into the light olive ratio decreases with depth. Rampton et. al. (1984) considered brown C horizon. Imperfectly drained soils have a similar that much of the weathering of these granites, which make up horizon sequence but are less pronounced in appearance and the Juniper Association parent material, was initiated before distinctly mottled. As drainage conditions worsen the Bfgj the last glaciation, as found in the Big Bald Mountain soils. horizon becomes less distinct and the total solum thickness is The profile coarse fragment content ranges from 20 to in reduced. Poorly to very poorly drained sites often have peaty excess of 50%. Angular to subrounded cobbles and stones phases with 15 to 40 cm of organic debris, usually from dominate but coarse fragments of all sizes, gravels to boulders, mosses, on the mineral soil surface. Horizon sequences consist are present. The Juniper association is very stony to of LFH or O, Ah and/or Aeg, Bg or Bgf, and Cg. The very excessively stony with 10 to 50% of the surface being dark brown or black coloured Ah horizon is usually thin but occupied by stone-sized coarse fragments. As previously under some conditions may exceed 10 cm in thickness. A dull mentioned, some areas also have boulder concentrations on the grayish leached Aeg horizon 5 to 15 cm thick overlies the B surface, with fragments ranging from 1 m to more than 4 m in horizon, which is commonly highly mottled with more than size. Juniper soils are low in natural fertility and acidic, with half of the soil material occurring as prominent iron mottles of pH(H2O) of 5.5 or less throughout the profile. The parent high chroma. Beneath this is the drab coloured parent rocks are slow to weather and yield infertile soils. The solum material. The Juniper textural profile consists of a sandy loam is usually weak to moderate, medium to fine, granular or to loam over a sandy loam to loamy sand subsoil. The acidic subangular blocky and very friable to friable while the subsoil granitic rock fragments weather to a coarse textured material. is weak, fine to medium subangular blocky to structureless and 63 friable. No significant root or water restricting soil layers Layer Friable upper soil Subsoil material occur within the profile. Ortstein, a cemented hardpan material formation, may be present in the B horizon but it is discontinuous and sporadic in occurrence. Depth (cm) 0 - 45 45 - 100+ Texture Class Sandy loam - loam Sandy loam - loamy Juniper soils have been mapped in proximity to several soil sand associations, but are most closely associated with the Catamaran and Tuadook soils, which are lithologically similar. % Sand 55 70 However, both the Catamaran and Tuadook soils have % Silt 33 20 developed in lodgment till and as such have dense compact subsoils whereas the Juniper subsoil is friable. The differing % Clay 12 10 modes of deposition have also resulted in Juniper being coarser % Coarse 25 subangular 35 subangular C/S/G textured and somewhat stonier than the other two. Soils such Fragments C/S/G as Gagetown, which have developed on glaciofluvial pH (H O) 4.5 - 5.0 5.0 sediments, are also common in some of the undulating to 2 hummocky Juniper deposits found in valleys bottoms. In more BD (g/cm3) 1.00 1.60 steeply sloping landscapes with veneer-thick soil materials, Juniper is commonly mapped with Big Bald Mountain. Big Ksat (cm/hr) 5 - 15 2 - 3 Bald Mountain is a residual soil, having developed directly as AWHC (cm/cm) 0.10 - 0.20 < 0.10 a result of the in situ weathering of the granitic bedrock. Juniper, as a till soil, is a heterogenous mixture of glacial debris ranging from silts and clays to boulders. Lithologically, Juniper is are also more diverse with diorites, granodiorites, Lavillette Association granite gneiss, volcanics and miscellaneous sedimentary and metamorphic coarse fragments in addition to the feldspar rich The Lavillette Association consists of organic soils that have granites. Juniper soils are also mapped with Long Lake and developed on deep (average thickness greater than 1.6 m), McGee soils along some sedimentary and metasedimentary- ombrotrophic domed bogs (Tarnocai 1981). They are mapped granitic bedrock boundaries. only in the Maritime Plain portion of the survey area (Fig. 37). Landform conditions vary from nearly level to very gently Juniper soils suffer from excessive stoniness and boulderiness, rolling, slopes of 2% or less being dominant. Lavillette soils droughtiness and to some degree rockiness. In many situations occupy 26,811 ha or 0.96% of the area. topographic conditions are also detrimental to potential land uses. While some localized areas may be the exception to the rule, Juniper soils as a whole have little or no potential for agricultural use. There soils should remain under forest. Forest management of these soils should take into account the droughty nature and low to very low inherent fertility on these materials, and where soils are shallow to bedrock or excessively stony on the surface, must consider the rather delicate nature of the ecosystem.

Summary of general characteristics of the Juniper Association

Map Symbol : JU Physiographic Region(s) : N.B. Highlands Elevation : 300-700 m Extent : 219,273 ha Percentage of Mapped Area : 7.87% Parent Material Type : Mineral Mode of Origin : Glacial till, noncompact Material Thickness : <1 - >5 m Soil Colour : Yellowish brown to brown Family Particle Size Class : Coarse loamy to sandy skeletal Petrology (parent material) : Granite, granodiorite, diorite, granite Figure 37. Location of mapped Lavillette soils. gneiss and some volcanics Inherent Fertility : Low As the name implies, domed bogs are typified by convex Topography (slope) : Undulating, rolling and hummocky to surfaces or domes. As most of the bog surface is raised above sloping and hilly (2-70%) Drainage (dominant) : Well the level of the surrounding terrain it is virtually unaffected by Classification (typical) : Orthic Humo-Ferric Podzol any nutrients in ground waters from adjacent mineral soils. Most deposits consist of the following zones: a central dome zone (also referred to as core); a slope zone with a flark 64 subzone; and a marginal zone (Airphoto Analysis Associates of 4.5), high bulk density (greater than 0.3 g/cm3) and ash Consultants Ltd. 1975). The dome or core zone is charac- content (30%) values, and very slow permeabilities (saturated terized by depths of as great as 5 to 10 m. The slope zone hydraulic conductivity of less than 0.1 cm/hr). borders the dome and extends to the almost-level marginal zone. A flark subzone occurs within the slope zone, Natural drainage varies little with site position on the bog. The immediately adjacent to the dome. It is characterized by a dome, slope and marginal zones are all very poorly drained distinctive arrangement of ridges with interspaced flashets that (Fig. 38). The water table is at or near the surface throughout forms a circular pattern, oriented perpendicular to the direction the year. Groundwater in bogs is extremely acid and low in of slope. The marginal zone or lagg, composed of relatively nutrients, even in lagg areas. shallow peat materials (usually less than 1 m in thickness), borders the bog, forming a transition from organic deposit to mineral soil. Wide lagg areas dissected by small streams are common. The marginal zones vary from the core and slope zones in that they are generally influenced to some degree by the nutrients in seepage waters from the surrounding mineral soils.

Lavillette deposits are usually void of significant tree cover. Bog domes and slopes are covered with sphagnum and feather mosses and ericaceous shrubs, but scattered dwarf black spruce and larch are common. Lagg areas are generally open and support sedge species in addition to mosses and shrubs. Dense stands of stunted black spruce and larch occupy the lagg to mineral soil transition zones. Figure 38. Lavillette soil association landscape. Peat stratigraphy usually consists of a surface layer 0.5 to greater than 4.0 m thick of fibric (weakly decomposed) sphagnum peats overlying a layer 0.3 to 2.0 m thick of mostly mesic Lavillette soils are mainly Typic, and some Mesic, Fibrisols on (moderately decomposed) and some humic (well-decomposed) the dome and slope zones with Terric Mesic or Humic sedge-sphagnum peats which grade into pure sedge peats. This Fibrisols on the marginal zone. Typic Fibrisols have material in turn is underlain by a relatively thin, confined, dominantly fibric middle and bottom tiers. Some minor layers basal layer of sedimentary peat. of mesic material occur, usually in the deeper portions of the profile. Where subdominant mesic layers have a total The surface fibric layer is dominated by sphagnum mosses, thickness greater than 25 cm in the middle and bottom tiers the readily identifiable as to origin because they are only slightly soils are classified as Mesic Fibrisols. Bog margin or lagg decomposed. The remains of shrubby plants are also zones have shallow (usually less than 160 cm) thickness of commonly found in this layer and may account for as much as organic material, consisting of fibric sphagnum peats over 20% by volume. In general this surface layer is composed of mesic or humic sedge-sphagnum peats. They are classified as materials that have a brown to dark reddish brown colour, an Terric Mesic or Humic Fibrisols. extremely acid reaction (pH in H2O of less than 4.0), low bulk densities (less than 0.075 g/cm3), moderately rapid to rapid Lavillette soils are associated with other organic soils as well permeabilities (saturated hydraulic conductivity of greater than as with poorly and very poorly drained members of some 10 cm/hr), and high contents of rubbed fibre with class 1 to mineral soils. Acadie Siding is an organic associate which class 4 ratings on the von Post scale of decomposition. The differs from Lavillette soils in that it consists of soils on middle layer is dominated by sedges (Carex spp.) with lesser less-developed peatland deposits--mostly shallow (less than 1.6 amounts of sphagnum mosses. These materials are at an inter- m of organic material) Terric Mesisols (moderately mediate to advanced stage of decomposition. They have a decomposed) or Humisols (well decomposed). Acadie Siding brown to dark brown colour, an extremely acid to acid reaction soils lack the pronounced circular surface pattern of Lavillette soils. Very poorly or poorly drained Barrieau-Buctouche, - (pH in H2O of less than 4.0), moderate to high bulk densities (greater than 0.15 g/cm3), moderate to very slow permeabilities Reece, Richibucto, Stony Brook and Tracadie soils are also (saturated hydraulic conductivity of less than 2 cm/hr), and commonly found with Lavillette soils. Mineral soils may have moderate to low contents of rubbed fibre with von Post scale surface layers of fibric organic material up to 60 cm thick and of decomposition class 5 to class 8. still be considered mineral soils. The boundary between Lavillette organic soils and adjacent mineral soils is, in most The basal layer of sedimentary peat or ooze is composed of places, abrupt and obvious. coprogenous earth, which is aquatic plant debris modified by aquatic animals. Very few or no plant remains are Lavillette soils are considered non-productive woodland. They recognizable to the naked eye. It usually has a dark brown to have potential agricultural uses for vegetable crop production but require specialized management practices and equipment. very dark grayish brown colour, an acid reaction (pH in H2O 65

Lavillette soils are often used as sources for peat moss and particle sizes ranging from silts and clays to stones and related products. boulders. Clast shapes are a function of the parent bedrock. Coarse fragment content is particularly high where weathered bedrock has been incorporated into thin veneer deposits. Long Summary of general characteristics of the Lavillette Association Lake soils are very stony on the surface, with 3 to 15% of the land area occupied by coarse fragments. In imperfectly and Map Symbol : LV Physiographic Region(s) : Maritime Plain poorly drained sites frost action frequently concentrates profile Elevation : < 150 m cobbles on the mineral soil surface under the forest floor. Extent : 26,811 ha Boulders are common but usually not in sufficient quantities Percentage of Mapped Area : 0.96% to warrant designation as a bouldery phase. Long Lake Parent Material Type : Organic Mode of Origin : Domed bog landforms are dominated by undulating, and rolling surface Material Thickness : >1.6 m over mineral soil expressions with slopes varying from less than 3% to in excess Soil Colour : Brown to dark reddish brown of 30%. Some hilly, ridged or sloping map units with slopes Degree of Decomposition : Weakly decomposed of up to 70% also occur. The soils are relatively uniform in Botanical Composition : Sphagnum peat Inherent Fertility : Very low thickness and bedrock outcrops are not all that common. Topography (slope) : Domed (<1.5%) in an undulating Those bedrock exposures that do occur are found on landscape (<5%) topographic highs and summits or along steeply inclined Drainage (dominant) : Very poor drainage channels that are deeply incised into the bedrock. Classification (typical) : Typic Fibrisol Bedrock exposures often consist of more resistant strata that weather at a slower rate than adjacent rock. Well drained soils of the Long Lake association support forest communities of Layer Friable upper soil Subsoil material material black spruce, balsam fir, yellow and white birch, red oak, white pine, and sugar and red maple. On poorly to very poorly Depth (cm) 0 - 60 > 60 drained sites the tree vegetation consists of black spruce, balsam fir, red maple, cedar and some tamarack and yellow Von Post rating 1 - 3 2 - 4 birch.

% Wood 5 5

pH (H2O) < 4.0 < 4.0

BD (g/cm3) < 0.05 0.08

Ksat (cm/hr) 50 20

AWHC (cm/cm) 0.10 0.10

Long Lake Association

The Long Lake association consists of soils that have developed in relatively thin (mostly less than 2 m thick) deposits of acidic, coarse loamy, compact morainal till derived from slate, siltstone, argillite, schist, quartzite and greywacke. They occur mostly in the Central Highlands physiographic region of the study area, and to a lesser extent in the Chaleur Uplands, at elevations of 300 to 700 m above sea level (Fig. Figure 39. Location of mapped Long Lake soils. 39). Long Lake soils occupy approximately 262,504 ha, or 9.42% of the map sheet. Well drained Long Lake soils are mostly Orthic Ferro-Humic Podzols (Fig. 40) with some Orthic Humo-Ferric Podzols. The soil parent material has been deposited as ground moraine, Climatic conditions in central New Brunswick are conducive plastered in place under the weight of advancing glacial ice. to the accumulation of organic matter in the podzolic B Composition strongly reflects the incorporation of local horizon. Most macro and meso environmental conditions are bedrock formations. Thin surficial mantles of ablational till, such that Long Lake soils have enough organic carbon content usually McGee material, are common, but their identification to qualify for the Ferro-Humic Podzols great group. The is difficult. The McGee and Long Lake parent materials are remaining well drained soils are Humo-Ferric Podzols. similar in composition and mixing actions during soil Ferro-humic podzolization is not as strongly expressed along formation have modified the upper soil profile, obliterating the eastern periphery of the Long Lake range where the most evidence of multiple till layers. The till is a Central Highlands merge with the Maritime Plain. heterogeneous mixture of flat, angular to subangular shaped Humo-Ferric Podzols dominate the Maritime Plain, which has 66 a slightly milder climate than the Highlands. result of increased weathering and/or siltation. Profile coarse Mesoenvironmental differences due to the type of vegetation fragment content averages 20 to 40%, with a preponderance of and thus the type of litter are also important in determining flat, horizontally lying channers, gravels and flagstones. In variation in solum formation within a map unit. Well drained lithic phases uplifted fragments of fractured bedrock increase conditions dominate steeply sloping hilly and rolling the percentage of coarse fragments in the lower profile. Long landscapes. In these landforms poorly and imperfectly drained Lake soils are medium in inherent fertility, but acidic conditions are confined to relatively narrow drainage channels. throughout, with pH(H2O) values of 4.0 to 5.5. The friable to Significant hectarages of imperfectly drained Long Lake soils very friable, weak to moderate, fine to medium, granular or occur as Gleyed Humo-Ferric Podzols in areas of undulating subangular blocky solum overlies a firm to very firm, massive, and gently rolling topography, where they are found in breaking to medium subangular blocky, subsoil. The subsoil association with both well drained or poorly drained associates. shatters readily upon extraction. Poorly drained soils of the Long Lake association are Orthic Gleysols. Internal drainage is restricted by a slowly to moderately slowly permeable subsoil with an estimated saturated hydraulic conductivity value of 0.1 to 1.0 cm/hr. Available water storage capacity ranges from 0.20 to 0.10 cm/cm, decreasing with depth because of reduced total porosity in the compact subsoil. Well drained sites are supplied with water solely via precipitation. Downward movement of excess moisture through the profile is impeded by the subsoil so some lateral flow occurs for short durations. Imperfectly and poorly to very poorly drained areas have developed because of a combination of topographic position, lack of gradient, subsoil compaction, seepage and high groundwater table.

Soil development varies from 45 to 60 cm in thickness. The common horizon sequence on well drained sites is LFH or O, Ae, Bhf, Bf, BC and C. O horizons are common under coniferous forests where mosses dominate the ground vegetation. The organic layer is 5 to 15 cm thick, becoming more humified with depth. It overlies a thin to moderately thick (5 to 20 cm), ashy coloured Ae horizon which breaks abruptly into the B horizon. The upper dark brown to dark reddish brown Bhf horizon varies from 5 to 20 cm in thickness. It merges with the strong brown to yellowish brown Bf horizon which gradually grades into the oxidized olive brown parent material. Morphological appearance may be deceptive. Significant amounts of translocated iron and aluminum are often present in horizons that display little colour change from the parent material. On the other hand, organic coatings on coarser textured Bf horizons give the impression of more organic matter than is actually present. Imperfectly drained soils have similar arrangements of profile Figure 40. Well drained Long Lake soil profile. horizons but are modified because of periodic saturation. They are mottled in the B and C horizons, especially a thin zone The Long Lake association is most commonly found with immediately above the compact subsoil where water is members of the McGee association. The two soils have been perched. The Ae horizon is often irregular or broken because derived from materials of similar lithological origin. They are of tree uprooting due to windthrow. An Ahe horizon up to 10 also alike in many other physical, chemical and morphological cm thick may be sandwiched between the H and Ae horizons features. Differentiation is primarily made on the basis of in imperfectly drained Long Lake soils. Poorly to very poorly subsoil compaction, and associated characteristics. Long Lake drained horizon sequences lack a podzolic B horizon. They subsoils have firm to very firm consistence, high bulk density consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The (greater than 1.75 gm/cm3) and voids consisting predominantly forest duff layer is usually thicker than found in well drained of micro pores. McGee subsoils are friable (to slightly firm), counterparts. The Long Lake textural profile consists of a lower in bulk density (usually less than 1.55 gm/cm3) and have loam or silt loam to sandy loam (8 to 18% clay) throughout, a higher proportion of macro pores. Along transition zones but the solum is often slightly finer textured (higher in silt and Long Lake soils have also been mapped in complexes with a clay content) than the subsoil. This is most obvious in number of other soils: Tetagouche, Jacquet River, Holmesville, imperfectly to poorly drained sites and is considered to be the Violette, Popple Depot, Juniper, Reece, Catamaran, and 67

Tuadook soils. New Brunswick Highlands, Chaleur Uplands and Notre Dame Mountains physiographic regions at elevations ranging from Excluding problems due to wetness in imperfectly and poorly 200 to 500 m above sea level (Fig. 41). Maliseet soils cover drained locations, the dominant features affecting land use are approximately 3,332 ha or 0.12% of the map area. They occur related to topography (excessive slope), coarse fragment in small, scattered tracts. content (both surface and profile) and the presence of a subsoil restricting layer which impedes root penetration and water percolation. Long Lake soils are moderately fertile and so produce respectable stands of most tree species that are climatically suited.

Summary of general characteristics of the Long Lake Association

Map Symbol : LL Physiographic Region(s) : N.B. Highlands, Chaleur Uplands Elevation : 300-700 m Extent : 262,504 ha Percentage of Mapped Area : 9.42% Parent Material Type : Mineral Mode of Origin : Glacial till, compact Material Thickness : <2 m Soil Colour : Olive brown Family Particle Size Class : Coarse loamy Petrology (parent material) : Slate, siltstone, agrillite, schist and some quartzite and greywacke Inherent Fertility : Medium Topography (slope) : Rolling and undulating to sloping and hilly (0.5-45%) Figure 41. Location of mapped Maliseet soils.. Drainage (dominant) : Well to moderately well Classification (typical) : Orthic Ferro-Humic Podzol and Orthic Humo-Ferric Podzol Maliseet soil parent materials were deposited as river terraces and are level to gently undulating with steep slopes between terraces. As such, they tend to be elongated deposits found in narrow strips along river and stream courses. Deposition has Layer Friable upper soil Subsoil material been by waters flowing at moderate velocity. Velocity of the material flowing water determined the size of the particles that were Depth (cm) 0 - 50 50 - 100+ deposited. Suspended particles were deposited when water turbulence ceased to exceed their settling velocities, a function Texture Class Loam Loam - sandy loam of particle diameter, shape and specific gravity, and fluid density. Most sediments consist of well rounded fine to % Sand 45 50 medium sand grains with varying amounts of silt. Changes in % Silt 39 38 stream velocity resulted in layers of varying thickness and particle size. Some gravel transport and deposition occurring % Clay 16 12 during periods of faster than normal streamflow have lead to % Coarse 20 flat, subangular 30 flat, subangular the inclusion of the occasional gravelly layer within Maliseet Fragments C/G/S C/G/S materials. Maliseet landscapes are variable in that they consist of terrace surfaces, with horizontal or gently inclined planes (0 pH (H O) 4.5 - 5.0 5.0 - 5.5 2 to 3% slope) separated by scarp faces (15 to 45% slope). BD (g/cm3) 1.10 1.75 Maliseet soils support mixed wood stands of balsam fir, black spruce, white pine, white birch, trembling aspen, white elm and Ksat (cm/hr) 2.5 - 10 0.1 - 1.0 white ash on the drier well drained sites. Moist sites along AWHC (cm/cm) 0.15 - 0.20 0.10 - 0.15 stream bottoms and lower terraces have cedar, black spruce, tamarack, red maple, white elm, speckled alder and black ash.

The Maliseet association consists of rapidly to well drained Maliseet Association Orthic Humic-Ferric Podzols, imperfectly drained Gleyed Humo-Ferric Podzols and Gleyed Eluviated Dystric Brunisols, The Maliseet association consists of soils developed in and poorly to very poorly drained Gleyed Eluviated Dystric relatively thick (3 m plus) deposits of acidic, sandy to coarse Brunisols and Orthic Gleysols and occasionally Rego Humic loamy fluvial (ancient alluvium) or possibly glaciofluvial Gleysols under very poorly drained conditions. On well material derived from slate, shale and miscellaneous quartzite drained sites water is supplied only by precipitation. Maliseet and volcanic rock types. Maliseet materials are underlain at soils have moderate available water storage capacity in the depth by the regionally prevailing till. They are found in the solum, (0.20 to 25 cm/cm), but it decreases to as little as 0.10 68 cm/cm or less in the subsoil. Finer textures and higher levels separated on percent coarse fragment content. Grand Falls and of organic matter content aid water retention in the upper Muniac soils usually have 50 to 70% gravels in the subsoil solum. Imperfectly and poorly drained sites are mostly while Maliseet soils have less than 20% gravels and usually restricted to lower terraces along valley floors. In these sites, less than 5%. Interval soils occupy similar soil landscapes to groundwater presence is the determining factor in soil Maliseet soils, but Interval soils are distinctly finer-textured drainage. Impeded drainage may also occur on some upper than Maliseet soils. Interval soils are also restricted in terraces at the base of the transition slope from the above occurrence to flood plains. terrace. Subsoil permeability varies from 1.0 cm/hr to more than 10 cm/hr. This wide range is due to parent material Maliseet soils are productive for both agricultural and forestry stratification. The C horizon is made up of layers of sandy crops. They respond to fertilizer treatments and the solum loam, loamy sand, fine gravel and silt. Most layers are texture is generally fine enough to have adequate water- moderately rapidly permeable. holding capacity. Medium natural fertility is an asset in forestry. Soil development in Maliseet materials ranges from 30 to 50 cm in thickness, but is typically less than 40 cm. Moderately Summary of general characteristics of the Maliseet Association well to imperfectly drained sites have the deepest solum Map Symbol : MA development. These sites have more suitable moisture regimes Physiographic Region(s) : Chaleur Uplands for biological production and soil formation. The horizon Elevation : 200 to 500 m sequence in well to rapidly drained soils is typically: LFH, Ae, Extent : 3,332 ha Bhf, Bf, BC and C. The Bhf horizon is thin and poorly Percentage of Mapped Area : 0.12% Parent Material Type : Mineral developed. Imperfectly drained profiles have LFH, Ae, Bfgj, Mode of Origin : Fluvial (ancient alluvium) BCgj and Cg horizons. Poorly to very poorly drained profiles Material Thickness : > 3 m have a number of different possible profiles: LFH, Ae, Bmgj, Soil Colour : Olive brown to yellowish brown BCg and Cg; or LFH or O, Aeg, Bg and Cg; or, very thin LFH Family Particle Size Class : Sandy to coarse loamy Petrology (parent material) : Slate, shale and miscellaneous quartz and or O, Ahg, BCg and Cg. Weathering has resulted in the volcanics surface soils having more fines (silt and clay) than is found in Inherent Fertility : Medium the subsoil. Windthrow, frost action and biological activity Topography (slope) : Undulating or terraced (2-15%) have obliterated any stratification that may have originally Drainage (dominant) : Well Classification (typical) : Orthic Humo-Ferric Podzol been present in the solum. The Maliseet texture profile grades from a fine sandy loam to sandy loam solum into a loamy sand to sandy loam subsoil. Clay content only exceeds 10% in the upper solum. Coarse fragments are few. Where they do occur Layer Friable upper soil Subsoil material they are usually fine gravels of slate, shale and quartzite. material Maliseet soils are medium to low in natural fertility and acidic Depth (cm) 0 - 35 35 - 100+ throughout the profile, with a range in pH (H2O) of 4.0 to 5.5. The exception to this is found in some poorly to very poorly Texture Class Fine sandy loam Fine sandy loam - drained sites in which the subsoil pH is elevated to 6.5 or even fine loamy sand higher as a result of inwashing of carbonates from surrounding calcareous soil parent materials and/or bedrocks. The parent % Sand 60 80 material colour is olive gray. In well drained sites the solum % Silt 25 10 consists of a thin LFH layer overlying a leached light gray coloured Ae horizon. The underlying B horizon consists of a % Clay 15 10 thin (less than 5 cm thick) reddish brown Bhf horizon over a % Coarse 5 rounded G 5 rounded G dark to yellowish brown Bf horizon that becomes Fragments progressively yellower in hue with depth. Imperfectly and poorly drained soils have iron (Fe) mottling or gleyed colours pH (H2O) 4.5 - 5.0 5.0 - 5.5 of low chroma, or both. The subsoils are loose and single BD (g/cm3) 1.00 1.45 grain or structureless but stratified. The A horizon is friable to very friable, very weak, fine platy. Most B horizons are very Ksat (cm/hr) 5 - 10 1 - 10 friable, weak to moderate, fine granular. Very poorly drained AWHC (cm/cm) 0.20 - 0.25 0.10 profiles may be restricted to a moderately thick (15 to 20 cm) Ah horizon over a thin transitional BC horizon that grades into the subsoil at 30 to 40 cm depth.

Maliseet soils are usually associated with other soils developed McGee Association in fluvial sediments, such as Grand Falls and Muniac. Maliseet, Grand Falls and Muniac are lithologically similar, The McGee association consists of soils that have developed but both Grand Falls and Muniac are sandy skeletal, i.e., in relatively thin (most less than 2 m thick) deposits of acidic, gravelly or very gravelly in the parent material. They are coarse loamy to loamy skeletal, noncompact, "water- 69 reworked" morainal till derived from slates, argillite, schist, the surface and as such are considered as nonrocky. greywacke and quartzite. McGee soils are found throughout Significant occurrences (2 to 25% surface area) of bedrock the Central Highlands, Chaleur Uplands and Notre Dame exposures are confined to sloping, hilly and ridged conditions. Mountains physiographic regions of the study area at Well drained sites support stands of white and yellow birch, elevations ranging from 300 to 800 m above sea level (Fig. sugar maple, black and red spruce, and balsam fir. Poorly to 42). They occupy large, extensive areas totalling some very poorly drained sites are found in low-lying depressions 417,254 ha which represents 14.97% of the map area. and drainage channels. Natural vegetation consists of water tolerant and frost hardy species such as black spruce, balsam fir, tamarack, cedar, red maple and alder.

The McGee association is dominated by well drained Orthic Ferro-Humic Podzols (Fig. 43) and Orthic Humo-Ferric Podzols. Podzolization is strongly expressed. The colder climate of central New Brunswick results in greater effective precipitation and hence the formation of a podzolic B horizon with appreciable amounts of organic matter accumulation. In some locations the organic carbon content of McGee B horizons straddles the taxa boundary. Where organic carbon levels in 10 cm or more of the B horizon meet the requirements of a Bhf (greater than 5% organic C), the profile is classified as a Ferro-Humic Podzol, otherwise it is a Humo-Ferric Podzol. It was not possible to separate these two great groups into homogeneous units at the level of mapping undertaken in this project. Imperfectly drained McGee soils are classified as Gleyed Humo-Ferric Podzols. Poorly to very poorly drained Figure 42. Location of mapped McGee soils. members are Orthic or Rego Gleysols. Where mapped, imperfectly and poorly to very poorly drained McGee soils are The origin or mode of deposition of McGee parent material is usually subdominant components of units dominated by well variable. It consists of morainal till sediments, probably both drained McGee soils. They also occur as predictable ablational and lodgment debris, that has been reworked to inclusions in units mapped solely as well drained. Well varying degrees by either water, periglacial action or colluvial drained sites occur on crest to middle or lower slope positions, action, alone or in combination. As the glaciers ablated, depending upon topographic conditions. Where slopes are materials within the ice were deposited. Melt waters also steep, the transition from well drained to poorly or very poorly modified previously deposited glacial sediments of lodgment drained is quite abrupt. Imperfectly drained areas are usually (basal) till, removing fines, weakly stratifying some surficial associated with rolling to undulating landscapes. Poorly to materials, etc. Periglacial environments on the margins of very poorly drained sites occupy drainage ways. McGee soils waning glacial ice sheets were characterised by cold have good internal drainage. The subsoil is pervious, and temperature climates in which frost action was an important based on pore size distribution, should be moderate to factor. Original parent material conditions were altered by moderately slow in permeability (1.0 to 5 cm/hr saturated frost heaving due to ice lense formation caused by freezing. hydraulic conductivity). Available water storage capacity is Deep frost penetration helped to loosen compacted basal till 0.20 to less than 0.10 cm/cm, decreasing with depth. sediments. Colluvial action, gravity induced movement on Precipitation is the sole source of water on well drained sites. steeply sloping surfaces, is an on-going process that has further Excess water readily flows downward through the profile and modified some McGee materials. These colluvial materials are into the underlying bedrock, which is usually weathered and associated with site positions at the base of steep slopes or fractured on the surface. However, under periods of excessive cliffs. They consist of sediment that strongly resembles the till moisture supply, some lateral flow may occur along the parent material but may be poorly sorted or stratified. McGee bedrock surface. Excess water in poorly drained sites is the materials occupy mostly rolling to hilly landscapes with gentle result of high groundwater levels and inflow of seepage water to very strongly sloping gradients of 5 to 45%. Most deposits from adjacent uplands. Soil drainage status is largely a are either veneers or blankets, ie. less than 2 m thick, and so function of topographic position. conform to the configuration of the underlying bedrock. Thicker sediments usually occur on lower slope positions. Profile development averages 40 to 60 cm in depth. The McGee soils are also found on steeply sloping banks of common horizon sequence in well drained profiles is: LFH or streams that are deeply incised into the bedrock. Here, some O, Ae, Bhf, Bf, BC and C. Under mixed woods the forest slopes may be in excess of 70%. Lessor areas of McGee soils floor layer is LFH, but under softwood stands, O horizons of occur on undulating, ridged and hummocky landscapes. peaty mors develop. The grayish coloured Ae horizon is often Shallowness to bedrock and bedrock exposures are an inherent 10 to 20 cm thick, tonguing into the brown to dark reddish characteristic of McGee map units. On undulating to rolling brown upper B horizon (Bhf). The Bhf horizon varies from 2 landscapes, however, exposures usually cover less than 2% of to 15 cm in thickness. The underlying Bf is a dark brown to 70

mottles occur. The Ah horizon is usually thin or absent. Under very poorly drained conditions there may be no horizonation apart from evidence of gleying. The McGee textural profile varies from a loam or sandy loam to a silt loam. Texture may vary considerably from profile to profile as well as within the profile. Some profiles are relatively well sorted, others are not. One peculiarity in the McGee texture profile is the high silt content in the Ae horizon compared to underling horizons. Percentage silt in the Ae may be more than twice that of the B and C horizons. This is attributed to a combination of weathering of coarser sized particles and differential movement of soil constituents within the profile. Frost action has caused disintegration of rock fragments into silt sized particles and percolating waters have translocated some of the clay fraction into the B horizon. The profile coarse fragment content averages 20 to 50% flat to subangular, gravels, cobbles and stones. Veneer phases may exceed this range. The coarse fragments are derived mainly from hard, tough, firmly indurated rock types such as slate, greywacke and quartzite. Some deposits, however, contain large quantities of weathered chloride-mica schist and argillite. Most landscapes are very stony with 3 to 15% of the surface area occupied by stones 1 to 2 m apart. Boulders, fragments greater than 1 m in diameter, are common. McGee soils are medium to low in

natural fertility and acidic, pH(H2O) 4.0 to 5.5. No root or water restricting soil layers occur within the profile. The solum is mostly moderate, medium granular and friable to very friable. The subsoil is weak, fine to medium subangular blocky and friable providing a deep porous well aerated potential rooting zone. Ortstein, cementation in the Bf or Bhf horizon, may occur, but only sporadically. It has little effect on land use.

McGee soils have been mapped in complex units with numerous other soils including Long Lake, Thibault, Holmesville, Catamaran, Jacquet River, Juniper, Popple Depot, Tetagouche, Tetagouche Falls and Violette, however, they are most commonly associated with the first three soil associations. Long Lake is texturally and lithologically very similar to McGee. The two soils are differentiated on the basis of subsoil compaction. Long Lake has a firm, dense compact subsoil. McGee subsoil is noncompact. Thibault is also similar in physical characteristics to McGee. One of the major differences that separates these two soil associations is soil reaction. Thibault soil parent materials are neutral. They have been derived from weakly calcareous shales, slate, quartzite, Figure 43. Well drained McGee soil profile. argillite and sandstone. Like Long Lake, Holmesville soils are developed on lodgment till parent material and have compact dark yellowish brown, becoming progressively yellower as it subsoils. grades into the BC. The McGee parent material is usually olive brown. Colouration is often deceptive, indicating less Major soil and landscape features affecting land use of McGee soil development than is confirmed by chemical analysis. soils include excessive stoniness, shallowness to bedrock and Other than being mottled and having thin (less than 5 cm thick) slope steepness. These limitations place significant restrictions Bhf formation, imperfectly drained sites are similar in on potential agricultural usage. Excluding poorly drained appearance to their well drained counterparts. An Ahe horizon conditions, McGee soils should be good to fair in terms of up to 5 cm thick may also be sandwiched between the H and forest production of suitable species such as white and black Ae horizons in imperfectly drained McGee soils. Poorly spruce, balsam fir, jack pine, birch and maple. drained profile sequences usually consist of O, (Ah), Aeg, Bg and Cg. The colours are dull with low chromas and prominent 71

Summary of general characteristics of the McGee Association level. Esker deposits are long, narrow, low, sinuous, ridges or mounds. Most sediments consists of well stratified sands and Map Symbol : MG Physiographic Region(s) : N.B. Highlands, Chaleur Uplands, Notre gravels with some cobbles. The soil and rock fragments are Dame Mountains smooth and rounded. The layers or strata vary in thickness and Elevation : 300-800 m composition, a reflection of the changing environmental Extent : 417,254 ha conditions during which they were deposited. Muniac soils are Percentage of Mapped Area : 14.97% Parent Material Type : Mineral nonstony. Mode of Origin : Glacial till, noncompact Material Thickness : <2 m Soil Colour : Olive to olive brown Family Particle Size Class : Coarse loamy Petrology (parent material) : Slate, agrillite, schist, greywacke and quartzite Inherent Fertility : Medium Topography (slope) : Undulating and rolling to sloping and hilly (2-100%) Drainage (dominant) : Well Classification (typical) : Orthic Ferro-Humic Podzol and Orthic Humo-Ferric Podzol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 50 50 - 100+

Texture Class Loam (sandy loam Sandy loam or silt loam)

% Sand 40 60 Figure 44. Location of mapped Muniac soils.

% Silt 45 25 The major forest species on well to rapidly drained sites are % Clay 15 15 black spruce, balsam fir, white birch, white pine, trembling aspen, red maple and yellow birch. Poorly to very poorly % Coarse 25 flat, subangular 35 flat, subangular drained lower slopes and depressions support communities of Fragments G/C/S G/C/S cedar, tamarack, black spruce, willow and balsam fir.

pH (H2O) 4.5 - 5.0 5.0 - 5.5 The Muniac Association is dominated by well to rapidly BD (g/cm3) 1.10 1.55 drained Orthic Humo-Ferric Podzols. Gleyed Humo-Ferric Ksat (cm/hr) > 10 > 10 Podzols occupy imperfectly drained sites, and Gleyed Humo-Ferric Podzols, Gleyed Eluviated Dystric Brunisols, AWHC (cm/cm) 0.15 - 0.20 0.10 Orthic Gleysols and Rego Humic Gleysols occur on poorly to very poorly drained sites. The subsoil parent material is rapidly pervious (usually greater than 10 cm/hr). Excess precipitation readily flows downward through the profile. Muniac Association Upper solum water holding capacities are enhanced by their finer texture (gravelly loam to gravelly sandy loam) and the The Muniac Association consists of soils developed in thick presence of organic matter. Here, water storage capacities may deposits (often in excess of 20 m) of neutral, sandy skeletal, reach 0.20 cm/cm. The available water storage capacity glaciofluvial material with calcareous to weakly calcareous decreases with depth. Muniac soils have low available water slate, shale, quartzite and sandstone coarse fragments. The storage capacity within the subsoil, averaging 0.10 cm/cm or glaciofluvial material is underlain by glacial till or bedrock. less. Precipitation is the sole source of water on well drained These soils occur in small tracts scattered throughout the sites. Off-drainage (imperfect, poor and very poor drainage) Chaleur Uplands and New Brunswick Highlands regions of the is the result of high ground water tables and groundwater flow. survey area (Fig. 44). Muniac association soils cover Most Muniac soils are either dry (well to excessively drained) approximately 2,450 ha or 0.09% of the map area. or wet (poorly to very poorly drained). Areas of imperfect drainage are restricted to subdominant components of map Muniac soils usually occur in old river terraces or as eskers. units of the above mentioned drainage categories. The topography varies from undulating to terraced, with horizontal or gently inclined terraces separated by steeply The depth of the solum of Muniac Association soils varies sloping scarp faces. The terraces are long, narrow surfaces from 25 to 50 cm. Thickest solum development is found on running parallel to streams and rivers, marking a former water well to imperfectly drained sites. Sites with moisture regimes 72 at the extremes, either excessively dry or excessively wet, tend Maliseet are coarse loamy nonskeletal materials, i.e., they lack to have shallower solum development. The common horizon the gravel content of Muniac soils. Grand Falls soils have sequence in well to rapidly drained soils is: LFH, Ae, Bf, BC developed on gravelly glaciofluvial materials, but they have and C. At higher elevations where there is greater effective been derived from non-calcareous rock types. precipitation, increased accumulation of organic matter in the upper podzolic B horizon leads to the formation of a thin Bhf Biological production on Muniac soils is limited by low horizon. Imperfectly drained profiles have: LFH, Ae, Bfgj, fertility retention and low water holding capacity. Excessive BCgj and Cg horizons, indicating the presence of distinct or wetness is an additional problem on poorly drained sites. prominent mottles. Poorly to very poorly drained soils have Where surface textures and organic matter enhance water horizons sequences of: LFH, Ae, Bmgj or Bfjgj and Cg; LFH retention, Muniac soils are productive for some agricultural or O, Aeg, Bg and Cg; or LFH, Ah and Cg as drainage gets crops, this primarily being because they are quick to dry and progressively worse. The stratification so characteristic of the warm up in the early spring. Muniac soil parent material is an soil parent material is not present in the solum. Mixing actions excellent source of aggregate for road building, construction of soil organisms, frost churning and tree uprooting and related uses. It is extracted for local use from numerous (windthrow) have altered the upper soil profile, obliterating sites. any of its original stratification. The Muniac texture profile usually grades from a gravelly sandy loam solum into a Summary of general characteristics of the Muniac Association gravelly to very gravelly loamy sand to sandy loam subsoil. In Map Symbol : MU poorly drained sites inwashed fines (siltation) may make the Physiographic Region(s) : Chaleur Uplands surface material slightly heavier. Coarse fragment content Elevation : 300-600 m increases with depth to in excess of 70% in some strata (layers) Extent : 2450 ha in the parent material. Percent coarse fragment content varies Percentage of Mapped Area : 0.09% Parent Material Type : Mineral from one stratum to another. Most coarse fragments are round Mode of Origin : Fluvial (glaciofluvial) edged, flat, elongated gravels or channers, 0.2 to 15 cm long, Material Thickness : Up to 20 m having been derived from highly fractured calcareous slate, Soil Colour : Olive to olive brown shale, quartzite, sandstone and related lithologies. Muniac Family Particle Size Class : Sandy skeletal Petrology (parent material) : Calcareous slate, shale, quartzites and soils are medium in natural fertility. Most profiles are acidic sandstones in the upper solum, increasing in pH with depth. Free Inherent Fertility : Medium carbonates are present at varying depths below one metre. Topography (slope) : Undulating or terraced (2-15%) Calcium is a highly mobile base ie. it is readily leached. Drainage (dominant) : Rapid Classification (typical) : Orthic Humo-Ferric Podzol During podzolization, intense leaching by strong organic acids has removed most of the calcium from the soil profile, thus resulting in an acidic solum. The bases dissolved by these percolating acids are removed in solution into the groundwater. Layer Friable upper soil Subsoil material Subsequently some bases are redeposited in poorly drained material areas by calcium carbonate enriched groundwater. In well drained soils the parent material colour is olive brown to light Depth (cm) 0 - 35 35 - 100+ olive brown. The solum consists of a relatively thin (1 to 5 Texture Class Sandy loam Loamy sand - sandy cm) LFH horizon over a light brownish gray Ae which is loam underlain by a dark brown to strong brown coloured Bf. Imperfectly drained soils have iron mottling of high chroma % Sand 65 80 and value in the lower B and C horizons. Poorly drained soils % Silt 23 10 are characterized by gray colours and prominent mottling indicative of intense reducing conditions. Matrix chromas are % Clay 12 10 generally 2 or less. The subsoils are loose and single grain, % Coarse 35 rounded, flat, 60 rounded, flat, while the sola are very friable to friable, with weak, fine to Fragments elongated G elongated G medium, granular structure in the B horizon and weak to moderate, fine, platy structure in the A horizon. pH (H2O) 5.0 - 5.5 5.5 - 7.5 BD (g/cm3) 1.20 1.50 Muniac soils are found in areas dominated by soils formed from calcareous shale, slate, quartzite and sandstone, such as Ksat (cm/hr) > 25 > 25 the Thibault, Caribou and Carleton associations. However, AWHC (cm/cm) 0.10 - 0.20 < 0.10 these are till soils and readily distinguished from Muniac soils. Till soils have developed in nonstratified deposits with angular coarse fragments (cobbles, gravels, and stones), finer textures and friable to very firm consistence. Muniac soils have been mapped in association with other soils formed on fluvial sediments: Grand Fall and Maliseet. They are differentiated on the basis of particle size class and coarse fragment lithology. 73

Nigadoo River Association soils have enough organic carbon in the B horizon to be classified as Orthic Ferro-Humic Podzols. Humo-ferric The Nigadoo River association consists of soils that have podzolization is the rule where climatic conditions are milder. developed in relatively thin (less than 2 m thick) deposits of Imperfectly drained Nigadoo River soils occur as Gleyed acidic, coarse loamy, compact morainal till sediments derived Humo-Ferric Podzols. Poorly drained soils are Orthic from metagabbro and metabasalt, with some granites, Gleysols or Fera Gleysols. They are found more extensively conglomerate and metagreywacke. They are scattered across in gently undulating landscapes, but also occur as localized the northern half of the Chaleur Uplands and New Brunswick areas in depressions and along drainage channels in more Highlands physiographic regions at elevations of 200 to 700 m strongly sloping map units. Internal drainage is restricted by above sea level (Fig. 45). Nigadoo River soils occupy a slowly to moderately slowly permeable subsoil with an approximately 35,342 ha, or 1.27% of the map sheet. estimated saturated hydraulic conductivity value of less than 0.1 cm/hr. Available water storage capacity ranges from 0.25 to 0.10 cm/cm, decreasing with depth because of increased coarse fragment content and reduced total porosity in the compact subsoil. Well drained sites are supplied with water solely via precipitation. Nigadoo River subsoils have firm consistence with a bulk density greater than 1.75 gm/cm3 and voids consisting predominantly of micro pores. Downward movement of excess moisture through the profile is impeded by the subsoil and lateral flow or seepage occurs along the subsoil contact. The seepage waters are moderately rich in nutrients and thus beneficial to most biological production. Imperfectly and poorly to very poorly drained areas have developed because of a combination of topographic position, lack of gradient, subsoil compaction, seepage and high groundwater table.

Figure 45. Location of mapped Nigadoo River soils.

The soil parent material has been deposited as ground moraine, plastered in place under the weight of advancing glacial ice. Composition strongly reflects the incorporation of local bedrock formations consisting of dark-coloured, basic, fine- grained volcanics. Smaller amounts of light-coloured, acidic granitic and metasedimentary rocks also occur. Nigadoo River soils are moderately to very stony with 2 to 15% of the land surface occupied by stones. Boulders are common but usually not in sufficient quantities to warrant designation as a bouldery phase. Nigadoo River soils have been mapped on a number of landforms ranging from undulating and rolling, to hummocky, hilly, sloping and ridged. Slopes vary from 2 to 45%. Bedrock outcrops are not common but may occur in some of the more strongly sloping landscapes, particularly topographic highs or along steeply inclined drainage channels. Well drained soils of the Nigadoo River association support mixed wood forest communities of red and sugar maple, beech, red oak, birch, white pine, black spruce and balsam fir. On poorly to very poorly drained sites the tree vegetation consists of black spruce, balsam fir, cedar and tamarack with some red Figure 46. Well drained Nigadoo River soil profile. maple and yellow birch. Soil development varies from 40 to 50 cm in thickness. The Nigadoo River soils are dominated by well, moderately well common horizon sequence on well drained sites is LFH, Ae, and imperfect drainage. Well drained sites are generally Orthic Bhf, Bf, BC and C. The organic layer averages 5 to 10 cm Ferro-Humic Podzols (Fig. 46). Climatic conditions in central thick. It overlies a thin (5 to 10 cm), ashy coloured Ae horizon New Brunswick promote the accumulation of organic matter which breaks abruptly into the B horizon. The upper reddish in the podzolic B horizon. As a result, most Nigadoo River brown to strong brown Bhf horizon varies from 5 to 15 cm in 74 thickness. It merges with a yellowish brown Bf horizon which Mode of Origin : Glacial till, compact gradually grades into the brown to yellowish brown parent Material Thickness : <2 m Soil Colour : Yellowish brown material. Imperfectly drained soils have similar profile Family Particle Size Class : Coarse loamy horizons but are mottled in the B and C horizons, especially a Petrology (parent material) : Metagabbro and metabasalt with some thin zone immediately above the compact subsoil where water granites, conglomerate and is perched. The Bhf horizon is also typically thinner in metagreywacke Inherent Fertility : Medium imperfectly drained sites. Poorly to very poorly drained Topography (slope) : Undulating to rolling and hummocky, horizon sequences lack a podzolic B horizon. They consist of hilly, sloping and ridged (2-45%) LFH or O, Aeg, Bg or Bgf, BCg, and Cg horizons. As with Drainage (dominant) : Moderately well most ill-drained catenary members, the forest duff layer is Classification (typical) : Orthic Ferro-Humic Podzol and Orthic Humo-Ferric Podzol usually thicker in the poorly and very poorly drained sites than that found in well and imperfectly drained counterparts. The Nigadoo River textural profile consists of a loam to silt loam or sandy loam (8 to 18% clay) throughout. Profile coarse Layer Friable upper soil Subsoil material fragment content averages 15 to 30%, with a preponderance of material subangular gravels and cobbles. Although the parent rocks are intermediate in weatherability, they yield sediments of medium Depth (cm) 0 - 45 45 - 100+ to high fertility. Nigadoo River soils are relatively acidic Texture Class Loam Sandy loam - loam throughout the profile with pH(H2O) values ranging from 4.0 to 5.5. The solum is friable to very friable and grades into a % Sand 40 55 firm and massive subsoil at approximately 45 cm. The subsoil % Silt 44 33 may be pseudoplaty as a result of its mode of deposition (having been plastered in place by glacial ice). % Clay 16 12

% Coarse 15 subangular G/C 25 subangular G/C The Nigadoo River association is most commonly found with Fragments other soil associations that have developed on till soil materials of volcanic rock-type origin, particularly Tetagouche, pH (H2O) 4.5 - 5.0 5.0 - 5.5 Tetagouche Falls and Popple Depot. Nigadoo River, BD (g/cm3) 1.10 1.80 Tetagouche and Tetagouche Falls soils have all developed from materials dominated by ferromagnesian, dark-coloured, Ksat (cm/hr) 2 - 10 < 0.1 “mafic”, volcanic rock types. They are differentiated on the basis of consistence and particle size. Nigadoo River soils are AWHC (cm/cm) 0.20 0.10 coarse loamy and compact in the subsoil. Tetagouche soils are fine loamy and compact in the subsoil. Tetagouche Falls soils are loamy and non-compact in the subsoil. Of all soils, Nigadoo River is probably most similar physically and Parleeville Association morphologically to Popple Depot soils. Both have developed on coarse loamy compact tills. They are separated on the basis The Parleeville association consists of soils developed in thin of lithology. Popple depot soils are dominated by light- (less than 1 m) to moderately thick (greater than 2 m) deposits coloured, or “felsic” volcanic rock types. In areas of complex of acidic (but increasing in pH with depth), coarse loamy to bedrock geology and/or along bedrock transition zones, loamy skeletal, noncompact, morainal glacial till material Nigadoo River soils are also mapped with Carleton, Long (ablational till) with coarse fragments of soft arkosic sandstone Lake and Thibault soils. and weathered conglomerate pieces (granites, quartzites, volcanics and some sandstones). Parleeville soils occur in the Excluding problems due to wetness in imperfectly and poorly southern portions of the New Brunswick Highlands and to very poorly drained locations, the dominant features Chaleur Uplands at elevations of 100 to 300 m above mean sea affecting land use are: coarse fragment content (both surface level (Fig. 47). The Parleeville ablational till material is and profile); topographic conditions (excessive slope) and the underlain by weathered red sandstone and conglomerate presence of a subsoil restricting layer which impedes root bedrock that has a weakly calcareous cementing agent. In penetration and water percolation. However, medium inherent veneer phases the bedrock occurs within 1 metre of the surface fertility is an asset to forest production. and is often weathered in situ, thus some of the soil parent material is residual in origin. Parleeville soils occupy approximately 16,800 ha or 0.60% of the map area. Summary of general characteristics of the Nigadoo River Association Parleeville soils are considered to have developed in ablational Map Symbol : NR Physiographic Region(s) : Chaleur Uplands, N.B. Highlands till. Ablational till is the accumulation of debris deposited Elevation : 200-700 m from glacial ice during down wasting or melting of the glacier. Extent : 35,342 ha In the case of Parleeville, some of the parent material may be Percentage of Mapped Area : 1.27% non-compact lodgment till or residual. Landforms range from Parent Material Type : Mineral 75

thin Bhf, Bf, Bfj, BC and C on well to moderately well drained sites; LFH or O, Ae, Bfgj, BCgj or BCg and Cg on imperfectly or poorly drained sites; and LFH or O, Ae, Bmgj, BCg and Cg, or LFH or O, Aeg, Bg and Cg on poorly or very poorly drained sites. Soil textures grade from a loam to sandy loam, which is sometimes gravelly, into a gravelly to very gravelly sandy loam to loam subsoil. Coarse fragment content increases with depth. It ranges from 15 to 30% but may be as high as 50% in some shallow lithic phases. Most coarse fragments are gravels of granite, quartzite, volcanics and arkosic sandstone that have weathered from the conglomerate bedrock. Parleeville soils are medium in natural fertility, owing to the bases associated with the weathered weakly calcareous cementing agent in the parent conglomerate bedrock. However, the profile is acidic

throughout the upper metre, ranging from a pH(H2O) of 4.0 to 5.5. The parent material is reddish brown to weak red. Typically, well drained soil profiles consist of a pinkish gray, friable, weak, fine platy Ae horizon over a yellowish red to Figure 47. Location of mapped Parleeville soils. yellowish brown, very friable, weak to moderately fine granular Bhf/Bf (the Bf being the lighter colour) which merges rolling to strongly undulating, with slopes of 2 to 15%. Where gradually into the friable, very weak, subangular blocky to down wasting of glacial ice was more rapid, thin layers of structureless BC and then C. Mottles and grayish gley colours Parleeville ablational till were deposited. Although the soil is modify the profile morphology in imperfectly and poorly shallow in these units, bedrock outcrops are scarce. The soil drained sites. Under poorly and very poorly drained parent material consists of a heterogeneous mixture of sand, conditions the podzolic sequence is not present. silt, clay and coarse fragments, mostly gravels, but with some cobbles. Most coarse fragments are subrounded to subangular Parleeville soils were not mapped in association with any other gravels of granite, quartzite, volcanics and arkosic sandstone. soil types. They tend to occur as “islands” within a sea of soils Parleeville soils are usually slightly to moderately stony on the developed from yellowish brown to olive brown coloured surface. Stones are greater than 2 m apart and occupy less than parent materials. As such, Parleeville soils are readily 3% of the surface area. Well drained Parleeville sites support identified by their strong reddish brown colour. In this respect, mixed stands of black spruce, balsam fir, grey and yellow parent material colour, they are most similar to Stony Brook birch, sugar maple and some beech. On ill-drained sites the soils. Stony Brook soils have fine loamy, very dense compact sugar maple and beech component is superseded by red maple, subsoils in comparison to the coarse loamy, open, porous cedar, tamarack, speckled alders and willow. subsoils in Parleeville. Parleeville soil parent materials are also more lithologically diverse. The Parleeville association is dominated by well to moderately well drained Orthic Humo-Ferric Podzols. Podzolization is Parleeville soils are suitable for a wide range of agricultural strongly expressed, even in sites that are less than well drained. and forestry crops. Veneer phases may pose some limitations Imperfectly drained sites are Gleyed Humo-Ferric Podzols and to crop production due to lowered water-holding capacities. poorly to very poorly drained sites, Gleyed Eluviated Dystric Forest site capability is enhanced by the moderately rich Brunisols or Orthic Gleysols. Internal drainage is good. The natural fertility. profile consists of a rapidly permeable solum over a moderately permeable subsoil. Saturated hydraulic Summary of general characteristics of the Parleeville Association conductivity values range from greater than 10 cm/hr in the Map Symbol : PA solum to 2 to 5 cm/hr in the subsoil. Available water storage Physiographic Region(s) : Chaleur Uplands, N.B. Highlands capacity ranges from 0.10 to 0.20 cm/cm, the higher values Elevation : 100-300 m being in the solum where finer textures and organic matter Extent : 16,800 ha contents enhance moisture retention. Precipitation is the sole Percentage of Mapped Area : 0.60% Parent Material Type : Mineral source of water input on well drained sites. Imperfectly and Mode of Origin : Glacial till, noncompact, some residual poorly to very poorly drained sites are the result of high water material table and groundwater flow. Drainage is largely determined by Material Thickness : < 2 m topography. Well to moderately well drained soils dominate Soil Colour : Reddish brown Family Particle Size Class : Coarse loamy to loamy skeletal areas of rolling topography. Undulating map units are Petrology (parent material) : Sandstone and conglomerate dominated by imperfectly drained conditions. Poorly drained Inherent Fertility : Medium sites are restricted to depressions and stream channel locations. Topography (slope) : Undulating to rolling (2-30%) Drainage (dominant) : Well Classification (typical) : Orthic Humo-Ferric Podzol Solum development in Parleeville soils varies from 35 to 55 cm in thickness. The common horizon sequence is: LFH, Ae, 76

Layer Friable upper soil Subsoil material similar composition. Mixing actions of soil formation have material obliterated most evidence of the ablational capping. The solum is underlain by a dense compact lodgment till subsoil (parent Depth (cm) 0 - 45 45 - 100+ material). Because of the relatively thin nature of these Texture Class Loam - sandy loam Sandy loam - loam deposits, the surface expression generally reflects the topography of the underlying bedrock. Landforms consist of % Sand 45 55 a mixture of blankets and veneers over undulating, rolling, hilly and sloping bedrock formations. Slopes range from 2 to % Silt 40 30 30% with the occasional slope ranging up to 70% were streams % Clay 15 15 and rivers are deeply incised into the landscape. Bedrock exposures occupying up to 25% of the map unit area may be % Coarse 15 rounded G 30 rounded G found in these more steeply sloping areas. Well drained Fragments Popple Depot soils support mixed softwood-hardwood stands of balsam fir, black spruce, red spruce, white birch, yellow pH (H2O) 4.5 - 5.0 5.0 - 5.5 birch, and sugar and red maple. Forest cover on poorly drained 3 BD (g/cm ) 1.10 1.50 sites is comprised of balsam fir, black spruce, cedar, red maple, Ksat (cm/hr) > 10 2 - 5 tamarack and some yellow birch.

AWHC (cm/cm) 0.15 - 0.20 0.10 Popple Depot soils are dominated by well drained Orthic Ferro-Humic Podzols and Orthic Humo-Ferric Podzols. Climatic conditions in central New Brunswick are conducive to the accumulation of organic matter in the podzolic B horizon. Macro- and mesoenvironmental conditions are such Popple Depot Association that organic carbon accumulates in sufficient quantities to qualify most Popple Depot soils for Ferro-Humic Podzol great The Popple Depot association consists of soils that have group status. Ferro-humic podzolization is not as strongly developed in moderately thin (less than 2 m) deposits of acidic, expressed along the eastern periphery of the Popple Depot coarse loamy compact morainal till derived from mixed range where the Central Highlands merge with the Maritime rhyolite and trachytes with some basalt and miscellaneous Plain, which has a slightly milder climate than the Highlands. slates and greywackes. Popple Depot soils are located in the Mesoenvironmental differences due to the type of vegetation New Brunswick Highlands and eastern Chaleur Uplands and thus the type of litter are also important in determining physiographic regions (Fig. 48). Elevations range from 120 to variation in solum formation within a map unit. Well drained 700 m above sea level. In total these soils occupy conditions dominate steeply sloping hilly and rolling approximately 148,083 ha or 5.31% of the total map area. landscapes. In these landforms poorly and imperfectly drained conditions are confined to relatively narrow drainage channels. Significant hectarages of imperfectly drained Popple Depot soils occur as Gleyed Humo-Ferric Podzols in areas of undulating and gently rolling topography, where they are found in association with well drained or poorly drained associates. Poorly drained soils of the Popple Depot association are Orthic Gleysols or Fera Gleysols. Internal drainage is restricted by a slowly permeable subsoil with an estimated saturated hydraulic conductivity value of 0.1 to 0.5 cm/hr. Available water storage capacity ranges from 0.20 to 0.10 cm/cm, decreasing with depth because of reduced total porosity in the compact subsoil. Well drained sites are supplied with water solely via precipitation. Downward movement of excess moisture through the profile is impeded by the subsoil. Some lateral flow occurs for short durations. Imperfectly and poorly to very poorly drained areas have developed because of a combination of topographic position, lack of gradient, subsoil compaction, seepage and high Figure 48. Location of mapped Popple Depot soils. groundwater table.

Solum thickness ranges from 35 to 55 cm. On well drained Popple Depot parent material has been deposited as ground sites the common horizon sequence is LFH, Ae, Bhf, Bf, BC moraine, basal till plastered in place during glacial advance and and C or Cx. The upper horizons, LFH, Ae, and Bhf are all subsequently covered with a thin discontinuous mantle of relatively thin (3 to 15 cm) but distinct in appearance. ablational till upon glacial retreat. Both materials are of Mineralization and humification processes in the organic layer 77 are slow. The F horizon dominates over the H horizon. The schists and quartzite. light grayish coloured Ae overlies the dark reddish brown coloured Bhf which in turn changes abruptly to a 10 to 25 cm Biological production on Popple Depot soils is affected by low thick, yellowish brown coloured Bf horizon. The Bf horizon inherent fertility, surface stoniness, depth to a root/water grades through a transitional BC horizon into a compact C restricting layer, climate, and to a lesser degree wetness and horizon. The C horizon may have fragipan formation, which topography. These limitations more severely handicap when moist is difficult to differentiate from the compact parent agriculture than forestry. Agricultural potential is marginal. material. When dry, the fragic material is brittle and slakes in Popple Depot soils should prove adequate to support water. Well drained profiles with fragipan development are moderately productive stands of forest tree species climatically classified as Fragic Humo-Ferric Podzols. However, most of suited to the region. the fragipan in Popple Depot soils is weakly expressed and limited in areal extent. Bedrock exposures occur in better Summary of general characteristics of the Popple Depot Association drained more steeply sloping sites and may occupy as much as Map Symbol : PD 10 to 25% of these units. Imperfectly drained members of the Physiographic Region(s) : N..B. Highlands Popple Depot association have a similar sequence of horizons, Elevation : 120-700 m but display distinct or prominent mottling, especially along the Extent : 148,083 ha contact with the dense, compact subsoil. Gleying becomes Percentage of Mapped Area : 5.31% Parent Material Type : Mineral more prominent in lower-slope site positions. Some Mode of Origin : Glacial till, compact imperfectly drained Popple Depot soils have thin Material Thickness : <2 m (approximately 5 cm thick) Ahe horizons sandwiched between Soil Colour : Yellowish brown to olive brown the H and Ae horizons. Poorly to very poorly drained Popple Family Particle Size Class : Coarse loamy (skeletal) Petrology (parent material) : Rhyolite and trachyte with some basalt Depot soils have profiles consisting of LFH of O, Aeg, Bg or and slates and greywacke Bgf, and Cg horizons. The predominance of coniferous forest Inherent Fertility : Low vegetation on these sites encourages mosses and the Topography (slope) : Undulating to rolling or hilly (2-30%) accumulation of thicker organic layers. Drainage (dominant) : Moderately well Classification (typical) : Orthic Ferro-Humic Podzol and Orthic Humo-Ferric Podzol The Popple Depot texture profile consists of a sandy loam to loam throughout, with 8 to 18% clay content. Weathering within the solum may result in a slightly finer texture in the upper profile than in the subsoil , however, this variation is still Layer Friable upper soil Subsoil material within the sandy loam-loam grouping. Profile coarse fragment material content ranges from 20 to 40% with subangular stones, cobbles Depth (cm) 0 - 45 45 - 100+ and gravels and even boulders. Most Popple Depot land surfaces are moderately to very stony with stones occupying 2 Texture Class Loam Sandy loam - loam to 15% of the surface area. Usually these soils are also moderately to very cobbly with surface coverage similar to that % Sand 50 55 of the stones. Surface boulders are present but not in % Silt 35 33 significant quantities to warrant designation. Popple Depot soils are low in natural fertility. The parent rocks weather % Clay 15 12 slowly and yield relatively infertile soil material. Both the % Coarse 20 subangular G/C 30 subangular G/C solum and subsoil are acidic, falling within a pH(H2O) range Fragments of 4.0 to 5.5. The solum is moderate, fine to medium, granular to subangular blocky structured and very friable. It pH (H2O) 4.5 - 5.0 5.0 - 5.5 provides a 40 to 50 cm potential rooting zone. The parent BD (g/cm3) 1.10 1.80 material is firm to very firm, compact, and slightly cemented in the upper C horizon. The C horizon is usually pseudo platy Ksat (cm/hr) 2 - 5 0.1 - 0.5 in situ but breaks to medium subangular blocky when AWHC (cm/cm) 0.15 - 0.20 0.10 extracted.

Popple Depot soils have been mapped with Catamaran, Jacquet River, Nigadoo River, Long Lake, McGee, Tetagouche and Reece Association Tetagouche Falls soils. Jacquet River soils have developed in tills of similar lithology to Popple Depot soils. They are The Reece Association consists of soils developed in differentiated on the basis of subsoil compaction. Jacquet moderately thin (1 to 2.5 m) to thin (less than 1 m) deposits of River soils have a noncompact subsoil. Popple Depot soils acidic, fine loamy, compact glacial till material (lodgment till) have a compact subsoil. Catamaran soils are closest to the with coarse fragments of soft sandstone. Reece soils occur in Popple Depot association in terms of physical, chemical and the lowlands portion of the study area at elevations ranging morphological properties. They are similar in colours, textures from 40 to 140 m above sea level (Fig. 49). The lodgment till and structures, but Catamaran soils are derived from granites, frequently has a surficial capping of coarse loamy ablational 78 till (Sunbury material). Reece soil materials are underlain by usually subdominant components of map units dominated by the soft gray-green Pennsylvanian sandstone that underlies imperfectly drained soils. Internal drainage is restricted by a most of the New Brunswick Lowlands or Maritime Plain. slowly permeable subsoil (0.1 to 0.5 cm/hr saturated hydraulic Some veneer phases occur where the bedrock is within 1 metre conductivity). The solum permeability is usually 5 cm/hr or of the soil surface. Reece soils occupy approximately 332,784 faster. Available water storage capacity ranges from 0.15 to ha, representing 11.94% of the map area. 0.20 cm/cm in the solum, but is less than 0.10 cm/cm in the subsoil. Low available water storage capacity in the subsoil is due to compaction and thus lower total pore space. On well drained sites precipitation is the dominant water source. Excess water flows laterally as subsurface flow. Where there is less gradient, water is removed from the soil somewhat slowly in relation to supply giving rise to moderately well drained conditions. Imperfectly drained sites occupy mid to lower slope positions where water is supplied by precipitation and subsurface flow or seepage. Poorly and very poorly drained conditions are strongly influenced by subsurface inflow and groundwater flow, in addition to precipitation. They occupy lower slope, toe and depressional sites. Lateral water movement is promoted by the dense, slowly permeable Reece subsoil.

Profile development is moderately thick, 40 to 70 cm. The common horizon sequence is LFH, Ae, Bf, BC or BCx and (II)C or (II)Cx, on well drained sites; LFH, Ae, Bfgj, BCgj or Figure 49. Location of mapped Reece soils. BCxgj and (II)Cg or (II)Cxg on imperfectly drained sites; and LFH or O, Aeg, Bgf and (II)Cg or (II)Cxg on poorly to very Lodgment till consists of successive layers of glacial debris poorly drained sites. Soil horizon continuity is often disrupted which is plastered into place below the glacier as it advances. by tree uprooting, especially on imperfectly and poorly drained The finer textured nature of Reece soil parent material is sites. Windthrow also promotes hummocky micro topography attributable to a shale component within the debris. At the in these sites. Poorly drained profiles may have a 10 to 30 cm time of glaciation the Pennsylvanian aged bedrock is thought thick accumulation of organic debris on the surface, especially to have had interbedded shale-sandstone near the surface. The in level and depressional areas where Reece soils are scouring nature of glacial ice readily abraded the shales. The associated with organic soils, Lavillette or Acadie Siding. softer shale (and siltstone) fragments have completely Climatic conditions on the western edge of the lowlands plain disintegrated. Only fragments of the more durable sandstone adjacent to the uplands boundary result in thin Bhf remain intact. The lodgment till is characterized by its development in the upper B horizon. Fragipan, indicated by physical heterogeneity. There is no size assortment and no the "x" suffix in the horizon designation, is a common evidence of stratification with exception of a pseudo platy characteristic of Reece soils. It is a hardpan with high bulk structure caused by compaction under ice pressures during density, very low organic matter content and slow to very slow deposition. Soil and coarse fragment shapes vary from sharp permeability that forms in the lower B and C horizons. When and angular to subrounded, depending upon fluctuations in the moist, fragipans are moderately to weakly brittle and difficult grinding actions caused by the ice. Reece soils have to differentiate from the compact lodgment till. When dry, moderately stony to very stony land surfaces. Stones are 1 to they have a hard consistence and seem to be cemented. But 10 m apart and occupy 0.1 to 15% of the surface area. Reece they are reversible pans and air dried clods of fragic horizons soils tend to be most stony where mapped in association with slake or fracture when placed in water. Most Reece soils occur Sunbury soils. This is the result of the ablational till capping below the maximum level of post glacial marine submergence. on the lodgment till. Reece landforms are typified by Coarser textures in the upper solum may be attributed to this. undulating to very gently rolling surface expressions with 2 to Sandy marine sediments may have been deposited during this 7% slopes. Well drained sites support stands of black spruce, period of submergence and subsequently incorporated into the balsam fir, sugar maple, white birch and beech. As drainage upper soil profile. The Reece texture profile consists of a sandy conditions deteriorate the sugar maple, white birch and beech loam to loam solum over a loam to sandy clay loam or clay give way to red maple and yellow birch. Cedar and tamarack loam subsoil. Profile coarse fragment content averages 10 to occur on very poorly drained sites. 25%, with higher percentages occurring in some lithic (veneer) phases. Coarse fragments are subangular to flat cobbles, The Reece association is dominated by imperfectly drained gravels and stones of soft, gray-green sandstone derived from Gleyed Humo-Ferric Podzols. There are extensive areas of the local bedrock. The sandstone is fine- to medium-grained. impeded drainage. Well to moderately well drained Orthic It is dominated by quartz but with significant feldspars, biotite Humo-Ferric Podzols (Fig. 50) and Fragic Humo-Ferric and muscovite. Reece soils are medium in natural fertility. Podzols or poorly to very poorly drained Fera Gleysols are 79

glacial till soils that occur on the lowland plain with Reece soils. Reece, Rogersville and Stony Brook soils have all developed on fine-loamy lodgment till materials. Rogersville soils are more reddish brown in colour, are somewhat heavier in texture, but most obviously, have a granitic component in their lithological composition. Stony Brook soils have a red to reddish brown subsoil which is the most obvious differentiating criteria from Reece soils. They are also slightly heavier in texture. Reece soils are most intimately associated with Sunbury soils. In fact, they may be identical in the upper solum. They are separated on the basis of subsoil characteristics. Sunbury soils are coarser textured and noncompact. Poorly drained Reece soils are often situated adjacent to organic soils, either Acadie Siding or Lavillette. Thickness of the organic layer is used to differentiate mineral from organic soils. Mineral soils such as Reece have less than 40 cm of organic debris on the surface. Reece soils have also been mapped with Long Lake and Catamaran soils along the Maritime Plain - New Brunswick Highlands boundary. Both Long Lake and Catamaran soils have developed on compact lodgment till materials, but they are coarse-loamy. Lithological differences are also used to separate Long Lake (slate, siltstone, argillite, schist, quartzite and greywacke) and Catamaran (granites with greywacke, schists, quartzite, slates and sandstones) from Reece (sandstone).

The major limitations to biological production on Reece soils are a result of the drainage-compact subsoil situation. Stoniness may also be detrimental in agricultural usage. From a forestry perspective Reece soils are among the most productive soil types found in the lowlands. Figure 50. Well drained Reece soil profile. Summary of general characteristics of the Reece Association The profile is acidic throughout, falling between pH(H O) 4.0 2 Map Symbol : RE and 5.5. Well drained soil parent materials are strong brown to Physiographic Region(s) : Maritime Plain dark yellowish brown. The profile consists of a grayish, Elevation : 40-140 m friable, weak, fine platy Ae horizon over a yellowish red to Extent : 332,784 ha yellowish brown, very friable, weak to moderate, fine granular Percentage of Mapped Area : 11.94% Parent Material Type : Mineral Bf horizon which grades through a BC horizon into a firm to Mode of Origin : Glacial till, compact very firm, weak subangular blocky or platy to structureless C Material Thickness : <2.5 m horizon. A thin slightly grayish zone of lateral leaching may Soil Colour : Strong brown to dark yellowish brown be present immediately above the compact layer. In Family Particle Size Class : Fine loamy Petrology (parent material) : Gray-green sandstone and weathered shale imperfectly drained soils temporarily perched water tables Inherent Fertility : Medium create a mottled zone along the friable-compact interface. Topography (slope) : Undulating to gently rolling (2-7%) Grayish gley colours dominate poorly drained profiles. Drainage (dominant) : Imperfect Fragipan formation is related to site drainage. It is most Classification (typical) : Gleyed Humo-Ferric Podzol strongly expressed on well drained sites where development averages 40 to 60 cm in thickness, the upper boundary of which occurs at depths of 50 to 70 cm below the mineral soil Layer Friable upper soil Subsoil material surface. Poorly drained conditions have weakly developed material pans that are thinner, 20 to 30 cm thick, and have formed closer to the surface, at depths of 30 to 40 cm. The upper Depth (cm) 0 - 50 50 - 100+ boundary is clear and abrupt while the lower boundary is Texture Class Sandy loam - loam Loam - sandy clay gradual or diffuse. Fragipans have very coarse prismatic loam structure separated by bleached vertical fissures or planes that produce a polyhedron pattern when cut horizontally, such as in % Sand 55 50 ditch bottoms. % Silt 30 23

Rogersville, Stony Brook and Sunbury associations are other % Clay 15 22 80

% Coarse 10 subangular 20 subangular C/G/S consist of well sorted sands, primarily medium- to fine-grained Fragments C/G/S particles, but some strata are gravelly or pebbly. Associated landforms have level to gently undulating surface expressions, pH (H2O) 4.5 - 5.0 5.0 - 5.5 with slopes of 0.5 to 2%. Steeper gradients may occur along BD (g/cm3) 1.10 1.80 river valleys. Well to rapidly drained Richibucto soils support softwood stands of predominantly jack pine and black spruce. Ksat (cm/hr) > 5 0.1 - 0.5 Stunted gray birch occurs on the more droughty sites. Red maple, white birch, black spruce and balsam fir occur on the AWHC (cm/cm) 0.15 - 0.20 < 0.10 wetter sites.

The Richibucto association is made up of rapidly to well Richibucto Association drained Orthic Humo-Ferric Podzols and Eluviated Dystric Brunisols, imperfectly drained gleyed subgroups of the The Richibucto association consists of soils developed in afore-mentioned, and poorly to very poorly drained Gleyed relatively thin (less than 2.5 m) deposits of acidic, sandy Eluviated Dystric Brunisols and Orthic Gleysols. In well and marine sediments derived from soft sandstone. They occur imperfectly drained associates the B horizon, although only in the lowlands portion of the study area where they are appearing morphologically typical of a Bf horizon, just meets confined to a narrow strip about 10 km wide along the coast, the chemical requirements for a podzol. The deceiving occasionally fingering inland more deeply along tidal rivers appearance is the result of the sandy nature of the material and (Fig. 51). Thin deposits (veneers less than 1 m thick) rest the fact that very little illuviated iron and organic matter is directly on weathered gray-green Pennsylvanian sandstone required to significantly affect a colour change. Poorly drained bedrock. Thicker deposits (greater that 1 m) may be underlain soils do not meet podzolic requirements. On rapidly to well by a thin mantle of morainal till overlying the bedrock. drained sites precipitation is the sole source of water. Excess Richibucto sands are also underlain by marine/lacustrine clays water readily flows downward through the pervious subsoil along some estuarial valleys. Most Richibucto soils are found which has saturated hydraulic conductivity values of greater at elevations of less than 50 m above sea level. They cover than 25 cm/hr. Available water storage capacity is low, usually approximately 60,029 ha, or about 2.15% of the map area. less than 0.10 cm/cm and decreases with depth. Slightly finer textures and higher organic matter contents enhance moisture retention in the solum. Imperfectly and poorly drained conditions are the result of high groundwater tables. Groundwater levels respond quickly to additions by precipitation because of the low moisture holding capacity of the soil profile and the relative ease of groundwater flow through the coarse textured subsoil. Substrata, bedrock (Fig. 52) or relatively impermeable morainal till or marine clays, also create deep (below the control section) seepage conditions which recharge these sites.

Soil formation averages 30 to 50 cm in depth, however, most development is concentrated in the upper 30 cm of the profile, below which is a zone of transition into the parent material. Common horizon sequences consist of: LFH, Ae, Bf or Bm, BC and C in rapidly to well drained sites; LFH, Ae, Bfgj or Bmgj, BCgj and Cg in imperfectly drained sites; and LFH or O, Aegj, Bmgj, BCg and Cg, or O, Aeg, Bg and Cg in poorly to very poorly drained sites. Rapidly to imperfectly drained Figure 51. Location of mapped Richibucto soils. profiles have a typical podzolic appearance. They have a thin organic duff layer over a light grayish coloured eluvial A Richibucto parent materials are marine sediments or marine horizon. The underlying reddish brown to yellowish brown B reworked glaciofluvial material, some of which may have been horizon has an abrupt upper boundary and becomes deposited subaqueously. They were deposited in an early progressively yellower as it grades through the BC into the postglacial, shallow brackish water environment. Acid brown to yellowish brown C horizon. Iron (Fe) mottling leaching has destroyed any calcareous fossils that may have modifies this appearance in imperfectly drained sites. Poorly been present but material composition and configuration and very poorly drained sites are often severely gleyed because coupled with its general location below the level of postglacial of the persistence of waterlogged conditions. Very poorly marine submergence indicate a marine mode of deposition. drained sites often have bluish gray subsoils. Horizonation is Richibucto soils have developed on wave-washed sediments weakly expressed. The texture profile grades from a loamy deposited as marine beach ridges, marine terraces and sand to sandy loam solum into a loamy sand to sand subsoil. discontinuous blankets and veneers of marine sand. They Clay content seldom exceeds 10% and is usually less than 5% 81 in the subsoil. The high degree of particle size sorting is than 1 m of marine sand over a compact cobbly morainal till. exemplified by subsoils in which sand accounts for 95 to 97% Tracadie soils are marine clays. Riverbank soils are very of the soil material. Most profiles are relatively free of coarse similar to Richibucto soils in morphological characteristics. fragments. Those coarse fragments that are present are usually However, unlike Richibucto soils, Riverbank soils are derived rounded gravels of soft gray-green sandstone. Occasionally from a mixture of lithologies and thus have greater there is as high as 20% gravels. These areas are thought to be mineralogical variability. Riverbank is also associated with remnants of beach ridges. Veneer phases may also be an different landforms; kames, eskers, stream terraces, etc. Very exception to this. Frost action and windthrow mix thin, flat poorly drained Richibucto soils are often mapped in complexes fragments of the underlying bedrock into the lower profile. with organic soils, either Acadie Siding or Lavillette. Richibucto soils are very low in natural fertility and nutrient Thickness of the organic layer is used to differentiate mineral retention capability. They are also acidic, with pH (H2O) 4.0 soils from organic soils. Mineral soils such as Richibucto have to 5.0, throughout. Soil structure is weakly expressed in the less than 40 cm of organic debris on the surface. solum and structureless or single grain in the subsoil. Consistence is typically very friable to loose, except for the Biological productivity on Richibucto soils is limited by very presence of ortstein, a firmly cemented hardpan, that occurs low moisture holding capacity, inherent natural fertility and sporadically in the solum. Ortstein is a discontinuous, nutrient retention. Selection of crops must be made with these irreversible pan in which the soil particles are bonded by Fe, constraints in mind. Richibucto sands are easily manipulated Al and organic matter complexes. It is more strongly in terms of moisture and nutrient status by irrigation and developed under poorly drained conditions where pans are fertilizer applications and so are ideal sites for specialty crops harder and cover a greater lateral extent. that require closely controlled environments. Richibucto parent material is also a source of industrial sand.

Summary of general characteristics of the Richibucto Association

Map Symbol : RB Physiographic Region(s) : Maritime Plain Elevation : < 50 m Extent : 60,029 ha Percentage of Mapped Area : 2.15% Parent Material Type : Mineral Mode of Origin : Marine Material Thickness : < 2.5 m Soil Colour : Yellowish brown to brown Family Particle Size Class : Sandy Petrology (parent material) : Soft gray-green sandstone Inherent Fertility : Very low Topography (slope) : Level to undulating (0.5-2%) Drainage (dominant) : Rapid Classification (typical) : Orthic Humo-Ferric Podzol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 40 40 - 100+

Texture Class Loamy sand - sandy Loamy sand - sand loam

% Sand 80 85

% Silt 10 10

% Clay 10 5

% Coarse < 2 rounded G < 2 rounded G Fragments

pH (H2O) 4.0 - 4.5 4.5 - 5.0 Figure 52. Well drained Richibucto soil profile, veneer phase. BD (g/cm3) 1.20 1.50

Richibucto soils are found in close proximity to other soils that Ksat (cm/hr) > 25 > 25 have developed on marine sediments, the Barrieau-Buctouche and Tracadie associations. Both soils are readily differentiated AWHC (cm/cm) 0.10 0.05 - 0.10 from Richibucto soils. Barrieau-Buctouche soils consist of less 82

Riverbank Association The Riverbank association consists of rapidly to well drained Orthic Humic-Ferric Podzols (Fig. 54), imperfectly drained The Riverbank association consists of soils developed in Gleyed Humo-Ferric Podzols, and poorly to very poorly relatively thick (sometimes in excess of 10 m) deposits of drained Gleyed Eluviated Dystric Brunisols, Orthic Gleysols acidic, sandy glaciofluvial material derived from igneous, and Fera Gleysols. On rapidly to well drained sites water is metamorphic and some sedimentary rock types. Riverbank supplied only by precipitation. Rainfall rapidly enters the soil materials are underlain by either bedrock, or the prevailing and a large part of the water passes through the profile or regional glacial till material. They are found primarily in the evaporates into the air. These soils have a low available water New Brunswick Highlands but also occur on the western edge storage capacity, 0.15 to 0.10 cm/cm or less, usually of the Maritime Plain at elevations ranging from 50 to 300 m decreasing with depth. Slightly finer textures and higher levels above sea level (Fig. 53). Riverbank soils cover approximately of organic matter content aid water retention in the upper 12,733 ha or 0.46% of the map area. They occur in small, solum. Imperfectly and poorly drained sites are restricted to scattered tracts. areas that are affected by high ground water levels, such as depressions and lower terraces along valley floors. Groundwater flow is the main water source. Seepage is absent. Subsoil permeability varies from less than 1 cm/hr to more than 25 cm/hr. This wide range is due to parent material stratification. However, most layers are rapidly permeable with transmissibility rates of more than 10 cm/hr..

Soil development in Riverbank materials averages 30 to 50 cm in thickness. Those sites with more suitable moisture regimes for biological production tend to have the greatest degree of solum development. Excessively dry and excessively moist sites have shallower sola. The common horizon sequence in well to rapidly drained soils is: LFH, Ae, Bf, BC and C. Imperfectly drained profiles have LFH, Ae, Bfgj, BCgj and Cg horizons. Poorly to very poorly drained profiles have a number of different possible profiles: LFH, Ae, Bmgj, BCg and Cg; or LFH or O, Aeg, Bg and Cg; or, LFH or O, Aeg, Bgf and Cg. The surface horizons of Riverbank soils display little evidence of the stratification so typical of their parent Figure 53. Location of mapped Riverbank soils. materials. They also contain more silt and clay than found in the subsoil. These modifications are attributed to soil forming Riverbank parent materials were deposited as either glacial processes. Windthrow, frost action and biological activity outwash plains and valley trains, or as ice contact stratified have mixed together the originally stratified surface materials. drift in features such as kames and eskers. Most deposits are Physical and chemical weathering in the solum has lead to the found in narrow strips on river terraces and bottoms. disintegration and decomposition of rocks and minerals. The Deposition has been by moderately fast flowing waters. Riverbank texture profile grades from a sandy loam to loamy Suspended particles were deposited when water turbulence sand solum into a loamy sand to sand subsoil. Clay content ceased to exceed their settling velocities, a function of particle seldom exceeds 10% in any horizon. The sand fraction varies diameter, shape and specific gravity and fluid density. from 70 to 95%. It has a wide variety of minerals such as Therefore, to a large degree, the velocity of the flowing water quartz, hornblende, biotite, muscovite and numerous feldspars. determined the size of the particles that were deposited. Most Most profiles are relatively free of coarse fragments, but sediments consist of well rounded fine to medium sand grains. occasionally some deposits have as much as 20% gravels and Changes in streamflow velocity resulted in layers of varying cobbles derived from mixed igneous, metamorphic and thickness and particle size. Deposits often contain thin layers sedimentary rock types such as granites, schists, gneisses, of silt or gravel. These strata may significantly modify internal slates, quartzite and volcanics. Riverbank soils are low in drainage characteristics. Riverbank landscapes are varied. natural fertility. They are also acidic throughout the profile,

They include terraced surfaces, with horizontal or gently with pH (H2O) of 4.0 to 5.0. The parent material colour is inclined planes (0-3% slope) separated by scarp faces (15-45% yellowish brown to olive brown. In well drained sites the slope); outwash plains, with undulating (0-5% slope) surface solum consists of a thin LFH layer overlaying a leached expressions; and ridges or eskers, with rounded crests and grayish coloured Ae horizon. The underlying Bf horizon is steep sides (5-30% slope). Riverbank soils support yellowish brown to strong brown, becoming progressively predominately softwood stands of jack pine and black spruce, yellower in hue with depth. Imperfectly and poorly to very with stunted grey birch on the drier sites. Moist sites along poorly drained soils have either iron (Fe) mottling or gleyed stream bottoms and lower terraces have black spruce, red colours of low chroma, or both. The subsoils are loose and maple and white birch. single grain (structureless) but stratified. The A horizon is friable to very friable, very weak, fine platy. Most B horizons 83

Richibucto soils are almost identical to Riverbank soils. Both consist of well sorted sands. Richibucto sands are of marine origin and restricted to the lowlands, usually in close proximity to the coast. Their parent materials were derived from soft Pennsylvanian sandstone. They lack the mineralogical variability found in the Riverbank association.

Low water holding capacity, low natural fertility and low fertility retention characteristics restrict biological productivity to selected crops. In forestry, tree species must be selected that minimize these impacts. Riverbank soils can be highly productive for specialty crops (strawberries, apples, etc.) where management inputs are high and moisture levels artificially controlled. Riverbank parent material is also a source of industrial or commercial sand.

Summary of general characteristics of the Riverbank Association

Map Symbol : RI Physiographic Region(s) : Maritime Plain, N.B. Highlands Elevation : 50-300 m Extent : 12,733 ha Percentage of Mapped Area : 0.46% Parent Material Type : Mineral Mode of Origin : Fluvial (glaciofluvial or possibly alluvium) Material Thickness : Up to 10 m Soil Colour : Yellowish brown to olive brown Family Particle Size Class : Sandy Petrology (parent material) : Mixed igneous, metamorphic and minor sedimentary Inherent Fertility : Low Topography (slope) : Undulating to terraced (0.5-5%) Drainage (dominant) : Rapid Classification (typical) : Orthic Humo-Ferric Podzol

Figure 54. Rapidly drained Riverbank soil profile. Layer Friable upper soil Subsoil material are very friable, weak to moderate, fine granular, however, material occasionally they may have cemented, massive ortstein layers. Ortstein is a strongly cemented irreversible but discontinuous Depth (cm) 0 - 50 50 - 100+ hardpan that restricts root penetration and is only slowly Texture Class Sandy loam - loamy Loamy sand - sand permeable to water. Fe, Al and organic complexes are the sand bonding agents. Ortstein layers vary from 10 to 60 cm in thickness. Technically speaking, ortstein is a cemented Bh, % Sand 75 90 Bhf or Bf horizon at least 3 cm thick. Those cemented % Silt 15 5 horizons that do not make the podzolic B criteria are not "true" ortsteins. Ortstein development is drainage dependent. In % Clay 10 5 poorly drained sites it is harder and covers a greater lateral % Coarse < 2 rounded G < 2 rounded G extent than in sites with better drainage. Fragments

Riverbank soils are usually associated with other soils pH (H2O) 4.0 - 4.5 4.5 - 5.0 developed in glaciofluvial sediments, such as Gagetown. BD (g/cm3) 1.20 1.50 Gagetown is sandy skeletal, i.e., gravelly or very gravelly in the parent material. Gagetown and Riverbank are Ksat (cm/hr) > 25 > 10 lithologically identical. They are separated on percent coarse AWHC (cm/cm) 0.10 - 0.15 0.05 - 0.10 fragment content. Gagetown soils have greater than 20% gravels (usually 50 to 70%) and Riverbank soils have less than 20% gravels (usually less than 2%). Riverbank soils have also been mapped with Interval soils. Interval soils have formed in coarse loamy alluvial sediments, usually silt loams to fine sandy loams, and are located within present-day flood plains. 84

Rogersville Association sugar maple, white birch and beech. As drainage conditions deteriorate the sugar maple, white birch and beech give way to The Rogersville Association consists of soils developed in red maple and yellow birch. Cedar and tamarack occur on moderately thin (1 to 2 m) deposits of acidic, fine loamy, very poorly drained sites. compact glacial till material (lodgment till) with coarse fragments of sandstone, granites, gneiss, schists and some The Rogersville association is dominated by imperfectly volcanics. Rogersville soils occur in the Maritime Plain drained Gleyed Humo-Ferric Podzols and Gleyed Podzolic portion of the study area at elevations ranging from 40 to 140 Gray Luvisols. Moderately well drained Orthic Humo-Ferric m above sea level (Fig. 55). The lodgment till may have a thin Podzols, Fragic Humo-Ferric Podzols and some Podzolic Gray surficial capping of coarse loamy ablational till or water Luvisols occur along with the imperfectly drained Rogersville reworked material. Rogersville soil materials are underlain by members where topographic conditions are more pronounced. the soft gray-green Pennsylvanian sandstone that underlies Poorly to very poorly drained Orthic Luvic Gleysols and most of the New Brunswick Lowlands. Rogersville soils Fragic Luvic Gleysols occur extensively on level to very gently occupy approximately 3,312 ha, representing 0.12% of the undulating sites. Internal drainage is restricted by a very map area. slowly permeable subsoil (less than 0.1 cm/hr saturated hydraulic conductivity) that occurs within 50 cm of the mineral soil surface. The solum permeability is usually 5 cm/hr or faster. Available water storage capacity ranges from 0.15 to 0.20 cm/cm in the solum, but is less than 0.10 cm/cm in the subsoil. Low available water storage capacity in the subsoil is due to lower total pore space as a result of compaction. Excess water as a result of snowmelt and/or heavy precipitation flows laterally as subsurface flow (seepage). Because of the prevailing level topography and restricted internal drainage, imperfectly drained sites may occupy mid to upper slope positions as well as lower slope positions. Poorly and very poorly drained conditions are strongly influenced by subsurface inflow and groundwater flow, in addition to precipitation. They occupy lower slope, toe and depressional sites.

Profile development is moderately thick, 40 to 70 cm. The common horizon sequence is LFH, Ae, Bf, Btj or Btjx and (II)Cgj, on moderately well drained sites; LFH, Ae, Bfgj, Btgj or Btxgj and (II)Cg on imperfectly drained sites; and LFH or Figure 55. Location of mapped Rogersville soils. O, Aeg, Bgf, BCg or Bxg and (II)Cg on poorly to very poorly drained sites. Soil horizon continuity is often disrupted by tree As a lodgment till, Rogersville soil parent material consists of uprooting because the imperfect and poor drainage limits successive layers of glacial debris scoured from the earth’s rooting depth. Windthrow also promotes hummocky micro surface and redeposited or plastered into place below the topography in these sites. Poorly drained profiles may have a glacier as it advanced. As such, the underlying bedrock 10 to 30 cm thick accumulation of organic debris on the lithology played an important role in soil characteristics. The surface, especially in level and depressional areas where finer textured nature of Rogersville soil parent material is Rogersville soils are associated with organic soils such as attributed to a shale component within the debris. At the time Lavillette or Acadie Siding. Climatic conditions on the of glaciation, the Pennsylvanian aged bedrock is thought to western edge of the lowlands plain adjacent to the uplands have had interbedded shale-sandstone near the surface. The boundary result in thin Bhf development in the upper B scouring nature of glacial ice readily abraded the shales. The horizon. Fragipan, indicated by the "x" suffix in the horizon softer shale (and siltstone) fragments have completely designation, is a common characteristic of Rogersville soils. disintegrated. Only fragments of the more durable sandstone It is a hardpan with high bulk density, very low organic matter remain intact. The granites, gneiss, schists and volcanics were content and slow to very slow permeability that forms in the transported in from central New Brunswick as the glacial ice lower B and C horizons. When moist, fragipans are travelled in a southeastern direction. The weight of glacial ice moderately to weakly brittle and difficult to differentiate from has resulted in the subsoil having a pseudo platy structure. the compact lodgment till. Fragipan formation is more Coarse fragment shapes vary but are mostly subangular to strongly expressed on well drained sites, but it occurs at greater subrounded. Rogersville soils have moderately stony to very depths, usually first appearing 50 to 70 cm below the mineral stony land surfaces. Stones are 1 to 10 m apart and occupy 0.1 soil surface. Poorly drained conditions have weakly developed to 15% of the surface area. Rogersville landforms are typified pans that are thinner, 20 to 30 cm thick, and have formed by undulating surface expressions with slopes of 2 to 5%. closer to the surface, at depths of 30 to 40 cm. Fragipan Well drained sites support stands of black spruce, balsam fir, formation is discontinuous in Rogersville soils. Clay 85 translocation from the upper solum has resulted in the presence Summary of general characteristics of the Rogersville Association of a weak Bt horizon. Illuvial clay accumulations form Btj, Map Symbol : RS Btgj and Btg horizons. The Bt horizon has a very weak, coarse Physiographic Region(s) : Maritime Plain, N.B. Highlands subangular blocky structure and is resistant to both root and Elevation : 40-140 m water penetration. These horizons are similar to the subsoil in Extent : 3312 ha terms of their compact consistence. Fragic layers may occur Percentage of Mapped Area : 0.12% Parent Material Type : Mineral within these horizons. The Rogersville soil texture profile Mode of Origin : Glacial till, compact consists of a loam to sandy loam solum over a loam to sandy Material Thickness : 1-2 m clay loam or clay loam subsoil. Profile coarse fragment Soil Colour : Brown content averages 10 to 25%. Coarse fragments are subangular Family Particle Size Class : Fine loamy Petrology (parent material) : Sandstone, granites, gneiss, schists and to somewhat subrounded cobbles, gravels and stones of mixed some volcanics and weathered shale lithologies - sandstone, granites, gneiss, schists and some Inherent Fertility : Medium volcanics. Rogersville soils are medium in natural fertility. Topography (slope) : Undulating (0.5-5%) The profile is acidic throughout, falling between pH(H O) 4.0 Drainage (dominant) : Imperfect 2 Classification (typical) : Gleyed Humo-Ferric Podzol and Gleyed and 5.5. Well drained soil parent materials are brown but may Podzolic Gray Luvisols be slightly reddish brown where Rogersville soils are transitional to Stony Brook soils. The profile consists of a grayish, friable, weak, fine platy Ae horizon over a yellowish red to yellowish brown, very friable, weak to moderate, fine Layer Friable upper soil Subsoil material granular Bf horizon which grades through a BC or Bt horizon material into a firm to very firm, weak, coarse platy to structureless C Depth (cm) 0 - 40 40 - 100+ horizon. A thin grayish zone of lateral leaching is usually present immediately above the compact layer. In imperfectly Texture Class Loam - sandy loam Loam - sandy clay drained soils temporarily perched water tables create a strongly loam - clay loam mottled zone along this friable-compact interface. Grayish % Sand 45 40 gley colours dominate poorly drained profiles. Average depth of friable soil material over a root or water restricting layer is % Silt 40 35 30 to 50 cm. % Clay 15 25

Rogersville association soils most closely resemble Reece soils % Coarse 10 subangular 20 subangular C/G/S in morphological appearance as well as physical and chemical Fragments C/G/S characteristics. The main difference is the petrological pH (H O) 4.5 - 5.0 5.0 - 5.5 composition of the till. Reece soils are derived from sandstone 2 and weathered shale/siltstone; Rogersville soils have a BD (g/cm3) 1.15 1.80 significant component of granites, gneiss, schists and volcanics. As a result, Reece soils tend to be slightly coarser Ksat (cm/hr) > 5 < 0.1 textured than Rogersville soils. Rogersville soils are also less AWHC (cm/cm) 0.15 - 0.20 < 0.10 permeable in the subsoil than Reece soils. While both soils have fragipans, Reece soils have more pronounced pan development. Reece soils also do not have horizons with appreciable amounts of illuviated clay (Bt horizons). Stony Brook Association Rogersville soils commonly have Bt horizons. Stony Brook is another lodgment-till soil that occurs on the Maritime Plain The Stony Brook association consists of soils developed in along with Rogersville soils. Stony Brook soils have a red to moderately thin (1 to 2 m) deposits of acidic, fine loamy, reddish brown subsoil which is the most obvious compact glacial till material (lodgment till) with soft sandstone differentiating criteria. They are also slightly heavier in coarse fragments. Stony Brook soils only occur in the lowland texture. Stony Brook soils lack the petrological variability portion of the study area, usually at elevations of 40 to 120 m found in Rogersville soils. Stony Brook soils have sandstone above sea level (Fig. 56). The thickness of the lodgment till coarse fragments exclusive of other rock types. Poorly and tends to be a uniform blanket. It is underlain by soft very poorly drained Rogersville soils are also associated with, gray-green Pennsylvanian sandstone, from which most profile or situated in, proximity to organic soils, either Acadie Siding coarse fragments have been derived. Frequently there is a thin or Lavillette. 40 to 50 cm thick mantle of Sunbury association coarse loamy ablation till on the surface. It is also possible that this capping The major limitations to biological production on Rogersville may be due to incorporation of sandy marine sediments. Stony soils are related to the drainage-compact subsoil situation. Brook soils occur below the zone of maximum post-glacial Stoniness may also be detrimental in agricultural usage. From marine submergence. They occupy approximately 151,867 a forestry perspective Rogersville soils are among the more ha, or 5.45% of the map area. productive soil types found in the lowlands. Stony Brook subsoils are very dense and compact, properties 86 that can be attributed to their mode of deposition as lodgment unsaturated zone. Available water storage capacity is 0.15 to tills plastered in place below hundreds of metres of glacial ice. 0.20 cm/cm in the solum but less than 0.10 cm/cm in the Their fine texture and red to reddish brown colour come from subsoil. On moderately well drained sites, precipitation is the incorporated red shale (35% clay content) and/or reddish dominant water source. Excess water is removed somewhat clayey marine sediments. Abrasive actions during glaciation slowly in relation to supply because of low perviousness in the have almost completely disintegrated the soft shales. Upon subsoil and lack of gradient. Conversely, subsoil compaction close examination small remnants can be identified in the soil prevents root penetration and also limits recharge of soil matrix. The soil material is a heterogeneous mixture of moisture in the solum. Because of this, some sites experience subangular to subrounded particles ranging in size from fine moisture deficiencies or droughtiness during summers with clays to stones and even the occasional boulder. Stony Brook low precipitation. Imperfectly and poorly to very poorly soils are moderately stony on the surface, with stones 2 to 10 drained sites are strongly influenced by inflow of lateral m apart occupying 0.1 to 3% of the land area. Stonier phases seepage waters. The seepage water found in these soils is may occur in complex units with Sunbury. Stony Brook usually nutrient poor, but it is often aerated, and thus still landscapes are undulating to level or flat morainal blankets. somewhat beneficial to tree growth. In poorly to very poorly Most slopes are complex but less than 5%. Bedrock outcrops drained depressional sites the water stagnates and is deleterious are not common. Well drained sites support stands of black to biological production. Most saturated conditions are due to spruce, balsam fir, white birch and some sugar maple and perched water tables or a combination of perched and true beech. On imperfectly drained sites the sugar maple and beech groundwater. are absent. Red maple, yellow birch, cedar, larch, black spruce and balsam fir occupy poorly to very poorly drained sites. Solum development is usually quite deep, 50 to 100 cm, however, only the upper 30 to 50 cm is adequately friable to be considered potential rooting zone. The common horizon sequence in moderately well drained profiles is LFH, Ae1, Bf, Ae2, (II)Bt and (II)C. The Ae2 horizon is created by lateral flow leaching. Imperfectly drained sites have a similar sequence but with distinct mottling in the upper 50 cm and prominent greyish streaks in the lower (Bt and C) horizons. Poorly to very poorly drained profiles have horizon sequences of LFH or O, Aeg, Bg, (II)Btg and (II)Cg, or, LFH or O, Aeg, Bgf, (II)Btg and (II)Cg. Shallow rooting, especially on ill drained sites, makes trees susceptible to windthrow. Hummocky micro topographies and irregular, broken soil horizons result. The Stony Brook texture profile consists of a loam to sandy loam upper solum over a loam to clay loam or sandy clay loam lower solum and subsoil. Inwashed fines tend to make soils in receiving sites slightly heavier textured. Profile coarse fragment content averages 10 to 25%. Most are subangular to flat, cobbles and gravels, but with some stones, of weathered fine- to medium-grained Pennsylvanian Figure 56. Location of mapped Stony Brook soils. grey-green sandstone. In deposits that are two tiered, i.e., ablational till over lodgment till, coarse fragments may be Dense, compact subsoils with high clay-silt content combined concentrated along the interface. These are referred to as with level to gently undulating topography results in a high “stone lines”. Stony Brook soils are derived from parent rocks proportion of wet soils. The predominant soils are imperfectly that weather moderately rapidly but yield materials that are low drained Gleyed Podzolic Gray Luvisols intermixed with some in natural fertility. The profile is acidic throughout, pH (H2O) Luvisolic Humo-Ferric Podzols. Increased clay content in the 4.0 to 5.5. Moderately well drained soils consist of a yellowish luvisolic horizon restricts downward movement of water. brown to reddish brown upper solum over characteristically Moderately well drained Podzolic Gray Luvisols (Fig. 57) and reddish brown Bt and C horizons. The Ae1 horizon is friable, Luvisolic Humo-Ferric Podzols occupy upper slope and crest weak, fine platy. It overlies a 15 to 35 cm thick, very friable, positions. Poorly to very poorly drained Orthic Luvic Gleysols weak to moderate, fine granular Bf/Bfj horizon. The Ae2 and Fera Luvic Gleysols are found on lower slope to horizon is weakly leached, friable, fine platy and often faintly depressional site locations. Internal drainage is severely mottled. The Bt and C horizons are firm to very firm and impeded by a very slowly permeable subsoil with hydraulic usually moderate, coarse platy, a structure inherited from the conductivities of less than 0.1 cm/hr. The solum is moderately parent material. Transition of the Bt horizon into the C rapid to rapidly permeable (saturated hydraulic conductivity horizon is gradual. Poorly drained materials are gleyed in the greater than 5 cm/hr). Perched water tables are common. upper horizons but the reddish coloured parent material Excess water flows through the solum and concentrates above persists in spite of reducing conditions. They also have the relatively impermeable subsoil. This saturated layer of soil thicker, 10 to 25 cm, surface organic layers. is separated from the underlying true ground water table by an 87

that limit crop production. Relatively low levels of natural fertility restrict forest productivity.

Summary of general characteristics of the Stony Brook Association

Map Symbol : SB Physiographic Region(s) : Maritime Plain Elevation : 40-120 m Extent : 151,867 ha Percentage of Mapped Area : 5.45% Parent Material Type : Mineral Mode of Origin : Glacial till, compact Material Thickness : 1-2 m Soil Colour : Red to reddish brown Family Particle Size Class : Fine loamy Petrology (parent material) : Soft gray-green sandstone and weathered shale Inherent Fertility : Low Topography (slope) : Undulating and level (0.5-5%) Drainage (dominant) : Imperfect Classification (typical) :Gleyed Podzolic Gray Luvisol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 40 40 - 100+

Texture Class Loam - sandy loam Clay loam - loam - sandy clay loam

% Sand 45 42

% Silt 35 30

% Clay 20 28 Figure 57. Moderately well drained Stony Brook soil profile. % Coarse 10 subangular C/G 20 subangular C/G Fragments Stony Brook soils share the Maritime Plain portion of the map area with other soils developed on morainal tills, the Reece, pH (H2O) 4.5 - 5.0 5.0 - 5.5 Rogersville and Sunbury associations. Stony Brook soils are BD (g/cm3) 1.15 1.80 readily differentiated based on their red to reddish brown coloured subsoils. Reece subsoils are yellowish brown and Ksat (cm/hr) > 5 < 0.1 slightly lighter textured. Rogersville subsoils may be AWHC (cm/cm) 0.15 - 0.20 < 0.10 somewhat reddish brown along soil transitional boundaries, but they are dominated by non-sandstone rock types such as granites, gneiss, schists and volcanics. Sunbury soils are readily differentiated from Stony Brook soils. Their subsoils St. Quentin Association are yellowish brown, much coarser textured, and noncompact. Some Stony Brook soils are mapped with Barrieau-Buctouche St. Quentin soils consist of peat materials found in swamps soils in areas along the coast where sandy marine deposits of formed from forest vegetation on poorly to very poorly drained varying thickness overly the lodgment till. Poorly drained sites. They are the result of a gradual building up process Stony Brook soils are often associated with organic soils, where the water table is near the surface and organic debris Lavillette and especially Acadie Siding. Organic soils have at accumulates They consist of relatively thin peatland deposits, least 40 cm of organic debris. Mineral soils, such as poorly averaging less than 2 m in thickness. The peat is composed of drained Stony Brook, may have surface organic layers up to 40 wood, leaves, needles, feather mosses and other forest debris. cm thick, but more commonly, organic surface layers are less St. Quentin soils occur in the Chaleur Uplands portion of the than 20 cm thick. survey area (Fig. 58) on level to undulating landscapes with slopes of less than 5%. Although they only account for 1,111 Most uses of Stony Brook soils are affected by the low ha, representing less than 0.04% of the survey area, St. permeability and undesirable structure of the subsoil. When Quentin soils often occur as unmapped inclusions in areas of this condition is coupled with a lack of slope gradient and the very poorly drained mineral soils. prevailing levels of precipitation and snowmelt, it results in a large percentage of Stony Brook soils with wetness problems Strong water movement from the deposit margins or from 88 mineral soils results in a nutrient-rich environment. St. Terric phases of the above listed taxa. Quentin peatlands usually have relatively level or flat surfaces. Although peat depths are relatively uniform, they decrease in St. Quentin soils are usually surrounded by very poorly to depth from the centre of the deposit outwards. Pronounced poorly drained mineral soil members. Mineral soils occurring surface patterns are usually lacking with the exception of the in areas of calcareous bedrock, such as Caribou, Thibault and presence of intermittent to semi-permanent drainage courses. Carleton, are likely associates. St. Quentin soils are Most deposits are topographically confined in depression-like differentiated from mineral soils based on the depth of organic areas. material present. To be classed as St. Quentin a soil must have at least 40 cm of mesic or humic organic material, otherwise it Vegetative cover consists of coniferous and deciduous trees, is included with the appropriate mineral soil association. tall shrubs, herbs and mosses. Tree cover is usually thick and quite diversified as a result of the nutrient-rich groundwater. St. Quentin soils have little potential use for agriculture. While Cedar, black spruce, trembling aspen, ash, red maple and alder they support often impressive forest stands, St. Quentin soils are common. require highly specialized management to ensure sustainability. They are easily damaged by harvesting operations.

Summary of general characteristics of the St. Quentin Association

Map Symbol : SQ Physiographic Region(s) : Chaleur Uplands Elevation : 300-600 m Extent : 1111 ha Percentage of Mapped Area : 0.04% Parent Material Type : Organic Mode of Origin : Swamps Material Thickness : < 2 m over mineral soil Soil Colour : Dark brown Degree of Decomposition : Moderately to very strongly decomposed Botanical Composition : Forest-fen peat Inherent Fertility : High Topography (slope) : Flat, bowl and horizontal (<1%) in an undulating landscape (<5%) Drainage (dominant) : Very poor Classification (typical) : Terric Mesisol or Terric Humisol

Figure 58. Location of mapped St. Quentin soils. Layer Friable upper Subsoil Subsoil St. Quentin soils are dominated by forest peat that is generally soil material material #1 material #2 moderately to well decomposed, with a structureless or very fine fibred structure, resulting in a slightly matted appearance. Depth (cm) 0 - 30 30 - 150 > 150 The colour is dark brown or reddish brown to almost black, pH Von Post 2 - 4 6 - 8 - greater than 5.5, and the peat material is in a mesic to humic rating state of decomposition with a rubbed fibre content that averages 10%. Von Post scale of decomposition is usually 6 % Wood 15 15 - to 8. Bulk density is high for a peat, being 0.1 to more than 0.2 Texture Class - - Sandy clay g/cm3. Saturated hydraulic conductivity is very slow at less loam than 0.1 cm/hr. Coarse- to medium-sized woody fragments are % Sand - - 60 randomly distributed throughout. The layer of forest peat is often underlain by a thin layer (less than 30 cm) of fen peat % Silt - - 15 derived from sedges. The underlying mineral material is variable, usually being the predominate material in the % Clay - - 25 surrounding area. % Coarse - - 20 angular Fragments G/C Drainage is very poor. Water table levels are at or near the surface throughout the year, resulting in ponding. Ground pH (H2O) 6.0 - 6.5 > 6.5 > 7.0 water is neutral and of elevated nutrient status. BD (g/cm3) 0.10 0.20 1.80

Where depth to the mineral soil contact is greater than 1.6 m, Ksat (cm/hr) 10 < 0.1 < 0.1 St. Quentin soils are classified as either Typic or Mesic AWHC 0.15 0.20 < 0.10 Humisols, or as Typic or Humic Mesisols, depending upon (cm/cm) their degree of decomposition. St. Quentin soils having a depth of 0.4-1.6 m to the mineral soil contact are classified as 89

Sunbury Association the melting ice. Materials consist of a heterogeneous mixture of sand, silt, clay and coarse fragments ranging from gravels The Sunbury association consists of soils developed in and cobbles to stones and boulders. Most particles are angular moderately thin (less than 2 m) deposits of acidic, coarse and sharp edged, but where fluvial action was more intense, loamy to sandy and frequently skeletal, noncompact, morainal subrounded and even rounded coarse fragments occur. glacial till material (ablational till) with coarse fragments of Meltwaters have removed many of the fines (silt and clay) soft sandstone. Sunbury soils occur only on the Maritime Plain leaving a matrix dominated by sand (greater than 60%). or lowlands portion of the study area (Fig. 59). They are found Sunbury soils are usually very stony on the surface. Stones are at elevations of 50 to 140 m above sea level. The Sunbury 1 to 2 m apart and occupy 3 to 15% of the surface area. ablational till material is underlain by either dense compact Stoniness may vary greatly over a very short distance. basal (lodgment) till or lies directly on the bedrock. In veneer Boulders are present but usually not in significant quantities to phases the bedrock occurs within 1 metre of the surface. The designate. Well drained Sunbury sites support stands of black bedrock is horizontally bedded gray-green Pennsylvanian spruce, jack pine, balsam fir and some sugar maple, white sandstone dominated by quartz but with some feldspars and birch and beech. On ill-drained sites the jack pine-sugar lesser amounts of biotite, muscovite and chloride. The coarse maple-beech component is superseded by red maple, yellow fragments within the profile have been derived from this birch, cedar and larch. sandstone bedrock. Sunbury soils occupy approximately 102,477 ha or 3.68% of the map area. The Sunbury association is dominated by well to moderately well drained Orthic Humo-Ferric Podzols (Fig. 60). Podzolization is strongly expressed, even in sites that are less than well drained. Imperfectly drained sites are Gleyed Humo-Ferric Podzols. Poorly to very poorly drained sites are Gleyed Humo-Ferric Podzols, Gleyed Eluviated Dystric Brunisols or Orthic Gleysols, depending upon the degree of impeded drainage. Internal drainage is excellent. The profile consists of a very rapidly permeable solum over a rapidly permeable subsoil. Saturated hydraulic conductivity values are greater than 5 cm/hr throughout the profile. Available water storage capacity ranges from less than 0.10 to 0.15 cm/cm, the higher values being in the solum where finer textures and organic matter contents enhance moisture retention. On well drained sites precipitation is the sole source of water. Excess water flows downward into the underlying subsoil. Imperfectly and poorly drained sites are the results of high water tables. Poorly drained sites are restricted to depressional or stream channel locations. They are typically associated with Figure 59. Location of mapped Sunbury soils. well and imperfectly drained Sunbury soils but seldom occupy a large enough area to be designated in the map unit. Ablational till is the accumulation of debris deposited from glacial ice during down wasting or melting of the glacier. Solum development in Sunbury soils varies from 35 to 55 cm Where Sunbury material has been deposited as end moraines in thickness. The common horizon sequence is: LFH, Ae, Bf, by dumping off the glacier margin as the ice melts, the till is BC and C on well to moderately well drained sites; LFH or O, thicker, masking the underlying landform configuration with Ae, Bfgj, BCgj or BCg and Cg on imperfectly or poorly hummocky or ridged mesotopography, but still maintaining the drained sites; and LFH or O, Ae, Bmgj, BCg and Cg, or LFH undulating to gently rolling surface expression characteristic of or O, Aeg, Bg and Cg on poorly or very poorly drained sites. the lowlands plain. Slopes average 3 to 9%. Where down The upper horizons in poorly drained sites are often wasting of glacial ice has been more rapid, thin layers of discontinuous because of uprooting of trees due to windthrow, Sunbury ablational till were deposited over large areas. Areas resulting in mounded micro topography. Most Sunbury soils of shallow (less than 1 m ) ablational till over bedrock are are below the maximum level of post-glacial marine mapped as Sunbury veneers. However, areas of similarly submergence (approximately 140 m asl). However, little or no shallow ablational till over lodgment till are assigned to the evidence remains to identify this event. Soil formation has appropriate lodgment till-derived soil association (usually obliterated any surficial modification that may have resulted Reece or Stony Brook). Some Sunbury map units also occupy from marine submergence. Soil textures grade from a gravelly steeply sloping positions along incised river channels, where or cobbly sandy loam solum into a cobbly or stony sandy loam slopes commonly range from 9 to more than 15% and material to loamy sand subsoil. Coarse fragment content increases with thickness is less than 1 metre over bedrock. Sunbury material depth. It ranges from 15 to 35% but may be as high as 60% in consists of nonstratified glacial drift with coarse fragments and some shallow lithic phases. Most coarse fragments are either soil particles not sorted according to size or weight, but rather channers or flagstones, but with some angular or irregular lying in the random sequence in which they were released from cobbles and stones. They are derived from soft gray-green 90

and consistence. They are reddish brown, fine loamy and firm to very firm. Reece soils may be identical to Sunbury soils in the colour (yellowish brown to brown) and morphological appearance. They differ in subsoil characteristics. Reece subsoil is fine loamy and compact (firm to very firm), whereas Sunbury subsoil is coarse loamy and friable. Guimond River soils are similar in composition to Sunbury soils, but they have stratified water-worked (rounded) sediments in comparison to the heterogenous, angular nature of Sunbury rock fragments.

Excessive stoniness and low available water holding capacity are the major limitations to agriculture, especially the stoniness. Some of the more strongly sloping Sunbury landscapes would also be a hindrance to the usage of agricultural equipment. Forestry uses are impacted by low natural fertility and droughtiness. Species selection must consider these two limitations.

Summary of general characteristics of the Sunbury Association

Map Symbol : SN Physiographic Region(s) : Maritime Plain Elevation : 50-140 m Extent : 102,477 ha Percentage of Mapped Area : 3.68% Parent Material Type : Mineral Mode of Origin : Glacial till, noncompact Figure 60. Well drained Sunbury soil profile. Material Thickness : < 2 m Soil Colour : Yellowish brown to brown Pennsylvanian sandstone. This thin, flat "channer-flagstone" Family Particle Size Class : Coarse loamy to sandy (skeletal) Petrology (parent material) : Soft gray-green sandstone shape is inherited from the sandstone which splits readily and Inherent Fertility : Low uniformly along bedding planes or joints. The sandstone is Topography (slope) : Undulating to gently rolling (3-9%) soft and highly weathered, rating less than 4 on the Mohs scale. Drainage (dominant) : Well It is dominated by quartz (60-80%) but with significant Classification (typical) : Orthic Humo-Ferric Podzol feldspars (10-30%) and biotite and muscovite (5-10%). Sunbury soils are low in natural fertility, especially exchangeable calcium and magnesium. The profile is acidic Layer Friable upper soil Subsoil material throughout, ranging from pH(H2O) 4.0 to 5.5 . In well drained material soils the parent material is yellowish brown to brown. Typically the mineral soil profile consists of a grayish, friable, Depth (cm) 0 - 45 45 - 100+ weak, fine platy Ae horizon over a yellowish red to yellowish Texture Class Sandy loam Sandy loam - loamy brown, very friable, weak to moderately fine granular Bf sand horizon which merges gradually into the friable, very weak, subangular blocky to structureless BC and then C. Mottles % Sand 70 75 and grayish gley colours modify the profile morphology in % Silt 15 15 imperfectly and poorly drained sites. However, only under the very wettest of conditions is the general podzolic sequence not % Clay 15 10 present. Occasionally, ortstein has formed in the solum, % Coarse 20 flat, subangular 30 flat, subangular resulting in a compact, very firm, massive B horizon. The Fragments C/S/G C/S/G ortstein is an irreversible, but discontinuous hardpan cemented by Fe, Al and organic complexes. It impedes downward pH (H2O) 4.5 - 5.0 5.0 - 5.5 movement of water and is a barrier to root growth, but the BD (g/cm3) 1.10 1.50 intermittent nature of its development is such that it does not significantly impact land use. Ksat (cm/hr) > 25 > 10

Sunbury association soils are most intimately associated with AWHC (cm/cm) 0.10 - 0.15 < 0.10 Reece soils, and to a lesser extent, Stony Brook soils. All three associations occur on the eastern Maritime Plain. Reece and Stony Brook soils often have a surficial capping of Sunbury material. Stony Brook soils are readily differentiated from Sunbury soils on the basis of parent material colour, texture 91

Tetagouche Association are Orthic Humo-Ferric Podzols but with some Orthic Ferro- Humic Podzols. Imperfectly drained sites are classified as The Tetagouche association consists of soils that have Gleyed Humo-Ferric Podzols, indicating the presence of developed in acidic, fine loamy, compact morainal till derived mottling and/or gleying. Poorly to very poorly drained sites from metagabbro, metabasalt, metagreywacke and some are typically Orthic Gleysols but may have some inclusions of conglomerate. Deposits are mostly less than 2 m thick Fera Gleysols. Imperfectly and poorly to very poorly drained (veneers and blankets) but some deeper phases also occur sites dominate the undulating and gently rolling landscapes. (greater than 3 m thick). Tetagouche soils are mostly located Well to moderately well drained Tetagouche soils usually in the northern portion of the Chaleur Uplands portion of the occur as significant components in more steeply sloping study area at elevations between 100 and 500 m above sea landscapes dominated by other soil types. Internal drainage is level (Fig. 61). They occupy approximately 18,079 ha, restricted by a slowly to very slowly permeable subsoil with an representing 0.65% of the map area. estimated saturated hydraulic conductivity value of less than 0.2 cm/hr. Available water storage capacity ranges from 0.25 to less than 0.10 cm/cm, decreasing with depth because of reduced total porosity in the compact subsoil. Downward movement of excess moisture through the profile is impeded by the subsoil and lateral flow or seepage occurs along the subsoil surface. Imperfectly and poorly to very poorly drained areas are strongly affected by seepage. Topographic position, lack of gradient, and high groundwater table also play a role.

Soil development is relatively thin, with solums ranging from 35 to 55 cm. The common horizon sequence on well drained sites is LFH, Ae, Bhf, Bf, Btj or BC and C. The organic layer is 3 to 10 cm thick, becoming more humified with depth. It overlies a thin (2 to 5 cm), light brownish gray coloured Ae horizon which breaks abruptly into the B horizon. The brown to dark brown Bhf horizon varies from 3 to 12 cm in thickness. It is thickest in the colder regions of the central New Brunswick Highlands. The Bhf horizon merges with a yellowish brown Bf horizon. At 35 to 45 cm the podzolic B Figure 61. Location of mapped Tetagouche soils. horizon grades into a weakly developed Btj or BC horizon . Clay translocation from the upper solum results in the The soil parent material has been deposited as ground moraine, presence of a weak Btj horizon. The Btj or BC horizon has a plastered in place under the weight of advancing glacial ice. very weak, coarse subangular blocky structure and is resistant Composition strongly reflects the incorporation of local to both root and water penetration. These transitional horizons bedrock formations composed largely of dark-coloured, basic, are similar to the subsoil in terms of their compact consistence. fine-grained volcanics. Coarse fragment content is higher They gradually grade into the unaltered parent material or C where weathered bedrock has been incorporated into thin horizon. Imperfectly drained soils have similar profiles but veneer sediments. Tetagouche soils are very stony on the are modified by periodic saturation. They are mottled and surface, with 3 to 15% of the land area occupied by coarse gleyed in the B and C horizons. An Ahe horizon up to 5 cm fragments. Boulders may be present, but not in sufficient thick may be sandwiched between the H and Ae horizons in quantities to warrant designation as a bouldery phase. imperfectly drained Tetagouche soils. The Ahe horizon Tetagouche landforms range from undulating to rolling surface formation is at the expense of the Bhf horizon formation, expressions with slopes of 2 to 9%, to some ridged and hilly which is very thin or nonexistent. Poorly to very poorly map units with slopes of in excess of 45%. Although thin, the drained horizon sequences typically consist of LFH or O, Aeg, soils are relatively uniform in thickness and bedrock outcrops Bg, Btjg or BCg, and Cg horizons. The forest duff layer is are not common enough to warrant a rocky designation. Those thicker in the poorly and very poorly drained conditions than bedrock exposures that do occur are found on topographic found in well drained counterparts, varying from 5 to 15 cm, highs and summits or along steeply inclined drainage channels but occasionally as thick as 30 cm. The Tetagouche textural that are more deeply incised into the bedrock. Well drained profile usually consists of a loam surface grading into a heavy soils of the Tetagouche association support forest communities loam to clay loam subsoil. Clay content is usually highest in of mixed softwood-hardwood forest cover type consisting of the subsoil and also tends to increase as drainage becomes yellow birch, cedar, spruce, balsam fir, sugar maple, beech, red poorer. Profile coarse fragment content varies from 10 to 25%. oak, white birch, white pine and striped maple. Poorly to very Subangular gravels and cobbles dominate. Tetagouche soils poorly drained members are dominated by cedar, black spruce, are medium in inherent fertility owing to the nature of the rock balsam fir, white birch, red maple, speckled alder and willows. types from which they have been derived. The soils are acidic

throughout, with pH(H2O) values of 4.0 to 5.5. The friable, Well to moderately well drained Tetagouche association soils weak to moderate, fine to medium, granular or subangular 92 blocky solum provides an available rooting zone of Ksat (cm/hr) > 5 < 0.2 approximately 45 cm. The underlying parent material is firm to very firm, massive or pseudoplaty, the pseudoplatiness a AWHC (cm/cm) 0.20 0.10 result of its having been plastered into place by glacial ice.

Tetagouche soils have been mapped in association with other till soils that have igneous lithology - Tetagouche Falls, Tetagouche Falls Association Nigadoo River and Popple Depot. The Nigadoo River association has the same lithology and dense compact subsoil, The Tetagouche Falls association consists of soils that have but it is coarser-textured. The Tetagouche Falls association has developed in acidic, loamy, non-compact morainal till derived the same lithology and similar textural profile, but it has a from metagabbro, metabasalt, metagreywacke and some relatively friable, non-compact subsoil. Popple Depot has conglomerate. Essentially, Tetagouche Falls soils are non- developed on a compact basal till, but of different rock types compact Tetagouche or Nigadoo River soils. Deposits range that are more quartz-based. Popple Depot is also coarse-loamy in thickness from veneers of less than 1 m thick to deeper in texture. Tetagouche soils have been mapped with phases of greater than 3 m thickness. Tetagouche Falls soils Catamaran, McGee, Long Lake and Violette in some are scattered throughout the New Brunswick Highlands and transitional areas between different bedrock formations. The Chaleur Uplands portions of the study area at elevations latter mentioned soils have developed from metasedimentary between 50 and 600 m above sea level (Fig. 62). They occupy bedrock types. approximately 48,940 ha, representing some 1.76% of the map area. The primary limitations affecting land use of Tetagouche soils are coarse fragment content (both surface and profile), soil drainage and shallowness to a compact subsoil layer. Medium inherent fertility, however, is an asset to forest production.

Summary of general characteristics of the Tetagouche Association

Map Symbol : TT Physiographic Region(s) : Chaleur Uplands Elevation : 100-500 m Extent : 18,079 ha Percentage of Mapped Area : 0.65% Parent Material Type : Mineral Mode of Origin : Glacial till, compact Material Thickness : < 2-3 m Soil Colour : Strong brown Family Particle Size Class : Fine loamy Petrology (parent material) : Metagabbro, metabasalt, metagreywacke and conglomerate Inherent Fertility : Medium Topography (slope) : Undulating and rolling to ridged and hilly (2-45%) Drainage (dominant) : Moderately well Classification (typical) :Orthic Humo-Ferric Podzol and Orthic Ferro- Humic Podzol Figure 62. Location of mapped Tetagouche Falls soils.

Tetagouche Falls soil parent material is non-compact and as such is considered to be an ablational till, however, some Layer Friable upper soil Subsoil material firmness may occur in the subsoil. The somewhat firm material consistence of the subsoil can be attributed to the composition Depth (cm) 0 - 45 45 - 100+ of the parent material in that it is loamy and acidic. The acidic nature of the subsoil does not promote soil formation physical Texture Class Loam Loam - clay loam and biochemical processes that favour the development and % Sand 45 40 stabilization of soil structure.

% Silt 35 35 Tetagouche Falls soils have subangular coarse fragments derived mostly from the underlying mafic volcanic bedrock. % Clay 20 25 The soil surface is typically very stony, with 3 to 15% of the % Coarse 10 subangular G/C 20 subangular G/C land surface occupied by coarse fragments. Well drained Fragments Tetagouche Falls soils have developed under a mixed softwood-hardwood forest cover type consisting of yellow pH (H O) 4.5 - 5.0 5.0 - 5.5 2 birch, cedar, spruce, balsam fir, sugar maple, beech, red oak, BD (g/cm3) 1.15 1.80 white birch, white pine and striped maple. Poorly to very 93 poorly drained members are dominated by cedar, black spruce, balsam fir, white birch, red maple, speckled alder and willows.

Well to moderately well drained soils of the Tetagouche Falls association are either Orthic Humo-Ferric Podzols or Orthic Ferro-Humic Podzols (Fig. 63). Imperfectly drained sites are classified as Gleyed Humo-Ferric Podzols, indicating varying oxidizing/reducing conditions due to periodic saturation. Poorly to very poorly drained sites are typically Orthic Gleysols but may have some inclusions of Fera Gleysols. Poorly and very poorly drained sites are usually restricted to localized areas such as drainage channels and small depressions in landscapes dominated by well to moderately well drained soils. Tetagouche Falls soils have moderately rapid to moderate internal drainage. The upper solum usually has moderately rapid permeability (5 to 15 cm/hr saturated hydraulic conductivity) and the subsoil has moderate to moderately slow permeability (2 to 3 cm/hr). Available moisture storage capacity exceeds 0.15 cm/cm throughout the profile and is greatest in the upper solum (0.20 to 0.25 cm/cm). Well drained sites are supplied with moisture through precipitation. In shallow to bedrock moderately well and imperfectly drained sites, precipitation may be augmented with some lateral flow or seepage along the bedrock interface. Poorly to very poorly drained sites occur only because of high groundwater levels. The soil parent material and underlying bedrock is relatively rich in nutrients and so seepage waters are beneficial to plant growth.

Soil development is relatively thin, with solums ranging from 35 to 55 cm. The common horizon sequence on well drained sites is LFH, Ae, Bhf, Bf, BC and C. The organic layer is 3 to 10 cm thick, becoming more humified with depth. It overlies a thin (2 to 5 cm), light brownish gray coloured Ae horizon which breaks abruptly into the B horizon. The upper B horizon consists of a brown to dark brown Bhf horizon 3 to 15 cm in thickness. The Bhf horizon merges with a yellowish brown Bf horizon. At 35 to 45 cm the podzolic B horizon grades into a BC horizon which then grades into the unaltered Figure 63. Well drained Tetagouche Falls soil profile. strong brown coloured parent material or C horizon. Imperfectly drained soils have similar profiles but are modified which they have been derived. The soils are acidic throughout, by periodic saturation. They are mottled and gleyed in the B with pH(H2O) values of 4.0 to 5.5. The friable to very friable, and C horizons. An Ahe horizon up to 5 cm thick may be weak to moderate, fine to medium, granular or subangular sandwiched between the H and Ae horizons in imperfectly blocky solum grades into a slightly firm weak, medium drained Tetagouche Falls soils. The Ahe horizon formation is subangular blocky subsoil. at the expense of the Bhf horizon formation, which is very thin or nonexistent. Poorly to very poorly drained horizon Tetagouche Falls soils have been mapped in association with sequences typically consist of LFH or O, Aeg, Bg, BCg, and other till soils that have igneous lithology - Tetagouche, Cg horizons. The forest duff layer is thicker in the poorly and Nigadoo River, Juniper, Popple Depot and Jacquet River. The very poorly drained conditions than found in well drained Nigadoo River association has the same lithology but is counterparts, varying from 5 to 15 cm, but occasionally as slightly coarser-textured and has a very dense compact subsoil. thick as 30 cm. The Tetagouche Falls textural profile usually Juniper, Popple Depot and Jacquet River are all derived from consists of a loam to sandy loam surface grading into a loam different rock types that are more quartz-based. All three soils subsoil. Clay content is typically around 18% in the subsoil are also slightly coarser textured, being coarse loamy but tends to be higher in poorly drained sites than in well compared to Tetagouche Falls which is loamy. Popple Depot drained sites due to inwashing of fines. Profile coarse soils also have dense compact subsoils. Tetagouche soils have fragment content varies from 15 to 35%. Subangular gravels developed from the same bedrock sources, but they are slightly and cobbles dominate. Tetagouche Falls soils are medium in finer textured and have compact subsoils. Tetagouche Falls inherent fertility owing to the nature of the rock types from soils have also been mapped with Boston Brook, Catamaran, 94

McGee, Long Lake and Thibault in some transitional areas morainal material that is the result of either ablational between different bedrock formations. The latter mentioned deposition, periglacial and other reworking of lodgment till, or soils have developed from sedimentary and metasedimentary residual development, alone or in combination. The bedrock types. underlying Devonian, Silurian and/or Ordovician age bedrock types are easily weathered. Thibault soils occupy The primary limitations affecting land use of Tetagouche Falls approximately 138,569 ha, representing 4.97% of the map soils are coarse fragment content (both surface and profile) and area. topographic conditions (excessive slope). Medium inherent fertility, however, is an asset to forest production.

Summary of general characteristics of the Tetagouche Falls Association

Map Symbol : TF Physiographic Region(s) : Chaleur Uplands Elevation : 50-600 m Extent : 48,940 ha Percentage of Mapped Area : 1.76% Parent Material Type : Mineral Mode of Origin : Glacial till, noncompact Material Thickness : <1 - >3 m Soil Colour : Strong brown Family Particle Size Class : Loamy Petrology (parent material) : Metagabbro, metabasalt, metagreywacke and conglomerate Inherent Fertility : Medium Topography (slope) : Rolling and ridged to hilly (5-70%) Drainage (dominant) : Well Classification (typical) : Orthic Humo-Ferric Podzol and Orthic Ferro-Humic Podzol

Figure 64. Location of mapped Thibault soils.

Layer Friable upper soil Subsoil material Although Thibault soil parent material is the end product of a material number of different processes, it is relatively uniform in composition. Either as a result of deposition or development, Depth (cm) 0 - 45 45 - 100+ it consist of a friable medium. Interstitial fines have been Texture Class Loam - sandy loam Loam removed from the soil matrix by washing. High coarse fragment contents (10 to 35%) prevail because of the fractured % Sand 50 47 bedrock component that has been incorporated into the profile % Silt 35 35 as a result of either glacial process or periglacial frost heaving. The parent rock types produce a characteristic flat, channery or % Clay 15 18 flaggy clast shape. Thibault soils have moderately stony to very stony land surfaces with 2 to 15% of the surface occupied % Coarse 20 subangular C/G 30 subangular C/G Fragments by stone sized clasts. Surface channers and flaggs are also abundant. The topographic conditions under which Thibault pH (H2O) 4.5 - 5.0 4.5 - 5.5 soils occur very considerably. They include undulating (2 to BD (g/cm3) 1.10 1.55 5% slope), rolling (5 to 15% slope), ridged (5 to 15% slope), hilly (15 to 45% slope), and sloping (15 to 70% slope) surface Ksat (cm/hr) 5 - 15 2 - 3 expressions. Veneers, with less than 1 m of regolith over the bedrock, are associated with the ridged, hilly and sloping AWHC (cm/cm) 0.20 - 0.25 0.20 landforms. Rocky phases of the Thibault soils are abundant in sloping map units where stream channels are deeply incised into the landscape. Scattered rock outcrops also occur along ridge or hill tops where more resistant bedrock strata persist. Thibault Association Thicker deposits are associated with areas of undulating and The Thibault association consists of soils that have developed gently rolling topography where slopes are longer and less in thin (less than 2 m thick) deposits of neutral to slightly dissected. Here, the till overburden tends to be more uniform acidic, coarse loamy non-compact morainal till derived from in thickness and bedrock outcrops are not common. Native weakly calcareous shale, slate, quartzite, argillite and vegetation on well drained Thibault soils is a diverse sandstone. Thibault soils occur mostly in the Chaleur softwood-hardwood forest composed of black and red spruce, Highlands physiographic region, and to a lesser extent in the balsam fir, white and yellow birch and sugar and red maple. Notre Dame Mountains, at elevations of 250 to 550 m above Less prolific species include white cedar, trembling aspen, sea level (Fig. 64). They have formed in loose, noncompact striped maple, mountain ash and beech. Vegetation on poorly 95 drained sites consists of such water tolerant trees as black conditions (imperfect and poor) are the result of high spruce, balsam fir, white cedar, red maple and speckled alder. groundwater levels. Intermittent springs also occur where groundwater is forced onto the land surface by a buildup of Moderately sloping landscapes combined with coarse loamy underground hydraulic pressures because of gravitational water particle size class and the open, porous nature of the subsoil, seepage along bedrock fracture planes. result in a high proportion of Thibault soils being well drained. The Thibault association is dominated by well drained Orthic Profile development averages 40 to 60 cm in thickness. The Humo-Ferric Podzols (Fig. 65). Imperfectly drained Gleyed common horizon sequence in well drained profiles is: LFH, Humo-Ferric Podzolic Thibault soils are often intermixed with Ae, Bhf (discontinuous), Bf, BC, and C. The soils generally their well drained counterparts on rolling or ridged topography. have a thin organic layer 2 to 6 cm thick dominated by L and They occupy segments of the landscapes where natural F horizons. In some profiles soil fauna have complexed the drainage is impeded ie. lower slopes, depressions, etc. Poorly colloidal humus with the mineral soil forming a transitional drained members of the Thibault association are Orthic or Fera dark gray to black, porous crumbly Ah horizon. The Gleysols. They occur as predictable inclusions in most map underlying light grayish coloured Ae horizon is 3 to 8 cm thick units but are usually restricted to narrow zones along drainage but exceeds 15 cm in some pockets where tree-throw has ways or confined to depressions. Internal drainage in Thibault disturbed the solum pattern. Transition from the A to the B soil material is good. The subsoil has 30 to 40% total pore horizon is abrupt. The 25 to 35 cm thick B horizon is a strong space of which more than one third is macropores. Based on brown colour along the upper boundary, becoming this pore size distribution, the subsoil has an estimated progressively yellower with depth. It consists of a thin permeability of moderate to moderately rapid (2.5 to 10 cm/hr discontinuous Bhf horizon overlaying a Bf horizon. saturated hydraulic conductivity). Available water storage Podzolization is not as strongly developed as in more acidic capacity decreases with depth from greater than 0.25 cm/cm in parent materials such as the McGee association. In the weakly the solum to 0.15 cm/cm in the subsoil. On well drained sites calcareous Thibault parent material, initiation of podzolic precipitation is the sole source of water supply. Excess water horizon formation was delayed until the carbonates had been flows through the profile and into the underlying vertically- leached from the upper part of the soil. Subsequently, Thibault standing, fractured bedrock. Impeded drainage conditions soils are not always podzolized to the same degree as adjacent soils that have developed in acidic parent materials. The Thibault B horizon is, however, a well developed podzolic Bf. The Bf horizon grades into a pale brown to light olive brown coloured BC and then C. Imperfectly drained profiles have a similar horizon sequence but are characterized by greyer colours or distinct to prominent mottling indicative of periodic reduction. Both the organic and Ae horizons are also usually thicker. Poorly drained soils consist of the following horizons: LFH, Aeg, Bg or Bgf, and Cg. Peaty phases are common where organic debris has accumulated to a thickness of greater than 15 cm. Mineral soil matrix colours are dull and subdued making differentiation of horizons difficult, especially where the sequence is Aeg, Bg, and Cg. Where present, the Bfg horizon is readily identifiable on the basis of prominent orange mottles. The Thibault textural profile varies from a loam-silt loam to a sandy loam. Silt plus clay content decreases from the surface downwards, indicative of the effects of weathering on soil particle size. This is particularly true of the Ae horizon which is highest in silt-plus-clay content. Imperfectly and poorly drained Thibault soils usually contain more fines in the solum than do their well drained counterparts. This is attributed to a combination of the inwashing of silt and clay from adjacent upland positions and the more pronounced influence of physical disintegration by frost action in water saturated conditions. Profile coarse fragment content averages 10 to 35% channers and flaggs. In lithic phases this may exceed 60 to 70% along the soil bedrock contact where in situ formation has taken place and the coarse fragments retain the vertically standing orientation of the bedrock. The weakly calcareous shale, slate, quartzite, argillite and sandstone parent rock is moderately rich in nutrients and weathers rapidly to release these nutrient elements into the soil. However, much of Figure 65. Well drained Thibault soil profile. the exchangeable calcium and magnesium has been lost by 96 leaching and the soil has gradually become more acidic. Soil Inherent Fertility : High reaction (pH in water) is less than 5.5 throughout the solum but Topography (slope) : Undulating and rolling to ridged, hilly and sloping (2-70%) the parent material has retained a weakly neutral status (pH Drainage (dominant) : Well greater than 5.5). Availability of plant nutrients however, is Classification (typical) : Orthic Humo-Ferric Podzol restricted by soil acidity, thus negating some of the benefits of the Thibault inherent fertility. In poorly drained conditions inwashed bases often enhance the profile nutrient content and increase the pH. There are no physically impeding layers Layer Friable upper soil Subsoil material material within the profile to restrict plant roots. The solum is moderate, medium, granular and friable. Subsoil conditions vary with Depth (cm) 0 - 50 50 - 100+ drainage. Well drained sites are usually friable and weak, fine granular to subangular blocky, but as drainage conditions Texture Class Loam - silt loam Loam - sandy loam worsen, the subsoil becomes slightly firm and very weakly % Sand 40 50 structured to amorphous. The amorphous nature of the Cg horizon in imperfectly and poorly drained soils reduces % Silt 40 38 percolation rates but is not considered to be a major factor in % Clay 20 12 determining drainage. % Coarse 10 flat C/S/G 25 flat C/S/G Thibault soils have been mapped in complex units with Fragments Carleton, Caribou, Holmesville and McGee soils and pH (H O) 4.5 - 5.5 > 5.5 occasionally Jacquet River, Nigadoo River, Long Lake, 2 Tetagouche Falls and Violette soils. Thibault, Caribou and BD (g/cm3) 1.10 1.50 Carleton soil associations have all developed on parent materials derived from weakly calcareous sedimentary or Ksat (cm/hr) > 10 2.5 - 10 metasedimentary bedrocks. Both Caribou and Carleton are AWHC (cm/cm) 0.20 - 0.25 0.15 - 0.20 fine-loamy materials in contrast with Thibault, which is coarse- loamy. Carleton soils also have dense compact subsoils. The McGee association is probably the most similar to the Thibault association in terms of soil physical and morphological Tracadie Association characteristics. Both soils have developed on non-compact coarse-loamy olive brown-coloured till materials. However, The Tracadie association consists of soils that have developed while Thibault soils have been derived from weakly in moderately thin (1 to 2 m) to very thick (sometimes in calcareous shale, slate, quartzite, argillite and sandstone parent excess of 20 m) deposits of neutral, clayey marine and rocks, McGee soils have been derived from acidic slates, glaciolacustrine sediments. Gauthier (1983) recorded up to argillite, schist, greywacke and quartzite. Holmesville soils, 100 m of marine clay in the subsurface of the Bathurst Basin. although mapped in complexes with Thibault soils, are quite Well logs also indicate significantly thick deposits along other different, having developed on lodgment till material. tidal river valleys, however, most occurrences are patchy and Holmesville soils are very compact in the subsoil. not nearly so thick. Tracadie soils are confined to the coastal margins of the Maritime Plain, but with some occurrences Land use of Thibault soils is restricted by topographic along Chaleur Bay in the New Brunswick Highlands conditions (excess slope), shallowness to bedrock, stoniness physiographic region of the study area (Fig. 66). They are and to a lesser degree by excess moisture. Where thicker mostly at elevations of less than 50 m above sea level. deposits occur on areas of moderate relief, Thibault soils have Tracadie soils cover approximately 15,590 ha, or about very good potential for growing agricultural crops climatically 0.56% of the map area. suited to the region. Thibault soils are considered highly suitable for forestry because of their inherent fertility, good Tracadie parent materials are marine or glaciolacustrine moisture holding capacity and deep available rooting zone. sediments, mostly silt and clay. They were deposited in a brackish, shallow water environment during postglacial marine Summary of general characteristics of the Thibault Association submergence and subsequently exposed when water levels Map Symbol : TH receded. Tracadie sediments have been derived from mixed Physiographic Region(s) : Chaleur Uplands, Notre Dame Mountains undifferentiated lithologies. They are rich in mica-illite and Elevation : 250-550 m chloride. Tracadie soil particles are well worn and weathered, Extent : 138,569 ha Percentage of Mapped Area : 4.97% first by stream flow, then by ocean forces, and finally, upon Parent Material Type : Mineral emergence, by soil forming factors. Most land surfaces are flat Mode of Origin : Glacial till, noncompact to very gently undulating, with less than 2% slope, and Material Thickness : < 2 m uniform, seldom interrupted by irregularities in topography. Soil Colour : Light olive brown Family Particle Size Class : Coarse loamy Valley depositions may have more relief, conforming to Petrology (parent material) : Weakly calcareous shale, slate, quartzite, pre-sedimentation structures and further modified by argillite and sandstone post-sedimentation erosion. Vegetative cover consists of water 97 tolerant species such as black spruce, cedar, tamarack, red structured Bt horizon which grades into the parent material maple, trembling aspen and alder. some 70 to 120 cm below the mineral soil surface. Immediately above the Bt horizon is a thin 3 to 10 cm thick, leached layer. The Bt and C horizons are typically pseudo platy, a structure inherited from the mode of deposition. Varving, the bedded or laminated annual sequence of deposition found in ponded freshwater, is present in varying degrees, indicative of the "brackish water" environment. Parent material colour varies from red to yellowish brown. Poorly to very poorly drained profiles usually have the following horizon arrangement: LFH or O, Aeg, Bg, Btg, and Cg. A thin (less than 10 cm thick) Ah horizon may be present at the organic-mineral soil interface. Prominent gray and brown streaks occur along vertical cracks associated with the prismatic structure of the Bt horizon.

Figure 66. Location of mapped Tracadie soils.

The Tracadie association is dominated by imperfectly drained Gleyed Gray Luvisols and Gleyed Brunisolic Grey Luvisols. These profiles are characterized by the combination of clay accumulation in the B horizon (Bt) and moderate to strong mottling and gley features. Moderately well drained sites are insignificant in areal extent. They occur as inclusions in map units dominated by either imperfectly or poorly drained members. Where they do occur they are classified as either Orthic Gray Luvisols or Brunisolic Gray Luvisols. Poorly and very poorly drained Tracadie soils are Orthic Luvic Gleysols (Fig. 67). Excess water is removed from the soil very slowly in relation to supply due to the low perviousness of the subsoil (saturated hydraulic conductivity of less than 0.1 cm/hr) and the lack of gradient. Subsurface water flow, in addition to precipitation, is the main source of water recharge. Perched water tables are common when water supply (seepage, snowmelt and precipitation) exceeds evapotranspiration. Surface water flows away so slowly that free water often ponds on the soil for a significant period of time. Available water storage capacity is high (0.20 to 0.25 cm/cm) in the upper solum (top 20 to 35 m) but relatively low (less than 0.10 cm/cm) below this, because of reduced total porosity.

Solum development may exceed 100 cm. This is the result of deep Bt horizon formation. However, the available rooting zone or friable portion of the solum seldom extends to a depth Figure 67. Poorly drained Tracadie soil profile. of more than 35 cm, and is frequently less than 25 cm thick. In imperfectly drained sites the common horizon sequence is LFH, Ae, AB or Bm, Aegj, Btgj, Btg and Cg. The In red coloured deposits the upper solum horizonation is organic-mineral soil contact is not always abrupt and there may particularly weakly expressed. Regardless of drainage, clay be a degraded Ah or Ahe horizon. The forest floor is usually accumulation in the B horizon is usually quite pronounced, a thin layer of deciduous-coniferous and related organic debris. with moderately thick clay films in many voids and channels The upper solum is friable. It consists of a well-developed and along most ped forces. The textural profile consists of a platy Ae horizon over a weak to moderate coarse granular to loam to silty clay loam surface material over a (silty) clay loam fine subangular blocky AB or Bm. This is underlain by a firm to silty clay or clay subsoil (Bt and C) Coarser textured to very firm, moderate to strong, prismatic or angular blocky surface soils occur where a thin overburden of marine sand 98 was deposited and incorporated into the solum. In the subsoil Layer Friable upper soil Subsoil material the combined silt plus clay content accounts for 80 to 95% of material the soil material. The percent clay range from 35 to 60%. Discontinuous sand lenses are an associated feature. Most Depth (cm) 0 - 30 30 - 100+ Tracadie soils are free of coarse fragments, both within the Texture Class Loam - silt clay Clay loam - silty clay profile and on the surface. Those coarse fragments that do loam occur are explained as being ice rafted debris. They consist of mixed lithological types. Some inclusions of marine modified % Sand 30 15 glacial till or glacier reworked marine/lacustrine sediments % Silt 45 45 may tend to have higher coarse fragment content. Tracadie soils are naturally moderately fertile, with high exchangeable % Clay 25 40 calcium and magnesium. However, leaching, due to prevailing % Coarse 0 0 rainfall conditions, has removed many of these bases from the Fragments upper profile, thus lowering the pH. Although the parent material is neutral to strongly calcareous, the surface soil (Ae pH (H2O) 5.0 - 5.5 > 6.5 and upper B) is strongly acidic with pH(H O) 5.0 to 5.5. Due 2 BD (g/cm3) 1.20 1.85 to its high clay content, the soil has a high cation exchange capacity and thus a good ability to retain or hold nutrients. Ksat (cm/hr) 2 - 5 < 0.1

Tracadie soils are commonly associated with other marine AWHC (cm/cm) 0.20 - 0.25 < 0.10 deposited soil types, Richibucto and Belldune River. Richibucto soils consist of marine sands, the textural opposite of the Tracadie clays. In some areas the Richibucto sand is underlain by Tracadie clays. The Belledune River soil is a Tuadook Association coarse loamy material with 20 to 50% gravels. These properties readily differentiate it from the Tracadie association. The Tuadook association consists of soils that have developed Organic soil formation is encouraged by the impeded drainage in relatively thin (mostly less than 2 m thick) deposits of conditions present in Tracadie soils. As a result, some poorly acidic, coarse loamy, compact morainal till materials derived to very poorly drained Tracadie soils are mapped in association from granite, granodiorite, diorite, granite gneiss and some with Lavillette organic soils. miscellaneous volcanics. They occur predominantly in the central to southern portion of the New Brunswick Highlands Use of Tracadie soils is affected by shallowness to a physiographic region at elevations of 300 to 700 m above sea root-restricting layer; high clay content, which enhances level (Fig. 68). Tuadook soils occupy approximately 82,171 nutrient retention and moisture holding capacities, but makes ha, or 2.95% of the map area. the soil difficult to work; and poor internal permeability and relatively level topography which make land drainage a problem. Although they are nutrient-rich materials, ill-drained conditions limit their use in forestry.

Summary of general characteristics of the Tracadie Association

Map Symbol : TC Physiographic Region(s) : Maritime Plain Elevation : < 50 m Extent : 15,590 ha Percentage of Mapped Area : 0.56% Parent Material Type : Mineral Mode of Origin : Marine or glaciolacustrine Material Thickness : Up to 20 m Soil Colour : Red to yellowish brown Family Particle Size Class : Clayey Petrology (parent material) : Undifferentiated Inherent Fertility : High Topography (slope) : Level to undulating (<2%) Drainage (dominant) : Imperfect Classification (typical) : Gleyed Gray Luvisol and Gleyed Brunisolic Gray Luvisol Figure 68. Location of mapped Tuadook soils.

The soil parent material has been deposited as ground moraine, plastered in place under the weight of advancing glacial ice. Composition strongly reflects the incorporation of local bedrock formations. Thin mantles of ablational till may be 99 present on the surface. Coarse fragment content is particularly The upper reddish brown to strong brown Bhf horizon varies high where weathered bedrock has been incorporated into thin from 5 to 15 cm in thickness. It merges with a yellowish veneer sediments. Tuadook soils are very stony on the surface, brown Bf horizon which gradually grades into the brown with 3 to 15% of the land area occupied by coarse fragments. parent material. Morphological appearance may be deceptive. Boulders are common but usually not in sufficient quantities Significant amounts of translocated iron and aluminum are to warrant designation as a bouldery phase. Tuadook often present in horizons that display little colour change from landforms are dominated by rolling surface expressions with the parent material. Imperfectly drained soils have similar slopes varying from 5 to 30%. Some undulating (2 to 5% slope) and hilly (9 to 45% slope) map units also occur. The soils are relatively uniform in thickness and bedrock outcrops are not all that common. Those bedrock exposures that do occur are found on topographic highs and summits or along steeply inclined drainage channels that are more deeply incised into the bedrock. Well drained soils of the Tuadook association support forest communities of yellow birch, white birch, sugar maple, red maple, striped maple, red oak, white spruce and balsam fir. On poorly to very poorly drained sites the tree vegetation consists of black spruce, balsam fir, red maple, yellow birch and some cedar.

Tuadook soils are dominated by well drained Orthic Ferro- Humic Podzols with some Orthic Humo-Ferric Podzols (Fig. 69). Climatic conditions in central New Brunswick are conducive to the accumulation of organic matter in the podzolic B horizon. Most Tuadook soils have enough organic carbon to qualify for the Ferro-Humic Podzol great group. The remaining well drained soils are Humo-Ferrics. Ferro-Humic podzolization is not as strongly expressed along the eastern and southern edges of the Tuadook range where the New Brunswick Highlands merge with the Maritime Plain, which has a slightly milder climate than the Highlands. Well to moderately well drained conditions dominate. Significant hectarages of imperfectly drained Tuadook soils occur as Gleyed Humo-Ferric Podzols. Under these drainage conditions, an Ahe horizon up to 10 cm thick may develop in lieu of the Ae horizon. The Ahe horizon usually develops at the expense of Bhf horizon thickness. Poorly drained soils of the Tuadook association are Orthic Gleysols. They are found more extensively in gently undulating landscapes, but also occur as localized areas in depressions and along drainage channels in more strongly sloping map units. Internal drainage Figure 69. Well drained Tuadook soil profile. is restricted by a slowly to very slowly permeable subsoil with an estimated saturated hydraulic conductivity value of less than profile horizons but with thicker LFH horizons (5 to 10 cm) 0.5 cm/hr. Available water storage capacity ranges from 0.20 and are mottled in the B and C horizons, especially a thin zone to 0.10 cm/cm, decreasing with depth because of reduced total immediately above the compact subsoil where water is porosity in the compact subsoil. Well drained sites are perched. The Ae horizon may be irregular or broken because supplied with water solely via precipitation. Downward of tree uprooting due to windthrow. Poorly to very poorly movement of excess moisture through the profile is impeded drained horizon sequences lack a podzolic B horizon. They by the subsoil and lateral flow or seepage occurs along the consist of LFH or O, Aeg, Bg, BCg, and Cg horizons. The subsoil contact. Imperfectly and poorly to very poorly drained forest duff layer is usually thicker than found in well and areas have developed because of a combination of topographic imperfectly drained counterparts. In some profiles an Ah position, lack of gradient, subsoil compaction, seepage and horizon may be found in place of the thicker organic horizon. high groundwater table. The Tuadook textural profile consists of a loam to silt loam or sandy loam (8 to 18% clay) throughout. Profile coarse Soil development varies from 40 to in excess of 60 cm in fragment content averages 15 to 35%, with a preponderance of thickness. The common horizon sequence on well drained subangular to somewhat subrounded cobbles and stones. sites is LFH, Ae, Bhf, Bf, BC and C. The organic layer Poorly and very poorly drained sites may have a “stone- averages 5 cm thick. It overlies a thin (5 to 10 cm), ashy pavement” on the mineral soil surface below the organic coloured Ae horizon which breaks abruptly into the B horizon. layers. Tuadook soils are low in inherent fertility and acidic 100 throughout. pH(H2O) values range from less than 4.0 to only % Clay 15 12 slightly greater than 5.0. The solum is friable to very friable, and varies from a weak to moderate, medium platy structure in % Coarse 20 subangular C/S 30 subangular C/S the Ae to a weak, fine to medium, granular or subangular Fragments blocky structure in the B. The subsoil is firm to very firm and pH (H O) 4.5 - 5.0 4.5 - 5.0 massive, breaking to coarse pseudoplaty. 2 BD (g/cm3) 1.10 1.80 The Tuadook association is most commonly found with Ksat (cm/hr) 2 - 5 0.1 - 0.5 members of the Juniper association. While both soils have been derived from materials of similar lithological origin, they AWHC (cm/cm) 0.15 - 0.20 0.10 are strikingly different in many respects. The most obvious difference is subsoil compaction, and associated characteristics. Tuadook subsoils have firm to very firm 3 consistence, high bulk density (greater than 1.75 gm/cm ) and Violette Association voids consisting predominantly of micro pores. Juniper subsoils are loose and friable, lower in bulk density (usually 3 The Violette association consists of soils that have developed less than 1.55 gm/cm ) and have a higher proportion of macro in relatively thin (less than 2 m thick) deposits of acidic, fine pores. Juniper soils are coarse-loamy to sandy in particle size loamy, compact morainal till sediments derived from quartzite class while Tuadook are more “modal” coarse loamy. Along and sandstones with miscellaneous argillite, slate and transition zones Tuadook soils have also been mapped in schists. Essentially, Violette are the fine-loamy equivalent of complexes with Catamaran and Long Lake soils. Holmesville. They occur in the Chaleur Uplands and New Brunswick Highlands physiographic regions of the study area Excluding problems due to wetness in imperfectly and poorly at elevations of 300 to 700 m above sea level (Fig. 70). to very poorly drained locations, the dominant feature Violette soils occupy approximately 32,076 ha, or 1.15% of affecting land use is coarse fragment content (both surface and the map sheet. profile). Excessive stones preclude their use for agriculture and impact on their use for forestry. Topographic conditions (excessive slope) and the presence of a subsoil restricting layer which impedes root penetration and water percolation, also impact on land use. Low inherent fertility limits potential forest crops.

Summary of general characteristics of the Tuadook Association

Map Symbol : TU Physiographic Region(s) : N..B. Highlands Elevation : 300-700 m Extent : 82,171 ha Percentage of Mapped Area : 2.95% Parent Material Type : Mineral Mode of Origin : Glacial till, compact Material Thickness : <2 m Soil Colour : Yellowish brown to brown Family Particle Size Class : Coarse loamy (skeletal) Petrology (parent material) : Granite, granodiorite , diorite, granite gneiss and some volcanics Inherent Fertility : Low Figure 70. Location of mapped Violette soils. Topography (slope) : Rolling, hilly and sloping (5-45%) Drainage (dominant) : Moderately well Classification (typical) : Orthic Ferro-Humic Podzol and Orthic The soil parent material has been deposited as ground moraine, Humo-Ferric Podzol plastered in place under the weight of advancing glacial ice. Parent material composition strongly reflects the incorporation of local bedrock formations. The till is a heterogeneous mixture of subangular-shaped particle sizes ranging from silts Layer Friable upper soil Subsoil material and clays to cobbles and stones. Violette soils are generally material not too stony to prevent their use for agriculture, with usually Depth (cm) 0 - 50 50 - 100+ less than 3% of the land surface area occupied by coarse fragments. Boulders are not common. Violette soils are found Texture Class Loam - silt loam or Loam - sandy loam on landforms varying from undulating or gently rolling to hilly sandy loam or sloping. Slopes of 5 to 15% are typical, but some slopes are % Sand 40 45 up to 45%. Although Violette landscapes are bedrock controlled, bedrock exposures are rare. Well drained soils of % Silt 45 43 the Violette association support forest communities of sugar 101 maple, beech, yellow birch, red oak, red and white spruce, ranging up to 30 cm thick. The Violette textural profile balsam fir, red maple and pin cherry. On poorly to very poorly consists of a loam to clay loam or sandy clay loam with 18 to drained sites the tree vegetation consists of black spruce, cedar, 35% clay in the subsoil. Surface textures are commonly speckled alder and balsam fir, with some red maple, tamarack loams, silt loams, clay loams or silty clay loams. Profile coarse and willows. fragment content varies from 10 to 25%, with a preponderance of subangular to somewhat subrounded gravels and cobbles. Well to moderately well drained Violette soils are Orthic Humo-Ferric Podzols and Podzolic Gray Luvisols (Fig. 71). They are found on the more steeply sloping landscapes. In these landscapes, poorly drained conditions are confined to relatively narrow drainage channels. Slow internal permeability contributes to impeded drainage conditions. Downward movement of excess moisture through the profile is impeded by the subsoil, resulting in lateral flow or seepage, particularly in the spring after snowmelt. Seepage results in wet lower slope and depressional positions. Even sites with significant slopes may be affected by wetness. Imperfectly and poorly drained Violette soils occur more extensively on undulating topography. Imperfectly drained Violette soils are Gleyed Humo-Ferric Podzols and Gleyed Podzolic Gray Luvisols. Poorly drained members are Orthic Gleysols or Orthic Luvic Gleysols. Internal drainage is restricted by a slowly permeable subsoil with an estimated saturated hydraulic conductivity value of less than 0.1 cm/hr. The solum is moderately permeable (saturated hydraulic conductivity of 2.0 to 5.0 cm/hr). Available water storage capacity ranges from 0.20 to 0.10 cm/cm, decreasing with depth because of reduced total porosity in the compact subsoil. Well to moderately well drained sites are supplied with water mostly via precipitation. Imperfectly and poorly to very poorly drained areas have developed because of a combination of topographic position, lack of gradient, subsoil compaction, seepage and high groundwater table.

Soil development varies from 35 to 80 cm in thickness. The common horizon sequence on well to moderately well drained sites is LFH, Ae, Bhf, Bf, BC or Bt and C. O horizons may occur under coniferous forests where mosses dominate the ground vegetation. The organic layer is 2 to 10 cm thick, becoming more humified with depth. It overlies a thin (5 to 10 cm), white, ashy coloured Ae horizon which breaks abruptly Figure 71. Moderately well drained Violette soil profile. into the B horizon. The upper strong brown to dark reddish brown Bhf horizon varies from 2 to 5 cm in thickness. It Violette soils are medium in inherent fertility and acidic merges with the brown to yellowish brown Bf horizon which throughout, with pH(H2O) values of 4.0 to 5.5. The friable to gradually grades into the oxidized olive to grayish brown very friable, weak to moderate, fine to medium, granular or parent material. At 35 to 45 cm the podzolic B horizon grades subangular blocky solum overlies a firm to very firm, massive into a BC, Btj or Bt horizon, which grades into the unaltered to medium platy subsoil. The subsoil is dense and compact parent material or C horizon between 45 and 80 cm from the and resists deformation. Subsoil bulk densities often exceed mineral soil surface. Imperfectly drained soils have similar 1.80 gm/cm3 and voids consist primarily of micro pores. profile horizons but are modified by periodic saturation. They are mottled in the B and C horizons, especially a thin zone The Violette association has been mapped in complexes with immediately above the compact subsoils where water is members of the Boston Brook, Caribou, Carleton, Catamaran, perched. The Ae horizon is often irregular or broken because Long Lake, McGee and Thibault associations. The Boston of tree uprooting due to windthrow. Poorly to very poorly Brook, Caribou, McGee, and Thibault soils have all developed drained horizon sequences lack a podzolic B horizon. They on non-compact till deposits in comparison to the compact consist of LFH or O, Aeg, Bg, and Cg horizons. A Btg subsoil of the Violette association. In addition, McGee and horizon may be present between the Bg and Cg horizons. The Thibault soils are coarse-loamy compared to the fine-loamy forest organic layer is thicker in the poorly and very poorly Violette soil. Caribou soils have developed on fine loamy drained conditions than found in well drained counterparts, materials that are derived from calcite-rich rock types. Boston 102

Brook is most similar in parent material mineralogical LAND TYPES composition and can be considered as a non-compact Violette soil equivalent. Carleton, Catamaran and Long Lake soils have Salt Marsh (SM) all developed on compact lodgment tills, but the Catamaran and Long Lake association soils are coarse loamy with less Salt marsh represents those areas of undifferentiated marine than 18% clay in the subsoil while Violette soils have in excess deposits along the coast or tidal rivers which are submerged of 18% clay. Carleton soils are similar in physical appearance at high tide by brackish to strongly saline water. They to Violette soils. They are differentiated on lithological and consist of flat very poorly drained land that is usually related differences. Carleton soils have formed in till materials covered by a thick mat of salt tolerant water-loving plants derived from weakly calcareous slates, shales and fine-grained and plant debris. These units are scattered along the coast sandstones with some limestone. As a result, Carleton soils are line from Chatham to Dalhousie. Salt marsh has been richer in nutrients and have subsoils with higher pH values, pH mapped in six polygons, occupying 669 ha. 6.5 and greater.

The dominant features affecting land use of Violette Sand Dunes (SD) association soils are related to problems due to wetness as a result of the presence of a subsoil restricting layer which Sand dunes consist of loose sand deposited by wind action impedes both root penetration and water percolation. into ridge-like piles. They are located above high tide level However, Violette soils are medium in natural fertility and are along the coast. Sand dunes occupy 140 ha, having been quite productive from a forestry perspective wherever wetness mapped in only 3 polygons. conditions are not excessively restricting.

Summary of general characteristics of the Violette Association Water (WA)

Map Symbol : VO Physiographic Region(s) : Chaleur Uplands, N.B. Highlands These are small water bodies that appear as unnamed units on Elevation : 300-700 m the soil map. They usually consist of fresh water but in some Extent : 32,076 ha instances along the coast they may include salt or brackish Percentage of Mapped Area : 1.15% water. Forty four (44) polygons were designated as water. Parent Material Type : Mineral Mode of Origin : Glacial till, compact They occupy a total of 5581 ha. Material Thickness : < 2 m Soil Colour : Light olive brown Family Particle Size Class : Fine loamy Petrology (parent material) : Quartzite, sandstone and some shale, argillite and slate Inherent Fertility : Medium Topography (slope) : Rolling and undulating to hilly (2-45%) Drainage (dominant) : Moderately well Classification (typical) : Orthic Humo-Ferric Podzol and Podzolic Gray Luvisol

Layer Friable upper soil Subsoil material material

Depth (cm) 0 - 40 40 - 100+

Texture Class Loam - silt loam Loam - clay loam

% Sand 40 40

% Silt 40 30

% Clay 20 30

% Coarse 10 subangular G/C 25 subangular G/C Fragments

pH (H2O) 4.5 - 5.0 5.0 - 5.5

BD (g/cm3) 1.20 1.80

Ksat (cm/hr) 2 - 5 < 0.1

AWHC (cm/cm) 0.20 0.10 103

PART 5. ELECTRONIC DATA FILES

The conventional product of a soil survey such as Soils of suitably handled separately. Plant nutrient supply is Central and Northern New Brunswick consists of a high manipulated by management, especially in agriculture. quality paper map with legend, and an accompanying report, Therefore, the ability of soils to supply water to growing like this one. The soil map portrays the extent and location plants is the focal point of these files. This does not of the soils and the soil report provides detailed technical preclude their use for other applications, but rather indicates information about the soils and land surface. With the that they may at times be lacking in some specific properties increased application of computer technologies to data required to make an assessment. handling, a second product is also available - soil survey information, both polygon lines and map unit attribute data, Core properties of these attribute files consist of the in electronic format. This allows for greater ability to following features: manipulate and apply the information in a consistent and timely manner. - drainage - water table The polygon and map attribute data in this report are stored - rooting depth nationally in the National Soils DataBase (NSDB) in the - texture Canadian Soil Information System (CanSIS), and - organic matter provincially in the New Brunswick Agricultural Land - pH Information System (NB'ALIS'). CanSIS is maintained by - base saturation the Eastern Cereal and Oilseed Research Centre, Research - cation exchange capacity Branch, Agriculture and Agri-Food Canada, in Ottawa and - water holding capacity can be accessed via its web page at - saturated hydraulic conductivity http://sis.ag r.gc.ca/cansis. NB'ALIS' is a joint federal- - bulk density provincial government system located in the Land and - electrical conductivity Environment Branch, New Brunswick Department of - slope Agriculture, Fisheries and Aquiculture, in Fredericton, New - stoniness Brunswick. Both CanSIS and NB'ALIS' are based on - taxonomy to the Subgroup level commercially available geographic information systems - state of decomposition (Organic soils) (GIS). - wood content (Organic soils)

GIS is designed to manage and manipulate large volumes of FILE STRUCTURE information that are spatially oriented. The ability to handle relationships among locations is the geographic feature of a The data is stored in five related files: GIS that sets it apart from a standard data base information system. It also has analytical capabilities. CanSIS uses Project File (PF) - documentation on survey specifications, ARC/INFO software while NB'ALIS' uses CARIS etc. from the Soil Survey Report. (Computer Aided Resource Information System) software. Polygon Attribute Table File (PAT) - links map polygons to Data exchange protocols have been established between the soil map units. two systems to ensure that information can be easily Soil Map Unit File (SMUF) - links soil map units to soil transferred back and forth. These systems are also names and landscape modifiers. compatible with most other land information systems. Soil Names File (SNF) - links soil names to attributes that pertain to the whole soil. Polygon data is essentially line information to define the Soil Layer File (SLF) - links soil names to attributes that map polygon boundaries and location. It is stored in a series vary in the vertical direction. of x-y coordinates referenced to a base map. This defines the geographic location aspect of the map polygon. Each polygon has an associated reference to link it with map Project File (PF) attribute files that describe the polygon. The following information is included in the PF file: As a system serving agricultural, forestry, and environmental needs, the information stored in these attribute files is - survey intensity level primarily concerned with the biological productivity of the - publication scale soils. Biological productivity is controlled by the - photography scale availability of energy, water, and nutrients. Since energy - sampling/observation strategy (free, transect, grid, etc.) availability is controlled by atmospheric climate, it is most - symbol configuration including concept of soil map unit 104

"building blocks" (series, association, etc.) 9 SOIL_CODE3 CHAR 3 - authors and contributors 10 MODIFIER3 CHAR 3 - publication date 11 EXTENT3 NUMERIC 2 - analytical methods 12 SLOPEP1 NUMERIC 5 1 - estimate of reliability 13 SLOPEP2 NUMERIC 5 1 - ARC/INFO library 14 SLOPEP3 NUMERIC 5 1 - date of last revision 15 STONE1 CHAR 1 16 STONE2 CHAR 1 17 STONE3 CHAR 1 Polygon Attribute Table File (PAT) 18 DATE DATE 8 YY.MM.DD ______

The purpose of the polygon attribute table file is to link 1 SMUF file field name descriptions are listed below. polygon numbers to soil map units. For the purpose of this discussion, a soil map unit is the entire symbol found within PROVINCE Code for province, i.e., NB for New a polygon drawn on the soil map. An explanation of the soil Brunswick map symbol from this report is given in PART 3. SOIL MAPUNITNOM Soil map unit symbol as coded in MAPPING METHODOLOGY, Map symbol. CanSIS from the original paper map SOIL_CODE Three character code for the soil name The list of attributes for the PAT file is as follows: (SOIL_CODE1, SOIL_CODE2, SOIL_CODE3) 1 Field Field Name Type Width Dec MODIFIER Three character code to show soil variations. The modifier applies to the 1 AREA FLOATING 4 3 soil name and the soil code 2 PERIMETER FLOATING 4 3 (MODIFIER1, MODIFIER2, 3 SOIL# BINARY 4 MODIFIER3) 4 SOIL-ID BINARY 4 EXTENT Percent of the map unit occupied by a 5 MAPUNITNOM CHAR 60 specific soil ______SLOPE Slope steepness in percent (SLOPEP1, 1 PAT file field name descriptions are listed below. SLOPEP2, SLOPEP3) STONE Stoniness class (STONE1, STONE2, AREA Area of polygon in square metres STONE3) PERIMETER Perimeter of polygon in metres DATE Date of last revision SOIL# Internal system number SOIL-ID Polygon number MAPUNITNOM Map symbol Soil Names File (SNF)

This file contains information that applies to the entire soil. Soil Map Unit File (SMUF) A record in the SNF file is unique with respect to the A record in the SMUF file is unique with respect to the following fields: following fields: PROVINCE PROVINCE SOIL_CODE MAPUNITNOM MODIFIER LU The list of attributes for the SMUF file is as follows: The list of attributes for the SNF file is as follows: Field Field Name1 Type Width Dec Field Field Name1 Type Width Dec 1 PROVINCE CHAR 2 2 MAPUNITNOM CHAR 60 1 PROVINCE CHAR 2 3 SOIL_CODE1 CHAR 3 2 SOILNAME CHAR 24 4 MODIFIER1 CHAR 3 3 SOIL_CODE CHAR 3 5 EXTENT1 NUMERIC 3 4 MODIFIER CHAR 3 6 SOIL_CODE2 CHAR 3 5 LU CHAR 1 7 MODIFIER2 CHAR 3 6 KIND CHAR 1 8 EXTENT2 NUMERIC 2 7 WATERTBL CHAR 2 105

8 ROOTRESTRI CHAR 1 Field Field Name1 Type Width Dec 9 RESTR_TYPE CHAR 2 10 DRAINAGE CHAR 2 1 PROVINCE CHAR 2 11 MDEP1 CHAR 4 2 SOIL_CODE CHAR 3 12 MDEP2 CHAR 4 3 MODIFIER CHAR 3 13 MDEP3 CHAR 4 4 LU CHAR 1 14 ORDER CHAR 2 5 LAYER_NO CHAR 1 15 S_GROUP CHAR 4 6 HZN_LIT CHAR 1 16 G_GROUP CHAR 3 7 HZN_MAS CHAR 3 17 PROFILE CHAR 14 8 HZN_SUF CHAR 5 18 DATE DATE 8YY.MM.DD 9 HZN_MOD CHAR 1 19 SLFNA CHAR 1 10 UDEPTH NUMERIC 3 ______11 LDEPTH NUMERIC 3

1 12 COFRAG NUMERIC 3 SNF file field name descriptions are listed below. 13 DOMSAND CHAR 2 PROVINCE See SOIL MAP UNIT FILE 14 VFSAND NUMERIC 3 SOILNAME Assigned soil name i.e., Caribou 15 TSAND NUMERIC 3 SOIL_CODE See SOIL MAP UNIT FILE 16 TSILT NUMERIC 3 MODIFIER See SOIL MAP UNIT FILE 17 TCLAY NUMERIC 3 LU Land use (agriculture or native) 18 ORGCARB NUMERIC 5 1 KIND Kind of soil (mineral, organic, etc.) 19 PHCA NUMERIC 4 1 WATERTBL Water table characteristics 20 PH2 NUMERIC 4 1 ROOTRESTRI Soil layer that restricts root growth 21 BASES NUMERIC 2 RESTR_TYPE Type of root restricting layer 22 CEC NUMERIC 3 DRAINAGE Soil drainage class 23 KSAT NUMERIC 6 3 MDEP Mode of deposition (MDEP1, MDEP2, 24 KP0 NUMERIC 3 MDEP3) 25 KP10 NUMERIC 3 ORDER Soil Order (Canadian System of Soil 26 KP33 NUMERIC 3 Classification, CSSC) 27 KP1500 NUMERIC 3 S_GROUP Soil Subgroup (CSSC) 28 BD NUMERIC 4 2 G_GROUP Soil Great Group (CSSC) 29 EC NUMERIC 3 PROFILE Representative soil profile reference 30 CACO3 NUMERIC 2 DATE Date of last revision 31 VONPOST NUMERIC 2 SLFNA Denotes presence of soil layer file 32 WOOD NUMERIC 2 records 33 DATE DATE 8 YY.MM.DD ______

1 Note: For fields 12 and 14-32, a three digit numeric field for the number Soil Layer File (SLF) of observations is optional. A code of zero (0) indicates an estimate.

2 This file is designed to handle attributes which vary in a SLF file field name descriptions follow. vertical direction, i.e., soil profile information. The mean value is reported for each attribute. The method of analysis PROVINCE See SOIL MAP UNIT FILE is listed in the project file. SOIL_CODE See SOIL MAP UNIT FILE MODIFIER See SOIL MAP UNIT FILE A record in the SLF file is unique with respect to the LU See SOIL NAMES FILE following fields: LAYER_NO 1-9, Horizon number

HZN_LIT Canadian System of Soil Classification PROVINCE (CSSC) horizon lithological discontinuity SOIL_CODE HZN_MAS CSSC master horizon (upper case) MODIFIER HZN_SUF CSSC horizon suffix (lower case) LAYER_NO HZN_MOD CSSC horizon modifier LU UDEPTH Upper horizon depth (cm) LDEPTH Lower horizon depth (cm) The list of attributes for the SLF file is as follows: COFRAG Coarse fragments (% by volume) DOMSAND Dominant sand fraction size VFSAND Very fine sand (% by weight) TSAND Total sand (% by weight) 106

TSILT Total silt (% by weight) The five files for the Soils of Central and Northern New TCLAY Total clay (% by weight) Brunswick are stored under the following names: ORGCARB Organic carbon (% by weight) PHCA pH in calcium chloride PFCNNB.TXT ASCII Format PH2 pH in water PATCNNB.DBF dBase Format BASES Base saturation (%) SMUFCNNB.DBF dBase Format CEC Cation exchange capacity (meq/100 g) SNFCNNB.DBF dBase Format KSAT Saturated hydraulic conductivity (cm/h) SLFCNNB.DBF dBase Format KP0 Water retention at 0 kilopascals KP10 Water retention at 10 kilopascals While application of the data sets using a GIS allows for the KP33 Water retention at 33 kilopascals ability to display results geographically , i.e., on maps, lack KP1500 Water retention at 1500 kilopascals of such a system does not preclude analyses of the attribute BD Bulk density of the soil matrix (g/cm3) file information. These data files are easily uploaded to a EC Electrical conductivity (dS/m) personal computer and can be analysed with any number of CACO3 Calcium carbonate equivalent (%) commercial database management software programs. The VONPOST von Post estimate of decomposition interpretations presented in the next section of this report are WOOD Volume (%) of woody material based on these files. DATE Date of last revision 107

PART 6. INTERPRETATIONS - SINGLE FACTOR AND GENERAL AGRICULTURE AND FORESTRY RATINGS

The purpose of soil survey is to enhance the ability to presented in Dillon et al. (1996) in which potential for predict, and to make precise, differential interpretations potato land expansion is based on inherent soil limitations, from area to area that can be used in land-use decision- climatic suitability, land cover type and property ownership making. Groupings or interpretations of soils and considerations. landscapes are techniques that are used to make soil information and maps more understandable to users (Olson In this report, interpretations will be limited to a presentation 1981). It is often difficult for the non-soils specialist to of the more important single-factor soil properties and comprehend all the intricate details provided in a soil general assessments for agriculture and forestry (Table 5). survey. Interpretations are a synthesis of soil survey data to These interpretations are for the dominant soil and facilitate its use, as not all readers/users will be equally well landscape elements in the map symbol. By no means is this versed in the use and application of soils information. Soils an exhaustive list of all possible interpretations that can be interpretations or groupings allow users such as planners and made. This is only the "tip of the iceberg." As previously developers to consider only those soil properties and mentioned, interpretations can range from those for very characteristics that are important for their specific intended specific reasons, to those of a much more general nature. uses. Soils interpretations are typically stratified into three Interpretations should be commensurate with the level of categories: single-factor or single parameter; soil suitability, detail provided by the survey and thus the scale of mapping. limitation or capability; and integrated soil/non-soil The soils mapping presented in this survey is 1:250,000 or assessments. exploratory in nature. However, while the information provided is not appropriately detailed for interpreting soil The simplest form of soil survey interpretation is a map or suitability for site-specific use, it can still prove valuable for table that shows a “single-factor” soil condition (Olson estimates of the different potential problems/opportunities 1981). These maps depict or present core properties of the that exist in different areas of the region. soils and landscapes that are mapped in the soil survey, such as drainage, depth to a compact layer, depth to bedrock, Soil maps remain useful long after the soil interpretations stoniness, rockiness, slope and soil texture. Because only published with them have become outdated. It should also one factor is considered, these maps are readily understood be remembered that these interpretations are not and can be very effective at showing the limitations to, or recommendations, but rather are indications of potential conversely the opportunities for, a given land use. difficulties, or conversely, potential opportunities, that the land base offers to various uses. On-site investigation is By “overlaying” or considering several different single- required prior to any actual usage of the land. factors at once, soils can be grouped to show suitability, limitations or capabilities for a given use. Soils interpretive guidelines for various agricultural crops (alfalfa, apples, SINGLE-FACTOR SOIL MAP UNIT CONDITIONS cereals, forages, potatoes, etc), forest tree species (balsam fir/white spruce, black spruce, eastern white cedar, jack Depth to bedrock (m) - Shallowness to bedrock limits the pine/red pine, white pine, sugar maple, white ash, yellow available rooting zone. It also has severe limitations on any birch, trembling aspen), urban development (frost action, land uses requiring moderately deep soil excavations, such housing, roads and streets, septic tank absorption fields, as subsurface tile drain installation in agriculture and for sewage lagoons), recreation (outdoor living, paths and basement construction, land-levelling for athletic fields and trails), and source materials (gravel, horticultural peat, installation of septic tank filter fields. Veneers (v) consist of roadfill, sand, topsoil) have been developed and used in less than 1 m of unconsolidated material over bedrock. New Brunswick (Wang and Rees 1983, Atlantic Advisory They are too thin to mask underlying irregularities in the Committee on Soil Survey 1988, Fahmy and Rees 1996). bedrock. Blankets (b) are moderately thin (1 to 2 m) Categories are made for each soil characteristic that is mantles of unconsolidated material thick enough to mask considered important to the specific use and limits are set minor irregularities in the underlying bedrock but still accordingly. conform to the general bedrock topography. Where no depth to bedrock is reported, the soil material is considered Integration of soil/landscape and non-soil themes is the third to be greater than 2 m thick. and most complicated form of soil interpretation. Most land evaluation requires other “non-soil” information for a more Depth to compact layer (cm) - The thickness of friable soil complete assessment of land potential. Climate, land use material available for root growth and water percolation is and property ownership are three other essential an important consideration in both agricultural and forest components. An example of this kind of interpretation is crop production and land management. Dense compact 108 subsoil layers resist penetration of plant roots and Fertility - Soil fertility is the quality of the soil that enables percolation of water. These soils are also late to dry in the it to provide the proper balance of nutrients for plant growth. spring and easily saturated (perched zone of saturation) by Mineralogy or petrographic origin of the soil materials is a high intensity or prolonged rainfall. Shallow rooting of determining factor in inherent site nutrient status. The crops may result in plant nutrient deficiencies, lack of composition of parent rock materials contribute largely to resistance to mid-summer drought, and winter damage due the chemical characteristics and pH of soil. Some rock types to frost heaving. Water percolation to subsurface drainage are rich in bases and weather rapidly, resulting in soils with lines is also impeded. Soil layers with bulk densities (BD) potentially high nutrient status. Other rocks contain few greater than 1.60 g/cm3 or permeabilities of less than 1.0 bases or are more resistant to weathering and release cm/hr, or both, are considered restricting layers. nutrients more sparingly. For a more detailed discussion on soils and tree nutrient supply, the reader is referred to Forest Drainage or wetness - Soil drainage refers to the rapidity soils of New Brunswick by Colpitts et al. (1995). While and extent of the removal of water from the soil in relation natural or inherent fertility of the soil is to a large degree a to additions, especially by surface runoff and by flow function of soil mineralogy, it also relates to soil nutrient through the soil. Persistence of excess water, especially in retention. Coarser-textured soils that are low in clay content the spring and after prolonged or heavy precipitation, tend to be more easily leached of nutrients than finer- hinders trafficability for many uses. Productivity of poorly textured soils. The fertility rating is an estimate of the soil drained soils is limited by a lack of aeration, susceptibility nutrient status based on the anticipated cumulative effects of to compaction, and lower soil temperature. Soil drainage these factors: classes are described below: Association Fertility Code Rapidly drained ®) - Water is removed from the soil rapidly in relation to supply. Soils are usually coarse- Acadie Siding very low vl textured, shallow, or both. Water source is Barrieau-Buctouche low l Belldune River medium m precipitation. Big Bald Mountain very low vl Boston Brook medium m Well drained (W) - Water is removed from the soil Caribou high h readily but not rapidly. Soils are generally intermediate Carleton high h in texture and depth. Water source is precipitation. Catamaran medium m Gagetown low l Moderately well drained (MW) - Water is removed Grand Falls low l from the soil somewhat slowly in relation to supply. Guimond River very low vl Soils are usually medium- to fine-textured. Holmesville medium m Interval high h Precipitation is the dominant water source in medium- Jacquet River low l to fine-textured soils; precipitation and significant Juniper low l additions by subsurface flow are necessary in coarse- Lavillette very low vl textured soils. Long Lake medium m Maliseet medium m Imperfectly drained (I) - Water is removed from the soil McGee medium m sufficiently slowly in relation to supply to keep the soil Muniac medium m wet for a significant part of the growing season. Nigadoo River medium m Precipitation, subsurface flow and groundwater act as Parleeville medium m Popple Depot low l a water source, alone or in combination. Soils have a Reece medium m wide range in texture and depth. Richibucto very low vl Riverbank low l Poorly drained (P) - Water is removed so slowly in Rogersville medium m relation to supply that the soil remains wet for a St. Quentin high h comparatively large part of the time the soil is not Stony Brook low l frozen. Subsurface flow or groundwater flow, or both, Sunbury low l in addition to precipitation, are the main water sources. Tetagouche medium m Soils have a wide range in texture and depth. Tetagouche Falls medium m Thibault high h Tracadie high h Very poorly drained (VP) - Water is removed from the Tuadook low l soil so slowly that the water table remains at or on the Violette medium m surface for the greater part of the time the soil is not frozen. Groundwater flow and subsurface flow are the major water sources. Soils have a wide range in texture and depth. 109

Flooding or inundation - Flooding occurs when water Class Phase Effect on % Surface Distance Cultivation Occupied Apart (m) levels rise above normal stream, river, and lake boundaries. Flooding interferes with time of planting, thus reducing an R0 non no sign. interference <2 >75 already short growing season. Erosion of unprotected bare R1 slightly slight interference 2-10 25-75 ground, and subsequent sediment loading of stream courses, R2 moderately tillage of inter-tilled 10-25 10-25 crops is impractical can also result. The following flooding classes are used: R3 very use of most machinery 25-50 2-10 is impractical None (N) - soils not subjected to flooding R4 exceedingly all use of machinery 50-90 <2 is impractical R5 excessively --- >90 --- Occasional (O) - soils subjected to flooding of short duration once every 3 years or more Slope or topography - Slope steepness is an indication of the landscape gradient. Important practical aspects of soil Frequent (F) - soils subjected to flooding of medium slope that impact on use and management include: rate and duration once every 2 years amount of runoff; erodibility of the soil; use of agricultural machinery; and uniformity of crop growth and maturity. Very frequent (VF) - soils subjected to prolonged flooding Although slope shape, length, and pattern also play an every year important role in slope effect, slope gradient is a convenient measure of slope impact on crop production and soil management. Slope classes are defined below: Stoniness - Stoniness refers to the percentage of the land surface occupied by coarse fragments of stone size (25 to Slope % 100 cm diameter). Plowing, harrowing, and seeding Class Slope equipment are significantly hindered by the presence of surface stones. Root crops, such as potatoes, are especially 1 0-0.5 sensitive to stoniness, in terms of potential tuber injury. 2 0.5-2 Alternately, stones are somewhat beneficial in terms of 3 2-5 improving the soil thermal regime and protecting soil 4 5-9 particles from being washed away. Classes of stoniness are 5 9-15 defined on the basis of the percentage of the land surface 6 15-30 occupied by stone fragments 25 to 100 cm in diameter: 7 30-45 8 45-70 Class Phase Effect on % Surface Distance 9 70-100 Cultivation Occupied Apart (m) Soil texture - Soil texture is an indication of the relative S0 non no hindrance <0.01 >30 S1 slightly slight hindrance 0.01-0.1 10-30 proportions of the various mineral soil particle size groups S2 moderately some interference 0.1-3 2-10 - sand (2 to 0.05 mm), silt (0.05 to 0.002 mm) and clay (less S3 very serious handicap 3-15 1-2 than 0.002 mm). Each of the textural soil classes has an S4 exceedingly cultivation prevented 15-50 0.1-1 established range for percentage sand, silt, and clay. Soil until stones cleared texture is one of the most permanent characteristics of a soil, S5 excessively too stony to permit >50 <0.1 and probably the most important. Size of the soil particles any cultivation affects most chemical, physical, and mineralogical reactions, and influences root growth for plants and engineering Boulderiness - Boulderiness refers to the percentage of the behaviour for machinery operation. Soil texture influences: land surface occupied by coarse fragments of boulder size capillarity (water holding capacity); soil erodibility (greater than 1 m diameter). It is defined with the same potential; cation exchange capacity and nutrient retention; class limits as stoniness. percolation; trafficability; and soil tilth. Subsoil texture impacts on subsoiling success. Coarser-textured soil Rockiness - Rockiness is an indication of the land surface materials are more prone to shattering when subsoiled dry. area that is occupied by bedrock exposures. Bedrock Soil texture class abbreviations are defined below: exposures interfere with tillage. Bedrock outcrops are incapable of supporting viable crops and result in fields with non-uniform crop growth and quality. Rockiness classes are defined below: 110

Typical % soils are found in New Brunswick.

Symbol Soil Texture Sand Silt Clay Class 2. Soils in this class have moderate limitations that restrict the range of crops or require moderate conservation c clay 28 22 50 practices. cl clay loam 32 35 33 l loam 41 41 18 Class 3. Soils in this class have moderately severe ls loamy sand 82 12 6 limitations that restrict the range of crops or require special s sand 93 3 4 conservation practices. Under good management these soils sc sandy clay 52 7 41 are fair to moderately high in productivity. scl sandy clay loam 61 11 28 si silt 9 86 5 Class 4. Soils in this class have severe limitations that sic silty clay 7 46 47 restrict the range of crops or require special conservation sicl silty clay loam 10 57 33 practices or both. The limitations may seriously affect such sil silt loam 23 64 13 farming practices as the timing and ease of tillage, planting sl sandy loam 65 25 10 and harvesting, and the application and maintenance of conservation practices.

Class 5. Soils in this class have very severe limitations that CANADA LAND INVENTORY CLASSIFICATION restrict their capability to producing perennial forage crops, but improvement practices are feasible. Some Class 5 soils The Canada Land Inventory program was designed to can be used for cultivated crops provided unusually provide a basis for land-use planning. Although some intensive management is used. regional modifications of its application were incorporated, the system is national in scope. It provides a relative Class 6. Soils in this class are capable only of producing ranking of the soil's or land's capability, in terms of a rating perennial forage crops, and improvement practices are not that is familiar and understood by many users. feasible. While these soils have some natural capability to sustain grazing, if not maintained, they rapidly revert back Soil capability classification for agriculture to forest. For this reason, no soils are classified as Class 6, but instead they have been classed as Class 7. In the Soil Capability Classification for Agriculture, mineral soils are grouped into seven classes according to their Class 7. Soils in this class have no capability for arable potential and limitations for agricultural use (Canada Land culture of common field crops or permanent pasture. Inventory 1965). The first three classes are considered capable of sustained production of common cultivated crops; the fourth is marginal for sustained arable culture; the Capability subclass fifth is capable of use only for improved pasture and hay; the The subclass groups soils with similar kinds of limitations sixth is capable of use for only unimproved natural grazing; and hazards. It provides information on the kind of conser- and the seventh class is for soils and land types (including vation problem or limitation. Subclass designations found rock outcrops and small bodies of water) considered within the survey area are: incapable of use for arable culture or permanent pasture. The system was designed for mineral soils only and so is not Adverse climate ©) denotes inadequate heat for optimal applicable to organic soils. growth, thus restricting the range of crops that can be grown. It is only used for Class 2 soils. The capability classification consists of two main categories: the capability class and the capability subclass. Undesirable soil structure and/or low permeability (D) is used for soils in which the depth of rooting zone is Capability class restricted by conditions other than a high water table or The class is the broadest category in this classification. It is consolidated bedrock. The restricting layer is usually a a grouping of subclasses that have the same relative degree compacted till material. Soil layers with bulk densities of limitation or hazard. The class indicates the general greater than 1.60 g/cm3 and/or permeabilities less than 1.0 suitability of the soils for agricultural use. The limitation or cm/hr are considered significantly restricting. hazard becomes progressively greater from Class 1 to Class 7. Low fertility (F) is used for soils having low fertility that either is correctable with careful management in the use of Class 1. Soils in this class have no significant limitations in fertilizers and soil amendments or is difficult to correct in a use for crops. Due to regional climate limitations feasible way. The limitation of soils in this subclass is (insufficient heat units and low natural fertility) no Class 1 usually due to a lack of available plant nutrients (low 111 nutrient holding capacity), high acidity and low exchange Class 1 greater than 7.7 m3 capacity. Class 2 6.3 to 7.7 m3 Class 3 4.9 to 6.3 m3 Inundation by streams, rivers, and lakes (I) includes soils Class 4 3.5 to 4.9 m3 subjected to flooding causing crop damage or restricting Class 5 2.1 to 3.5 m3 agricultural use. Class 6 0.7 to 2.1 m3 Class 7 less than 0.7 m3 Moisture limitation (M) denotes soils where crops are adversely affected by droughtiness owing to inherent soil characteristics. These soils have low water holding Capability subclass. capacities. As expressed by the principle of limiting factors, plant response is determined by the least optimum factor. Factors Stoniness (P) indicates soils sufficiently stony on the that limit tree growth are shown as subclasses. Knowing the surface to hinder tillage, planting, and harvesting operations. kind of limitation is important in determining the type of Stony soils are usually less productive than comparable non- forest management to be used. Silvicultural practices can be stony soils. used that overcome or minimize the detrimental effects of a given growth-limiting factor. The degree of limitation of the Consolidated bedrock ®) designates soils where the growth-limiting factor determines the class designation. presence of bedrock near the surface restricts their agricultural use. This includes soils that have bedrock The capability subclasses found within the survey area are: within 1 m of the surface and also considers the presence of bedrock exposures. climate U exposure, which, although significant in Topography (T) indicates soils where topography is a coastal regions, is not listed, as only soil limitation. Both the percent of slope and the pattern of limitations are considered frequency of slopes in different directions are important factors in increasing the cost of farming over that of smooth soil moisture ground, in decreasing the uniformity of growth and maturity M soil moisture deficiency of crops, and in increasing the hazard of water erosion. W excess soil moisture

Excess water (W) is used for soils where excess water other permeability and depth of rooting zone: than that brought about by inundation is a limitation to their D physical restriction to rooting caused by dense use for agriculture. Excess water may result from or consolidated layers, other than bedrock inadequate soil drainage, a high water table, seepage or R restriction of rooting zone by bedrock runoff from surrounding areas. other soil factors: F low fertility I soils periodically inundated by streams or Land capability classification for forestry lakes P stoniness which affects forest density or The Land Capability Classification for Forestry is based on growth the soil's ability to grow commercial timber (Canada Land Inventory 1967). Three categories are used in this system: Indicator species the capability class, the capability subclass, and the indicator Tree species that can be expected to yield the volume as- species. sociated with each class are shown as part of the symbol. They are indigenous coniferous species adapted to the Capability class. region and land: When assigning land to a given class, the environment of bs for black spruce subsoil, soil surface, local and regional climate, as well as or the characteristic tree species, are all taken into account. jp for jack pine. The capability class, then, is an expression of all the environmental factors as they apply to tree growth, i.e., it defines the degree of limitation to the growth of commercial forests. Associated with each capability class is a productivity range based on mean annual increment of the best species or group of species adapted to the site. Ex- pressed in cubic metres per hectare per annum, the classes are: Table 5. Selected interpretations of soil map units

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry AS 3 383 AS >2 120 VP vl N S0 B0 R0 0.25 n/a n/a O 7W AS + TU(b)6/u2 1 137 AS >2 120 VP vl N S0 B0 R0 1.25 n/a n/a O 7W BB(b)5 + RB(b)4/u2 1 253 BB 1-2 65 I l N S0 B0 R0 1.25 ls s/scl 3WF 4Fjp BB(b)4/l-u2 1 1270 BB 1-2 65 I l N S0 B0 R0 1.25 ls s/scl 3WF 4Fjp BB(b)5 + SB(b)6/u2 1 1384 BB 1-2 65 I l N S0 B0 R0 1.25 ls s/scl 3WF 4Fjp BB(b)4 + TC5/u2 1 7566 BB 1-2 65 I l N S0 B0 R0 1.25 ls s/scl 3WF 4Fjp BB4 + SB4/u2 1 2171 BB >2 65 I l N S0 B0 R0 1.25 ls s/scl 3WF 4Fjp BB(b)4/u2 2 2173 BB 1-2 65 I l N S0 B0 R0 1.25 ls s/scl 3WF 4Fjp BB(b)6 + SB(b)6/u2 + AS 1 14917 BB 1-2 65 P l N S0 B0 R0 1.25 ls s/scl 4W 5Wbs BB(b)6 + SB(b)6/u2 2 10073 BB 1-2 65 P l N S0 B0 R0 1.25 ls s/scl 4W 5Wbs BB(b)6 + RB5/u2 1 7453 BB 1-2 65 P l N S0 B0 R0 1.25 ls s/scl 4W 5Wbs BB(b)7/u2 2 542 BB 1-2 65 VP l N S0 B0 R0 1.25 ls s/scl 5W 6Wbs BB(b)3 + RB(v)1/u3 1 517 BB 1-2 65 W l N S0 B0 R0 3.5 ls s/scl 3MF 4FMjp BB(b)3 + SB(b)4/u2 1 3219 BB 1-2 65 W l N S0 B0 R0 1.25 ls s/scl 3MF 4FMjp BM(v)1/m4-6 R2 1 2427 BM <1 70 W vl N S2 B0 R2 17 sl ls 5TR 6RMFjp BM(v)1 + JU(v)1/y6 B2 1 1334 BM <1 70 W vl N S2 B2 R0 22.5 sl ls 5TRP 6MFjp BM(v)1 + JU(v)1/s6-7 R2 1 1955 BM <1 70 W vl N S2 B0 R2 30 sl ls 5TR 6RMFjp BM(v)1 + JU(b)1/y6 B2 1 1446 BM <1 70 W vl N S2 B2 R0 22.5 sl ls 5TRP 6MFjp BM(v)1 + JU(v)1/y6 2 659 BM <1 70 W vl N S2 B0 R0 22.5 sl ls 5TR 6MFjp BM(v)1 + JU(v)1 + JR(v)1/y7 R1 1 8859 BM <1 70 W vl N S2 B0 R1 37.5 sl ls 6T 6UMFjp BO(b)3 + HM(v)2/u3 1 1467 BO 1-2 100 W m N S3 B0 R0 3.5 l cl 3P 3Fbs BR4/u3 2 17634 BR >2 100 I m N S1 B0 R0 3.5 sl sl 3WF 3UFjp BR2 + TC6/u3 1 13138 BR >2 100 W m N S1 B0 R0 3.5 sl sl 3MF 3UFMjp BR3 + GG3/u3 1 593 BR >2 100 W m N S1 B0 R0 3.5 sl sl 3MF 3UFMjp CB(b)4 + CR(b)4/m5 1 2585 CB 1-2 100 I h N S2 B0 R0 12 sil cl 4T 3FWbs CB(b)4 + CR(b)4 + CB(v)2/m5 1 358 CB 1-2 100 I h N S2 B0 R0 12 sil cl 4T 3FWbs CB6 + BO6/u3 1 2009 CB >2 100 P h N S2 B0 R0 3.5 sil cl 4W 4Wbs CB(v)2/u3 1 2234 CB <1 100 W h N S2 B0 R0 3.5 sil cl 3R 3Fbs CB(v)2 + TH(v)1/s5-7 1 3673 CB <1 100 W h N S2 B0 R0 27 sil cl 5T 3Fbs CB(b)2/m4 1 30362 CB 1-2 100 W h N S2 B0 R0 7 sil cl 3T 3Fbs CB(v)1 + TH(v)1 + HM(b)2/s6 1 2763 CB <1 100 W h N S2 B0 R0 22.5 sil cl 5T 3Fbs CB(b)2 + TH(b)2/u3 1 4883 CB 1-2 100 W h N S2 B0 R0 3.5 sil cl 2C 3Fbs CB(v)2 + BO(v)2/y5 1 1945 CB <1 100 W h N S2 B0 R0 12 sil cl 4TR 3Fbs CB(v)2 + HM(b)2/m4 1 517 CB <1 100 W h N S2 B0 R0 7 sil cl 3TR 3Fbs CB(v)2 + TH(v)2 + CR(b)2/r5-4 1 7717 CB <1 100 W h N S2 B0 R0 10 sil cl 4TR 3Fbs CB(b)2 + TH(b)3/u3 1 465 CB 1-2 100 W h N S2 B0 R0 3.5 sil cl 2C 3Fbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry CB(v)1/s6 1 1608 CB <1 100 W h N S2 B0 R0 22.5 sil cl 5T 3Fbs CB(b)3 + CR(b)3/m5 1 6132 CB 1-2 100 W h N S2 B0 R0 12 sil cl 4T 3Fbs CR(b)5 + TH(b)4 + VO(b)5/u3 1 2986 CR 1-2 55 I h N S2 B0 R0 3.5 l l 4WD 3FDWbs CR(b)4 + TH(b)4/m5 1 1055 CR 1-2 55 I h N S2 B0 R0 12 l l 4T 3FDWbs CR(v)2 + TH(v)1/s8-9 R1 1 9431 CR <1 55 MW h N S2 B0 R1 72.5 l l 7T 5Rbs CR(v)2 + CB(v)2 + VO(v)2/y6 1 15839 CR <1 55 MW h N S2 B0 R0 22.5 l l 5T 3FDbs CR(v)2 + TH(v)1/s7 1 839 CR <1 55 MW h N S2 B0 R0 37.5 l l 6T 3FDbs CR(v)2 + CB(v)1 + TH(v)1/y7 R1 1 23114 CR <1 55 MW h N S2 B0 R1 37.5 l l 6T 4Rbs CR(v)2 + HM(v)1/y6 1 2449 CR <1 55 MW h N S2 B0 R0 22.5 l l 5T 3FDbs CR(b)2 + TH(b)2 + CT(b)2/m4 1 2025 CR 1-2 55 MW h N S2 B0 R0 7 l l 3T 3FDbs CR(v)2/m5-4 1 333 CR <1 55 MW h N S2 B0 R0 10 l l 4TR 3FDbs CR(v)2 + TH(v)1/y6-7 1 4648 CR <1 55 MW h N S2 B0 R0 30 l l 5T 3FDbs CR(b)2 + CB(b)1/m5-4 1 5570 CR 1-2 55 MW h N S2 B0 R0 10 l l 4T 3FDbs CR(b)2 + CB(b)2 + VO(b)2/m5-4 1 16370 CR 1-2 55 MW h N S2 B0 R0 10 l l 4T 3FDbs CR(v)2 + CB(b)2/m4 1 1024 CR <1 55 MW h N S2 B0 R0 7 l l 3TR 3FDbs CR(v)1 + VO(v)1/y6 1 2490 CR <1 55 W h N S2 B0 R0 22.5 l l 5T 3FDbs CR(b)3/m4 1 667 CR 1-2 55 W h N S2 B0 R0 7 l l 3T 3FDbs CR(v)1 + TH(v)1/s9 R1 1 1361 CR <1 55 W h N S2 B0 R1 85 l l 7T 5Rbs CR(b)3 + TH(b)2/m4 1 8555 CR 1-2 55 W h N S2 B0 R0 7 l l 3T 3FDbs CR(v)3/m4-5 1 3257 CR <1 55 W h N S2 B0 R0 10 l l 4TR 3FDbs CT(b)4/u3 4 7576 CT 1-2 50 I m N S3 B0 R0 3.5 l sl 4WD 4DWbs CT(b)4 + LL(b)4/u3 2 7421 CT 1-2 50 I m N S3 B0 R0 3.5 l sl 4WD 4DWbs CT5/u3 1 7769 CT >2 50 I m N S3 B0 R0 3.5 l sl 4WD 4DWbs CT(b)5 + RE(b)5/u3 2 9870 CT 1-2 50 I m N S3 B0 R0 3.5 l sl 4WD 4DWbs CT5 + JU5/u3 1 3683 CT >2 50 I m N S3 B0 R0 3.5 l sl 4WD 4DWbs CT(b)4 + RE(b)4/u3 1 1176 CT 1-2 50 I m N S3 B0 R0 3.5 l sl 4WD 4DWbs CT(b)4 + LL(b)4/i3-4 1 3718 CT 1-2 50 I m N S3 B0 R0 5.5 l sl 4WD 4DWbs CT6 + JU4/u3 1 448 CT >2 50 P m N S3 B0 R0 3.5 l sl 5WD 5WDbs CT(b)6 + LL(b)6/u3 1 2247 CT 1-2 50 P m N S3 B0 R0 3.5 l sl 5WD 5WDbs CT(v)6/u3 1 2094 CT <1 50 P m N S3 B0 R0 3.5 l sl 5WD 5WDbs CT(b)7 + LL(b)7/u3 + AS 1 1187 CT 1-2 50 VP m N S3 B0 R0 3.5 l sl 7W 6Wbs CT(b)2 + RE(b)2/u3 1 1999 CT 1-2 50 W m N S3 B0 R0 3.5 l sl 3DP 4DFbs CT(v)2/m4-5 1 4509 CT <1 50 W m N S3 B0 R0 10 l sl 4TR 4DFbs CT(b)2/m4 + JU3/h4 1 5032 CT 1-2 50 W m N S3 B0 R0 7 l sl 3TDP 4DFbs CT(v)1 + LL(v)1/s6 1 805 CT <1 50 W m N S3 B0 R0 22.5 l sl 5T 4DFbs CT(b)2 + JU(v)1/y7-8 R1 1 814 CT 1-2 50 W m N S3 B0 R1 50 l sl 6T 4RDFbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry CT(b)2 + JU(b)2/m5 1 1282 CT 1-2 50 W m N S3 B0 R0 12 l sl 4T 4DFbs CT(b)3/y5-6 1 3005 CT 1-2 50 W m N S3 B0 R0 19.5 l sl 5T 4DFbs CT(v)2 + LL(v)2/s5 1 904 CT <1 50 W m N S3 B0 R0 12 l sl 4TR 4DFbs CT(b)2 + LL(b)2/m4 3 47239 CT 1-2 50 W m N S3 B0 R0 7 l sl 3TDP 4DFbs CT(b)2/m4 1 124 CT 1-2 50 W m N S3 B0 R0 7 l sl 3TDP 4DFbs CT(b)2 + JU(b)2/m4 1 6484 CT 1-2 50 W m N S3 B0 R0 7 l sl 3TDP 4DFbs CT(b)2 + PD(b)2 + JR(v)3/m4 1 5935 CT 1-2 50 W m N S3 B0 R0 7 l sl 3TDP 4DFbs CT(b)3/m4 1 3828 CT 1-2 50 W m N S3 B0 R0 7 l sl 3TDP 4DFbs CT(b)3 + LL(b)3/s5-6 1 2463 CT 1-2 50 W m N S3 B0 R0 19.5 l sl 5T 4DFbs CT(b)2/m4-5 1 14661 CT 1-2 50 W m N S3 B0 R0 10 l sl 3TDP 4DFbs CT(v)2 + JU(v)1/s6 1 933 CT <1 50 W m N S3 B0 R0 22.5 l sl 5T 4DFbs CT(v)2 + LL(v)1/s6 R1 1 2319 CT <1 50 W m N S3 B0 R1 22.5 l sl 5T 4RDFbs GF5/u3 2 6392 GF >2 100 I l N SO B0 R0 3.5 sl ls 3WF 4Fjp GF3/t3-5 3 2374 GF >2 100 R l N SO B0 R0 8.5 sl ls 3TMF 5MFjp GF3/t3-5 + IN5/u2 1 200 GF >2 100 R l N SO B0 R0 8.5 sl ls 3TMF 5MFjp GF3/h4 2 6330 GF >2 100 R l N SO B0 R0 7 sl ls 3TMF 5MFjp GF3 + GG3/t3-5 1 3027 GF >2 100 R l N SO B0 R0 8.5 sl ls 3TMF 5MFjp GF3 + MA3/t3-5 1 510 GF >2 100 R l N SO B0 R0 8.5 sl ls 3TMF 5MFjp GF2/u3 1 306 GF >2 100 R l N SO B0 R0 3.5 sl ls 3TMF 5MFjp GF3/m4 1 1533 GF >2 100 R l N SO B0 R0 7 sl ls 3TMF 5MFjp GF3/t3 1 692 GF >2 100 R l N SO B0 R0 3.5 sl ls 3MF 5MFjp GG5 + RI5/u3 1 377 GG >2 100 I l N SO B0 R0 3.5 ls ls 3WF 4Fjp GG5 + GF5/u2 1 1782 GG >2 100 I l N SO B0 R0 1.25 ls ls 3WF 4Fjp GG5/u3 1 445 GG >2 100 I l N SO B0 R0 3.5 ls ls 3WF 4Fjp GG4 + MU4/u3 1 931 GG >2 100 I l N SO B0 R0 3.5 ls ls 3WF 4Fjp GG4 + GF4/t3-5 1 6820 GG >2 100 I l N SO B0 R0 8.5 ls ls 3WF 4Fjp GG6 + JU6/u3 1 1844 GG >2 100 P l N SO B0 R0 3.5 ls ls 5W 6Wbs GG1/h4 1 3055 GG >2 100 R l N SO B0 R0 7 ls ls 4MF 5MFjp GG3 + RI3/t2-4 1 9916 GG >2 100 R l N SO B0 R0 4.75 ls ls 4MF 5MFjp GG3 + RI3/t3 2 8204 GG >2 100 R l N SO B0 R0 3.5 ls ls 4MF 5MFjp GG3/t3-5 1 2644 GG >2 100 R l N SO B0 R0 8.5 ls ls 4MF 5MFjp GG1/u2 1 638 GG >2 100 R l N SO B0 R0 1.25 ls ls 4MF 5MFjp GG3/u3 1 695 GG >2 100 R l N SO B0 R0 3.5 ls ls 4MF 5MFjp GG3 + RI3/t3 + IN6/u2 1 3068 GG >2 100 R l N SO B0 R0 3.5 ls ls 4MF 5MFjp GG1/s8 1 257 GG >2 100 R l N SO B0 R0 57.5 ls ls 6T 5MFjp GG3 + JU3/u3 1 1408 GG >2 100 R l N SO B0 R0 3.5 ls ls 4MF 5MFjp Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry GG1/h6 1 420 GG >2 100 R l N SO B0 R0 22.5 ls ls 5T 5MFjp GG3 + JU3/t3-5 1 614 GG >2 100 R l N SO B0 R0 8.5 ls ls 4MF 5MFjp GG3/h3-5 1 1814 GG >2 100 R l N SO B0 R0 8.5 ls ls 4MF 5MFjp GM3/u3 1 1312 GM >2 100 R vl N SO B0 R0 3.5 ls ls 4MF 5MFjp GM(b)1 + BB(b)3/u2 1 524 GM 1-2 100 R vl N SO B0 R0 1.25 ls ls 4MF 5MFjp HM(v)4 + LL(v)4 + MG(b)2/u3 1 10067 HM <1 50 I m N S2 B0 R0 3.5 l l 4RWD 4RDWbs HM(b)5 + CR(b)5/u3 1 5413 HM 1-2 50 I m N S2 B0 R0 3.5 l l 4WD 4DWbs HM(b)5 + MG(b)4/u3 1 2860 HM 1-2 50 I m N S2 B0 R0 3.5 l l 4WD 4DWbs HM(b)6 + LL(b)6/u3 1 1529 HM 1-2 50 P m N S2 B0 R0 3.5 l l 5WD 5WDbs HM(b)3 + MG(b)3/m4 1 1460 HM 1-2 50 W m N S2 B0 R0 7 l l 3TD 4Dbs HM(b)2 + MG(v)1/m*6-7 1 1989 HM 1-2 50 W m N S2 B0 R0 30 l l 5T 4Dbs HM(b)2 + LL(b)2 + MG(v)1/m4 1 2315 HM 1-2 50 W m N S2 B0 R0 7 l l 3TD 4Dbs HM(v)2 + CR(v)2/m4 1 1549 HM <1 50 W m N S2 B0 R0 7 l l 3TRD 4Dbs HM(v)2 + MG(b)1/y5-6 1 3766 HM <1 50 W m N S2 B0 R0 19.5 l l 5T 4Dbs HM(v)1 + MG(v)1/y6-7 R1 1 5508 HM <1 50 W m N S2 B0 R1 30 l l 5TR 4RDbs HM(v)2 + MG(v)1/m6 R1 1 1963 HM <1 50 W m N S2 B0 R1 22.5 l l 5TR 4RDbs HM(b)2 + MG(b)2/m4 1 138 HM 1-2 50 W m N S2 B0 R0 7 l l 3TD 4Dbs IN4 + RI4/u2 1 3650 IN >2 100 I h F S0 B0 R0 1.25 sil sil 3IW 3FIbs IN4 + GF4/u2 1 2346 IN >2 100 I h F S0 B0 R0 1.25 sil sil 3IW 3FIbs JR5 + PD5/u2 1 2134 JR >2 100 I l N S3 B0 R0 1.25 l l 4P 4Fbs JR(b)6 + PD(b)6/u3 1 2104 JR 1-2 100 P l N S3 B0 R0 3.5 l l 4W 5WFbs JR(b)2 + TH(b)2 + TF(b)2/m*4-5 1 4517 JR 1-2 100 W l N S3 B0 R0 10 l l 4TP 4Fbs JR(v)1/y7 R1-2 1 327 JR <1 100 W l N S3 B0 R1-2 37.5 l l 6T 4RFbs JR2/h4-5 1 1692 JR >2 100 W l N S3 B0 R0 10 l l 4TP 4Fbs JR(b)3 + PD(v)2/h4 1 3098 JR 1-2 100 W l N S3 B0 R0 7 l l 4P 4Fbs JR(v)2 + MG(v)2/m4 1 4221 JR <1 100 W l N S3 B0 R0 7 l l 4RP 4Fbs JR(b)3 + MG(b)3/h4-6 1 7180 JR 1-2 100 W l N S3 B0 R0 17 l l 5T 4Fbs JR(v)1 + PD(v)2/s7 R2 1 2190 JR <1 100 W l N S3 B0 R2 37.5 l l 6T 5RFbs JR(v)1 + CT(v)2/y9 R3 2 556 JR <1 100 W l N S3 B0 R3 85 l l 7T 6RFbs JR(v)1 + PD(v)2/y6 R1 1 7436 JR <1 100 W l N S3 B0 R1 22.5 l l 5TR 4Fbs JR(v)1/r5-6 1 1161 JR <1 100 W l N S3 B0 R0 19.5 l l 5T 4Fbs JU5/h4 B1 1 29934 JU >2 100 I l N S3 B1 R0 7 sl sl 5P 4Fbs JU5 + GG5/h4 B2 1 6745 JU >2 100 I l N S3 B2 R0 7 sl sl 5P 5PFbs JU5 + JR5/h4 1 2199 JU >2 100 I l N S3 B0 R0 7 sl sl 4P 4Fbs JU(b)5/u3 B2 1 4906 JU 1-2 100 I l N S3 B2 R0 3.5 sl sl 5P 5PFbs JU(b)5/u3 1 836 JU 1-2 100 I l N S3 B0 R0 3.5 sl sl 4P 4Fbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry JU5/u3 B2 1 4689 JU >2 100 I l N S3 B2 R0 3.5 sl sl 5P 5PFbs JU5 + TU5/u3 2 13762 JU >2 100 I l N S3 B0 R0 3.5 sl sl 4P 4Fbs JU5/u3 1 3207 JU >2 100 I l N S3 B0 R0 3.5 sl sl 4P 4Fbs JU(b)4/m4 1 1138 JU 1-2 100 I l N S3 B0 R0 7 sl sl 4P 4Fbs JU4 + GG4/h4 1 13594 JU >2 100 I l N S3 B0 R0 7 sl sl 4P 4Fbs JU5/h4 2 4680 JU >2 100 I l N S3 B0 R0 7 sl sl 4P 4Fbs JU5/h4 B5 1 3309 JU >2 100 I l N S3 B5 R0 7 sl sl 7P 6Pjp JU5 + CT5/u3 1 938 JU >2 100 I l N S3 B0 R0 3.5 sl sl 4P 4Fbs JU5/h4 B2 1 4467 JU >2 100 I l N S3 B2 R0 7 sl sl 5P 5PFbs JU(b)6/h4 1 1268 JU 1-2 100 P l N S3 B0 R0 7 sl sl 5W 6Wbs JU6/u2-3 + AS 1 1718 JU >2 100 P l N S3 B0 R0 2.75 sl sl 5W 6Wbs JU6 + GG5/u3 1 1281 JU >2 100 P l N S3 B0 R0 3.5 sl sl 5W 6Wbs JU(v)1/y6 1 189 JU <1 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(v)1/y8 R2 2 1319 JU <1 100 W l N S3 B0 R2 57.5 sl sl 6T 5RFjp JU(v)1 + BM(v)1 + TU(b)2/y8 R2 1 974 JU <1 100 W l N S3 B0 R2 57.5 sl sl 6T 5RFjp JU(v)1 + BM(v)1 + TU(b)2/s7 1 1427 JU <1 100 W l N S3 B0 R0 37.5 sl sl 6T 4Fjp JU(v)2 + BM(v)1/m4 1 374 JU <1 100 W l N S3 B0 R0 7 sl sl 4RP 4Fjp JU(v)1 + TU(b)2/y6 R1 1 546 JU <1 100 W l N S3 B0 R1 22.5 sl sl 5TR 4RFjp JU3/h4 1 4483 JU >2 100 W l N S3 B0 R0 7 sl sl 4P 4Fjp JU(v)1 + JR(v)1/y7 R1 1 2491 JU <1 100 W l N S3 B0 R1 37.5 sl sl 6T 4Fjp JU(b)1 + BM(v)1/m5-6 B2 1 1609 JU 1-2 100 W l N S3 B2 R0 19.5 sl sl 5TP 5PFjp JU(b)2/m5-4 1 9465 JU 1-2 100 W l N S3 B0 R0 10 sl sl 4TP 4Fjp JU3 + TF3/h5 1 360 JU >2 100 W l N S3 B0 R0 12 sl sl 4TP 4Fjp JU(v)3 + CT(b)2/s6 1 3899 JU <1 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(v)1 + TU(v)2/y5-6 B2 1 16784 JU <1 100 W l N S3 B2 R0 19.5 sl sl 5TRP 5PFjp JU(b)1 + BM(v)1/y5 1 3370 JU 1-2 100 W l N S3 B0 R0 12 sl sl 4TP 4Fjp JU(b)2/m4 2 1531 JU 1-2 100 W l N S3 B0 R0 7 sl sl 4P 4Fjp JU(v)1/y5-6 1 7350 JU <1 100 W l N S3 B0 R0 19.5 sl sl 5T 4Fjp JU(b)3/m5 B2 1 3482 JU 1-2 100 W l N S3 B2 R0 12 sl sl 5P 5PFjp JU(v)1 + BM(v)1 + TU(b)2/y6 1 7299 JU <1 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(b)2/m6 1 1187 JU 1-2 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(b)2/m4-5 1 3061 JU 1-2 100 W l N S3 B0 R0 10 sl sl 4TP 4Fjp JU(v)1 + TU(v)2/y5-7 1 4808 JU <1 100 W l N S3 B0 R0 27 sl sl 5T 4Fjp JU(v)2 + TU(b)2/m4 1 3866 JU <1 100 W l N S3 B0 R0 7 sl sl 4RP 4Fjp JU(b)3/m3-4 1 225 JU 1-2 100 W l N S3 B0 R0 5.5 sl sl 4P 4Fjp JU(v)2 + MG(v)2 + TU(b)4/m4 1 1699 JU <1 100 W l N S3 B0 R0 7 sl sl 4RP 4Fjp Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry JU(v)1 + MG(v)1/y6 1 1773 JU <1 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(v)1/y7 R3 1 244 JU <1 100 W l N S3 B0 R3 37.5 sl sl 6TR 6RFjp JU(v)1 + CT(v)2/y6 1 3662 JU <1 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(b)1/m6 1 857 JU 1-2 100 W l N S3 B0 R0 22.5 sl sl 5T 4Fjp JU(v)1 + MG(v)1 + LL(b)2/y8 R1 1 4697 JU <1 100 W l N S3 B0 R1 57.5 sl sl 6T 5RFjp JU(b)1 + TU(b)2/y5-6 1 24240 JU 1-2 100 W l N S3 B0 R0 19.5 sl sl 5T 4Fjp JU2/m5 1 253 JU >2 100 W l N S3 B0 R0 12 sl sl 4TP 4Fjp JU(v)2/m4 1 182 JU <1 100 W l N S3 B0 R0 7 sl sl 4RP 4Fjp JU(b)3 + TU(b)3/u3 1 902 JU 1-2 100 W l N S3 B0 R0 3.5 sl sl 4P 4Fjp JU(v)1/y6-7 1 9673 JU <1 100 W l N S3 B0 R0 30 sl sl 5T 4Fjp LL(b)4 + MG(v)4/u3 2 9363 LL 1-2 50 I m N S3 B0 R0 3.5 l l 4WDP 4DWbs LL(b)4 + RE(b)4/m4 1 2487 LL 1-2 50 I m N S3 B0 R0 7 l l 4WDP 4DWbs LL(b)4 + CT(b)4 + MG(b)3/m4 1 3215 LL 1-2 50 I m N S3 B0 R0 7 l l 4WDP 4DWbs LL(b)4 + CT(b)3/m4 1 13580 LL 1-2 50 I m N S3 B0 R0 7 l l 4WDP 4DWbs LL(b)5/u2-3 1 4511 LL 1-2 50 I m N S3 B0 R0 2.75 l l 4WDP 4DWbs LL(b)4 + TT(b)4 + MG(b)3/m3-4 1 13183 LL 1-2 50 I m N S3 B0 R0 5.5 l l 4WDP 4DWbs LL(b)4 + RE(b)4/u3 3 5423 LL 1-2 50 I m N S3 B0 R0 3.5 l l 4WDP 4DWbs LL(b)4 + NR(b)4 + PD(b)4/u3 1 12426 LL 1-2 50 I m N S3 B0 R0 3.5 l l 4WDP 4DWbs LL(v)4/u3 1 765 LL <1 50 I m N S3 B0 R0 3.5 l l 4RPWD 4DWbs LL(b)5 + MG(b)4 + HM(b)5/u3 1 12721 LL 1-2 50 I m N S3 B0 R0 3.5 l l 4WDP 4DWbs LL(b)5 + MG(b)4/u3 1 516 LL 1-2 50 I m N S3 B0 R0 3.5 l l 4WDP 4DWbs LL(b)6 + VO(b)6 + MG(b)5/u3 1 29080 LL 1-2 50 P m N S3 B0 R0 3.5 l l 5WD 5WDbs LL(b)6 + PD(b)6/r-u3 1 12698 LL 1-2 50 P m N S3 B0 R0 3.5 l l 5WD 5WDbs LL(b)6 + MG(b)5/u2 1 824 LL 1-2 50 P m N S3 B0 R0 1.25 l l 5WD 5WDbs LL(b)6 + RE(b)6/u2 2 29592 LL 1-2 50 P m N S3 B0 R0 1.25 l l 5WD 5WDbs LL6 + MG5/u2-3 1 4151 LL >2 50 P m N S3 B0 R0 2.75 l l 5WD 5WDbs LL(b)2 + MG(v)1/s5-4 1 3475 LL 1-2 50 W m N S3 B0 R0 10 l l 4TP 4Dbs LL(b)2 + MG(v)1 + JU(v)1/y7 R1-2 1 5546 LL 1-2 50 W m N S3 B0 R1-2 37.5 l l 6T 4RDbs LL(b)3 + MG(b)3 + JU(b)3/u3 1 1290 LL 1-2 50 W m N S3 B0 R0 3.5 l l 4P 4Dbs LL(v)1 + HM(v)2/s6 R1 1 1377 LL <1 50 W m N S3 B0 R1 22.5 l l 5TR 4RDbs LL(v)1 + JU(v)1/y6-7 R1 1 576 LL <1 50 W m N S3 B0 R1 30 l l 5TR 4RDbs LL3 + JR3/h4-5 1 4770 LL >2 50 W m N S3 B0 R0 10 l l 4TP 4Dbs LL(v)2 + MG(v)2/r4 1 2940 LL <1 50 W m N S3 B0 R0 7 l l 4RP 4Dbs LL(b)3 + MG(b)3/m4-6 1 8745 LL 1-2 50 W m N S3 B0 R0 17 l l 4TP 4Dbs LL(b)2 + RE(b)2/u3 1 4014 LL 1-2 50 W m N S3 B0 R0 3.5 l l 4P 4Dbs LL(v)2 + MG(v)1/y6 R1 1 3709 LL <1 50 W m N S3 B0 R1 22.5 l l 5TR 4RDbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry LL(b)2 + MG(b)3/u3-4 2 25369 LL 1-2 50 W m N S3 B0 R0 5.5 l l 4P 4Dbs LL(v)1 + MG(v)1/m5-6 1 3818 LL <1 50 W m N S3 B0 R0 19.5 l l 5T 4Dbs LL(v)2 + PD(v)2/s7-6 R1 1 278 LL <1 50 W m N S3 B0 R1 30 l l 5TR 4RDbs LL(b)3/m4 1 4190 LL 1-2 50 W m N S3 B0 R0 7 l l 4P 4Dbs LL(v)2 + PD(v)2 + JR(v)1/y6 1 8402 LL <1 50 W m N S3 B0 R0 22.5 l l 5T 4Dbs LL(v)2 + MG(b)2/m5 1 1627 LL <1 50 W m N S3 B0 R0 12 l l 4TRP 4Dbs LL(v)2 + MG(v)1/y6-7 R1 1 9974 LL <1 50 W m N S3 B0 R1 30 l l 5TR 4RDbs LL(v)2 + MG(v)2/m4 1 3358 LL <1 50 W m N S3 B0 R0 7 l l 4RP 4Dbs LL(b)3 + RE(b)3/u3 1 509 LL 1-2 50 W m N S3 B0 R0 3.5 l l 4P 4Dbs LL(b)2 + MG(v)2/m4 2 11280 LL 1-2 50 W m N S3 B0 R0 7 l l 4P 4Dbs LL(b)2 + MG(b)2/m4 1 2294 LL 1-2 50 W m N S3 B0 R0 7 l l 4P 4Dbs LL(b)2 + TU(b)2/m4 1 10211 LL 1-2 50 W m N S3 B0 R0 7 l l 4P 4Dbs LL(b)2/m4 1 1825 LL 1-2 50 W m N S3 B0 R0 7 l l 4P 4Dbs LL(b)2 + MG(v)2/s5 1 1279 LL 1-2 50 W m N S3 B0 R0 12 l l 4TP 4Dbs LV + RE(b)7/l2 5 745 LV >2 160 VP vl N S0 B0 R0 1.25 n/a n/a O 7W LV + TC7/l1 1 216 LV >2 160 VP vl N S0 B0 R0 0.25 n/a n/a O 7W LV + SB(b)7/l2 1 92 LV >2 160 VP vl N S0 B0 R0 1.25 n/a n/a O 7W LV + RE(b)6/u2 1 4523 LV >2 160 VP vl N S0 B0 R0 1.25 n/a n/a O 7W LV 54 21502 LV >2 160 VP vl N S0 B0 R0 0.25 n/a n/a O 7W LV + BB7/l1 1 223 LV >2 160 VP vl N S0 B0 R0 0.25 n/a n/a O 7W LV + AS + RB(b)7/l1 1 324 LV >2 160 VP vl N S0 B0 R0 0.25 n/a n/a O 7W LV + RB(b)7/l1 2 198 LV >2 160 VP vl N S0 B0 R0 0.25 n/a n/a O 7W LV + RS(b)7/l2 1 88 LV >2 160 VP vl N S0 B0 R0 1.25 n/a n/a O 7W MA5/u3 1 907 MA >2 100 I m N S0 B0 R0 3.5 sil fsl 3W 3Fjp MA3 + GF3/u3 1 1236 MA >2 100 R m N S0 B0 R0 3.5 sil fsl 2C 3FMjp MA3 + GF3/t3-5 1 1222 MA >2 100 R m N S0 B0 R0 8.5 sil fsl 3T 3FMjp MG(v)4 + LL(b)4/u*3 1 4601 MG <1 100 I m N S3 B0 R0 3.5 l sl 4RP 4Fbs MG(b)4 + LL(b)4/m4 1 299 MG 1-2 100 I m N S3 B0 R0 7 l sl 4P 4Fbs MG(b)5 + LL(b)5/u3 1 321 MG 1-2 100 I m N S3 B0 R0 3.5 l sl 4P 4Fbs MG(v)2/m5-6 1 8468 MG <1 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(v)1 + LL(b)2/r6-7 1 2987 MG <1 100 W m N S3 B0 R0 30 l sl 5T 4Fbs MG(v)1 + JR(v)1 + HM(b)2/y-s5-6 R11 10752 MG <1 100 W m N S3 B0 R1 19.5 l sl 5TR 4RFbs MG(v)1 + HM(v)2/m6 R1 1 1941 MG <1 100 W m N S3 B0 R1 22.5 l sl 5TR 4RFbs MG(v)1 + TH(v)1/s6-8 R1 1 895 MG <1 100 W m N S3 B0 R1 42.5 l sl 6T 4RFbs MG(v)1/y6-5 1 2413 MG <1 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(v)1 + JR(v)1/s7-6 R1 1 8155 MG <1 100 W m N S3 B0 R1 30 l sl 5TR 4RFbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry MG(v)1 + TH(v)1/s6 1 1869 MG <1 100 W m N S3 B0 R0 22.5 l sl 5T 4Fbs MG(v)1 + TH(b)2/s8-9 R2 1 1341 MG <1 100 W m N S3 B0 R2 72.5 l sl 7T 5Rbs MG(v)1/s8-9 R2 1 10436 MG <1 100 W m N S3 B0 R2 72.5 l sl 7T 5Rbs MG(v)1 + HM(b)2/m*6 2 15682 MG <1 100 W m N S3 B0 R0 22.5 l sl 5T 4Fbs MG(v)1/s9 R2 1 2614 MG <1 100 W m N S3 B0 R2 85 l sl 7T 5Rbs MG(v)2 + LL(b)2/m4 1 19131 MG <1 100 W m N S3 B0 R0 7 l sl 4RP 4Fbs MG(v)2 + LL(b)2/m-y5-6 1 19152 MG <1 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(b)3 + CT(b)3/m4 1 2479 MG 1-2 100 W m N S3 B0 R0 7 l sl 4P 4Fbs MG(v)1 + HM(b)3/m5-6 1 3075 MG <1 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(v)1 + LL(v)2/y6 R2 1 4423 MG <1 100 W m N S3 B0 R2 22.5 l sl 5TR 5Rbs MG(v)2 + HM(b)2 + CR(b)2/m5 1 22106 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(v)3 + LL(b)3/m-r4 1 6328 MG <1 100 W m N S3 B0 R0 7 l sl 4RP 4Fbs MG(v)2 + LL(v)3 + HM(v)3/m5-6 1 3347 MG <1 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(v)1 + HM(v)2/s8-9 R2 1 840 MG <1 100 W m N S3 B0 R2 72.5 l sl 7T 5Rbs MG(b)3 + LL(v)2 + CT(v)2/m5 1 11933 MG 1-2 100 W m N S3 B0 R0 12 l sl 4TP 4Fbs MG(v)2/m5 1 4149 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(v)1 + HM(b)2/y5 1 18655 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(v)2 + LL(v)2/s5 1 2879 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(v)2 + JR(v)2/m4-6 1 4247 MG <1 100 W m N S3 B0 R0 17 l sl 5T 4Fbs MG(v)1 + JR(v)1/y8-9 R3 4 3487 MG <1 100 W m N S3 B0 R3 72.5 l sl 7T 6Rbs MG(v)1 + TH(v)1/m5 1 4874 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(v)1 + TF(v)1/y6 1 559 MG <1 100 W m N S3 B0 R0 22.5 l sl 5T 4Fbs MG(b)2 + TH(b)2/m-y5 1 11882 MG 1-2 100 W m N S3 B0 R0 12 l sl 4TP 4Fbs MG(b)1 + TH(b)1/m*5 1 54 MG 1-2 100 W m N S3 B0 R0 12 l sl 4TP 4Fbs MG(v)1 + JR(v)2/s6 R1 1 7253 MG <1 100 W m N S3 B0 R1 22.5 l sl 5TR 4RFbs MG(v)1 + HM(b)2/r6-7 1 4491 MG <1 100 W m N S3 B0 R0 30 l sl 5T 4Fbs MG(v)1/y7 R1-2 1 12043 MG <1 100 W m N S3 B0 R1-2 37.5 l sl 6T 4RFbs MG(v)1/s8 R2 1 1151 MG <1 100 W m N S3 B0 R2 57.5 l sl 6T 5Rbs MG(v)1 + LL(v)2/m5 1 3608 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(b)1 + HM(b)2/y5-6 1 2416 MG 1-2 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(v)1 + HM(b)2/y6 1 4491 MG <1 100 W m N S3 B0 R0 22.5 l sl 5T 4Fbs MG(v)2/s5-6 1 1017 MG <1 100 W m N S3 B0 R0 19.5 l sl 5T 4Fbs MG(v)1/y-r*6-7 R1 1 43236 MG <1 100 W m N S3 B0 R1 30 l sl 5TR 4RFbs MG(v)1/m5 2 3099 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(v)1/r*7 R2 1 16410 MG <1 100 W m N S3 B0 R2 37.5 l sl 6T 5Rbs MG(b)2 + TH(b)2/m5-4 1 11961 MG 1-2 100 W m N S3 B0 R0 10 l sl 4TP 4Fbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry MG(v)1 + TH(v)1/m*6 1 2386 MG <1 100 W m N S3 B0 R0 22.5 l sl 5T 4Fbs MG(v)1 + JU(v)1/s6-8 R1 1 4471 MG <1 100 W m N S3 B0 R1 42.5 l sl 6T 4RFbs MG3/h5 1 1202 MG >2 100 W m N S3 B0 R0 12 l sl 4TP 4Fbs MG(v)1/s6-8 R1 1 1689 MG <1 100 W m N S3 B0 R1 42.5 l sl 6T 4RFbs MG(b)1 + TH(b)2/m*5 1 11621 MG 1-2 100 W m N S3 B0 R0 12 l sl 4TP 4Fbs MG(b)2 + HM(b)2/m4 1 1707 MG 1-2 100 W m N S3 B0 R0 7 l sl 4P 4Fbs MG(v)1/y-r*7 R1-2 1 33160 MG <1 100 W m N S3 B0 R1-2 37.5 l sl 6T 4RFbs MG(b)2 + TH(b)2/m4-5 1 759 MG 1-2 100 W m N S3 B0 R0 10 l sl 4TP 4Fbs MG(v)3 + LL(b)4 + JU(v)3/y5 1 6197 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(b)1 + LL(b)2 + CT(b)2/s5 1 4112 MG 1-2 100 W m N S3 B0 R0 12 l sl 4TP 4Fbs MG(v)1 + TT(b)2 + PD(v)1/y5 1 14872 MG <1 100 W m N S3 B0 R0 12 l sl 4TRP 4Fbs MG(b)2 + HM(b)2 + TH(b)2/m4-5 1 28432 MG 1-2 100 W m N S3 B0 R0 10 l sl 4TP 4Fbs MG(v)1 + TH(v)1/s7-8 R1 1 5968 MG <1 100 W m N S3 B0 R1 50 l sl 6T 5RFbs MG(v)1/s7-8 R1 2 2556 MG <1 100 W m N S3 B0 R1 50 l sl 6T 5RFbs MG(b)2 + TH(b)2 + HM(b)2/m4-5 1 18762 MG 1-2 100 W m N S3 B0 R0 10 l sl 4TP 4Fbs MG(b)2 + HM(v)3/m4-5 1 2993 MG 1-2 100 W m N S3 B0 R0 10 l sl 4TP 4Fbs MU4 + MA4/t3-5 1 1835 MU >2 100 I m N S0 B0 R0 8.5 sl ls 3TWF 3Fbs MU2 + GG4/u3 1 483 MU >2 100 R m N S0 B0 R0 3.5 sl ls 3MF 4Mjp MU2/u3 1 548 MU >2 100 R m N S0 B0 R0 3.5 sl ls 3MF 4Mjp NR(b)4 + PD(b)4 + LL(b)4/m4 1 2741 NR 1-2 45 I m N S3 B0 R0 7 l sl 4WD 4DWbs NR(v)4 + TT(v)4/m4 1 5104 NR <1 45 I m N S3 B0 R0 7 l sl 4RWD 4DWbs NR(b)5/m4 1 1123 NR 1-2 45 I m N S3 B0 R0 7 l sl 4WD 4DWbs NR(v)2/h6 1 1643 NR <1 45 W m N S3 B0 R0 22.5 l sl 5T 4Dbs NR(b)3/u3 1 1953 NR 1-2 45 W m N S3 B0 R0 3.5 l sl 3D 4Dbs NR(v)2 + PD(v)2/y6-7 1 3319 NR <1 45 W m N S3 B0 R0 30 l sl 5T 4Dbs NR(v)3/m3 + PD(b)3/m4 + TF3/h4-5 1 12446 NR <1 45 W m N S3 B0 R0 3.5 l sl 3RPD 4Dbs NR(v)1 + TF(v)1/r5-7 R1 1 9131 NR <1 45 W m N S3 B0 R1 27 l sl 5TR 4Dbs NR(v)2/s5 1 154 NR <1 45 W m N S3 B0 R0 12 l sl 4TR 4Dbs PA(b)4/u3 1 2702 PA 1-2 100 I m N S2 B0 R0 3.5 l sl 3W 3Fbs PA4/u3 1 3102 PA >2 100 I m N S2 B0 R0 3.5 l sl 3W 3Fbs PA(v)2/m4 1 1358 PA <1 100 W m N S2 B0 R0 7 l sl 3TR 3Fbs PA(v)1/m5-6 1 2885 PA <1 100 W m N S2 B0 R0 19.5 l sl 5T 3Fbs PA(v-b)2/m4-5 1 6752 PA <1 100 W m N S2 B0 R0 10 l sl 4TR 3Fbs PD(v)4/m4 R1 1 12895 PD <1 45 I l N S3 B0 R1 7 l sl 4RWDP 4RDWbs PD(b)5 + LL(b)5/u3 1 1885 PD 1-2 45 I l N S3 B0 R0 3.5 l sl 4WDP 4DWbs PD(b)6 + JR(b)5/u3 1 922 PD 1-2 45 P l N S3 B0 R0 3.5 l sl 5WD 5WDbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry PD(b)6 + LL(b)5/u2 1 2913 PD 1-2 45 P l N S3 B0 R0 1.25 l sl 5WD 5WDbs PD(v)2 + LL(v)2 + MG(b)5/u3 1 16178 PD <1 45 W l N S3 B0 R0 3.5 l sl 4P 4DFbs PD(v)2/m5-4 1 272 PD <1 45 W l N S3 B0 R0 10 l sl 4TRP 4DFbs PD(v)2 + LL(v)1/s8 R1 1 4054 PD <1 45 W l N S3 B0 R1 57.5 l sl 6T 5RDFbs PD(v)3 + LL(v)3/m4 1 12949 PD <1 45 W l N S3 B0 R0 7 l sl 4RP 4DFbs PD(b)2 + LL(b)2/u3 1 8444 PD 1-2 45 W l N S3 B0 R0 3.5 l sl 4P 4DFbs PD(b)3 + LL(b)3/u3 1 1947 PD 1-2 45 W l N S3 B0 R0 3.5 l sl 4P 4DFbs PD(b)2/u3 1 3383 PD 1-2 45 W l N S3 B0 R0 3.5 l sl 4P 4DFbs PD(b)2 + NR(b)2/m4-5 1 8752 PD 1-2 45 W l N S3 B0 R0 10 l sl 4TP 4DFbs PD(v)1 + JR(v)1/y6-5 R2 1 18767 PD <1 45 W l N S3 B0 R2 19.5 l sl 5TR 5Rbs PD(v)3 + TF(v)3/m4-5 1 27320 PD <1 45 W l N S3 B0 R0 10 l sl 4TRP 4DFbs PD(v)2 + JR(v)2/y5 1 14030 PD <1 45 W l N S3 B0 R0 12 l sl 4TRP 4DFbs PD(v)2 + JR(v)1/y5-6 1 26286 PD <1 45 W l N S3 B0 R0 19.5 l sl 5T 4DFbs PD(b)2 + TF(b)1/y6 R1 1 4653 PD 1-2 45 W l N S3 B0 R1 22.5 l sl 5TR 4RDFbs PD(v)2 + JR(v)1/s7 R2 1 2538 PD <1 45 W l N S3 B0 R2 37.5 l sl 6T 5Rbs RB(v)5/u2 1 5321 RB <1 100 I vl N S0 B0 R0 1.25 ls ls 3RWF 4Fjp RB(v)4/u2 6 14412 RB <1 100 I vl N S0 B0 R0 1.25 ls ls 3RWF 4Fjp RB(v)4/l-u2 1 810 RB <1 100 I vl N S0 B0 R0 1.25 ls ls 3RWF 4Fjp RB(v)4 + BB(b)5/u2 1 1599 RB <1 100 I vl N S0 B0 R0 1.25 ls ls 3RWF 4Fjp RB(b-v)3/l2 + AS 4 14136 RB 1-2 100 R vl N S0 B0 R0 1.25 ls ls 3MF 4FMjp RB3 + TC6/u2 1 7667 RB >2 100 R vl N S0 B0 R0 1.25 ls ls 3MF 4FMjp RB3 + GM3/u3 1 1633 RB >2 100 R vl N S0 B0 R0 3.5 ls ls 3MF 4FMjp RB(v)2/u2 6 7933 RB <1 100 R vl N S0 B0 R0 1.25 ls ls 3RMF 4FMjp RB(v)1 + BB(b)4 + SB(b)4/u3 1 2292 RB <1 100 R vl N S0 B0 R0 3.5 ls ls 3RMF 4FMjp RB(v)1/u3 1 237 RB <1 100 R vl N S0 B0 R0 3.5 ls ls 3RMF 4FMjp RB2 + BB3/u3 1 1246 RB >2 100 R vl N S0 B0 R0 3.5 ls ls 3MF 4FMjp RB(v)1/u2 1 548 RB <1 100 R vl N S0 B0 R0 1.25 ls ls 3RMF 4FMjp RB(v)3/l2 1 2092 RB <1 100 R vl N S0 B0 R0 1.25 ls ls 3RMF 4FMjp RB(v)3/l2 + AS 1 291 RB <1 100 R vl N S0 B0 R0 1.25 ls ls 3RMF 4FMjp RB(v)1 + BB(b)4/u3 1 415 RB <1 100 R vl N S0 B0 R0 3.5 ls ls 3RMF 4FMjp RB(b)2 + BB(b)4/u2 1 4520 RB 1-2 100 R vl N S0 B0 R0 1.25 ls ls 3MF 4FMjp RB(v)2 + BB(b)3/u2 1 3156 RB <1 100 R vl N S0 B0 R0 1.25 ls ls 3RMF 4FMjp RE(b)5/u3 2 8176 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(b)4 + SN(b)3/u3 2 34795 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(b)4 + SN(b)4/u2-3 1 12428 RE 1-2 50 I m N S2 B0 R0 2.75 sl l 4WD 4DWbs RE(b)4/u2 1 3406 RE 1-2 50 I m N S2 B0 R0 1.25 sl l 4WD 4DWbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry RE(b)4/u3 6 19642 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(b)5 + SN(b)4/u3 1 1060 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(b)5/u2-3 1 13072 RE 1-2 50 I m N S2 B0 R0 2.75 sl l 4WD 4DWbs RE(b)4 + SN(b)2/u3 1 1552 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(v)4/u3-4 1 6566 RE <1 50 I m N S2 B0 R0 5.5 sl l 4RWD 4DWbs RE(v)4 + SN(v)2/u3 3 11834 RE <1 50 I m N S2 B0 R0 3.5 sl l 4RWD 4DWbs RE(b)5 + SN(b)4/u2-3 1 3905 RE 1-2 50 I m N S2 B0 R0 2.75 sl l 4WD 4DWbs RE(b)4 + SN(v)3/u3 1 7123 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(b)4 + SN(b)2/m4-3 1 13955 RE 1-2 50 I m N S2 B0 R0 5.5 sl l 4WD 4DWbs RE(b)5/u2 2 184 RE 1-2 50 I m N S2 B0 R0 1.25 sl l 4WD 4DWbs RE(b)4 + SN(b)4/u3 1 1458 RE 1-2 50 I m N S2 B0 R0 3.5 sl l 4WD 4DWbs RE(v)4 + SN(v)2/m4-3 1 3716 RE <1 50 I m N S2 B0 R0 5.5 sl l 4RWD 4DWbs RE(b)4/u2-3 2 2062 RE 1-2 50 I m N S2 B0 R0 2.75 sl l 4WD 4DWbs RE(b)6/u2-3 1 7377 RE 1-2 50 P m N S2 B0 R0 2.75 sl l 5WD 5WDbs RE(b)6/u2 3 11487 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)6 + SB(b)6/u2 + AS 1 35936 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)6/u2 + AS 7 41075 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)6 + SN(b)5/u2 + LV 1 4439 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)6 + SN(b)5/u3-2 1 10430 RE 1-2 50 P m N S2 B0 R0 2.75 sl l 5WD 5WDbs RE(b)6 + LL(b)6/u2 + GG5/h3-4 1 6851 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)6 + LL(b)6/u3 1 14185 RE 1-2 50 P m N S2 B0 R0 3.5 sl l 5WD 5WDbs RE(b)6 + SN(b)5/u2 2 2969 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)6 + SN(b)5/u2 + AS 5 16226 RE 1-2 50 P m N S2 B0 R0 1.25 sl l 5WD 5WDbs RE(b)7 + CT(b)7/u2 1 636 RE 1-2 50 VP m N S2 B0 R0 1.25 sl l 7W 6Wbs RE(b)7/u2 + AS 1 1223 RE 1-2 50 VP m N S2 B0 R0 1.25 sl l 7W 6Wbs RE(b)7/u2 1 1487 RE 1-2 50 VP m N S2 B0 R0 1.25 sl l 7W 6Wbs RE(b)2/u3-2 1 585 RE 1-2 50 W m N S2 B0 R0 2.75 sl l 3D 4Dbs RE(v)2 + SN(v)1/s5 1 899 RE <1 50 W m N S2 B0 R0 12 sl l 4TR 4Dbs RE(v)2/s4 1 513 RE <1 50 W m N S2 B0 R0 7 sl l 3TRD 4Dbs RE(b)2 + SN(b)2/u3 7 21049 RE 1-2 50 W m N S2 B0 R0 3.5 sl l 3D 4Dbs RE(b)2 + SN(b)1/u3 1 9466 RE 1-2 50 W m N S2 B0 R0 3.5 sl l 3D 4Dbs RE(v)2 + SB(b)4/u3 1 4345 RE <1 50 W m N S2 B0 R0 3.5 sl l 3RD 4Dbs RE(v)2 + LL(v)2/s6-5 1 3290 RE <1 50 W m N S2 B0 R0 19.5 sl l 5T 4Dbs RE(v)2 + SN(v)1/s5-4 1 1026 RE <1 50 W m N S2 B0 R0 10 sl l 4TR 4Dbs RE(b)2/u3 + SN(v)2/s5 1 10792 RE 1-2 50 W m N S2 B0 R0 3.5 sl l 3D 4Dbs RE(b)2 + SN(b)2/u3-2 1 2821 RE 1-2 50 W m N S2 B0 R0 2.75 sl l 3D 4Dbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry RE(b)2/u3 4 21731 RE 1-2 50 W m N S2 B0 R0 3.5 sl l 3D 4Dbs RE(v)2 + SN(v)2/u2 1 4174 RE <1 50 W m N S2 B0 R0 1.25 sl l 3RD 4Dbs RE(b)2 + SN(v)2/m4 1 24042 RE 1-2 50 W m N S2 B0 R0 7 sl l 3TD 4Dbs RE(b)3 + SN(b)3/u2 1 253 RE 1-2 50 W m N S2 B0 R0 1.25 sl l 3D 4Dbs RI4/u3 2 670 RI >2 100 I l N S0 B0 R0 3.5 sl s 3WF 4Fjp RI6 + GG6/u2 1 4110 RI >2 100 P l N S0 B0 R0 1.25 sl s 4W 6Wbs RI2/u3 1 1622 RI >2 100 R l N S0 B0 R0 3.5 sl s 3MF 4MFjp RS(b)4/u3 1 125 RS 1-2 45 I m N S2 B0 R0 3.5 l l 4WD 4DWbs RS(b)4 + RE(b)4/u3 1 3040 RS 1-2 45 I m N S2 B0 R0 3.5 l l 4WD 4DWbs RS(b)4/u2-3 1 443 RS 1-2 45 I m N S2 B0 R0 2.75 l l 4WD 4DWbs RS(b)6/u2 1 590 RS 1-2 45 P m N S2 B0 R0 1.25 l l 5WD 5WDbs SB(b)5 + SN(b)4/u3 2 7821 SB 1-2 40 I l N S2 B0 R0 3.5 l cl 4DW 4DWbs SB(b)4/u3 9 27214 SB 1-2 40 I l N S2 B0 R0 3.5 l cl 4DW 4DWbs SB(b)4 + SN(b)2/u3 1 12580 SB 1-2 40 I l N S2 B0 R0 3.5 l cl 4DW 4DWbs SB(b)5/u2 1 2436 SB 1-2 40 I l N S2 B0 R0 1.25 l cl 4DW 4DWbs SB(b)5/u3 5 18231 SB 1-2 40 I l N S2 B0 R0 3.5 l cl 4DW 4DWbs SB(b)4 + RE(b)4/u3 1 7810 SB 1-2 40 I l N S2 B0 R0 3.5 l cl 4DW 4DWbs SB(b)2 + SN(b)2/u3 1 5863 SB 1-2 40 MW l N S2 B0 R0 3.5 l cl 3D 4DFbs SB(b)2 + RE(b)2/u3 1 172 SB 1-2 40 MW l N S2 B0 R0 3.5 l cl 3D 4DFbs SB(v)2/s5-6 2 3208 SB <1 40 MW l N S2 B0 R0 19.5 l cl 5T 4DFbs SB(b)3/u3 1 1422 SB 1-2 40 MW l N S2 B0 R0 3.5 l cl 3D 4DFbs SB(v)2 + SN(v)1/u3 1 692 SB <1 40 MW l N S2 B0 R0 3.5 l cl 3DR 4DFbs SB(b)2/u3 5 4274 SB 1-2 40 MW l N S2 B0 R0 3.5 l cl 3D 4DFbs SB(b)2 + RE(b)2 + SN(v)2/m5 1 3511 SB 1-2 40 MW l N S2 B0 R0 12 l cl 4T 4DFbs SB(b)2/u2-3 1 2348 SB 1-2 40 MW l N S2 B0 R0 2.75 l cl 3D 4DFbs SB6/u2 + AS 1 1002 SB >2 40 P l N S2 B0 R0 1.25 l cl 5WD 5WDbs SB(b)6/u3 1 2385 SB 1-2 40 P l N S2 B0 R0 3.5 l cl 5WD 5WDbs SB(b)6 + RE(b)5/u2 2 4942 SB 1-2 40 P l N S2 B0 R0 1.25 l cl 5WD 5WDbs SB(b)6 + BB(b)5/u3 1 2708 SB 1-2 40 P l N S2 B0 R0 3.5 l cl 5WD 5WDbs SB(b)6/u2 + AS 3 38043 SB 1-2 40 P l N S2 B0 R0 1.25 l cl 5WD 5WDbs SB(b)6/u2 1 2733 SB 1-2 40 P l N S2 B0 R0 1.25 l cl 5WD 5WDbs SB(b)7/u2 + AS 1 6531 SB 1-2 40 VP l N S2 B0 R0 1.25 l cl 7W 6Wbs SB(b)7 + BB(b)7/u2 1 1837 SB 1-2 40 VP l N S2 B0 R0 1.25 l cl 7W 6Wbs SD 2 102 SD >2 n/a n/a n/a n/a n/a B0 R0 n/a n/a n/a - - SM 3 378 SM >2 n/a n/a n/a n/a n/a B0 R0 n/a n/a n/a - - SM + BB7/l1 1 214 SM >2 n/a n/a n/a n/a n/a B0 R0 n/a n/a n/a - - Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry SM + SD 1 127 SM >2 n/a n/a n/a n/a n/a B0 R0 n/a n/a n/a - - SN(v)1 + RE(b)2/s4-5 1 6303 SN <1 100 W l N S3 B0 R0 10 sl sl 4TR 4FMjp SN(v)1/s4-5 1 1725 SN <1 100 W l N S3 B0 R0 10 sl sl 4TR 4FMjp SN(v)2/u2 1 1095 SN <1 100 W l N S3 B0 R0 1.25 sl sl 3RPM 4FMjp SN(v)2 + RE(b)4/u2-3 3 13888 SN <1 100 W l N S3 B0 R0 2.75 sl sl 3RPM 4FMjp SN(v)1/s5 1 1057 SN <1 100 W l N S3 B0 R0 12 sl sl 4TR 4FMjp SN(v)1/s4 1 708 SN <1 100 W l N S3 B0 R0 7 sl sl 3RPM 4FMjp SN(b)3 + SB(b)3/u3 1 1725 SN 1-2 100 W l N S3 B0 R0 3.5 sl sl 3PM 4FMjp SN(b)2/u3 1 1020 SN 1-2 100 W l N S3 B0 R0 3.5 sl sl 3PM 4FMjp SN2 + RE2/u3 1 3900 SN >2 100 W l N S3 B0 R0 3.5 sl sl 3PM 4FMjp SN(v)2 + RE(b)2/u3 1 1352 SN <1 100 W l N S3 B0 R0 3.5 sl sl 3RPM 4FMjp SN(b)2 + RE(b)3/u3 1 1668 SN 1-2 100 W l N S3 B0 R0 3.5 sl sl 3PM 4FMjp SN(b)2/u2 1 1651 SN 1-2 100 W l N S3 B0 R0 1.25 sl sl 4PM 4FMjp SN(v)1 + RE(b)2/s6 1 785 SN <1 100 W l N S3 B0 R0 22.5 sl sl 5T 4FMjp SN(v)2/u3 1 2528 SN <1 100 W l N S3 B0 R0 3.5 sl sl 3RPM 4FMjp SN(b)2 + RE(b)2/u3 2 1919 SN 1-2 100 W l N S3 B0 R0 3.5 sl sl 3PM 4FMjp SN(v)2 + RE(b)2/s4-5 3 2434 SN <1 100 W l N S3 B0 R0 10 sl sl 4TR 4FMjp SQ 7 1111 SQ >2 150 VP h N S0 B0 R0 0.25 n/a n/a O 6Wbs TC6 + BB6/u2 1 153 TC >2 30 P h N S0 B0 R0 1.25 sicl sic 5WD 5WDbs TC6/u3 1 2662 TC >2 30 P h N S0 B0 R0 3.5 sicl sic 5WD 5WDbs TC(b)6 + RB(b)6/u2 1 739 TC 1-2 30 P h N S0 B0 R0 1.25 sicl sic 5WD 5WDbs TC(b)6 + SB(b)5/u2 1 816 TC 1-2 30 P h N S0 B0 R0 1.25 sicl sic 5WD 5WDbs TC6 + BR4/u2-3 1 2026 TC >2 30 P h N S0 B0 R0 2.75 sicl sic 5WD 5WDbs TC(b)6 + BB(b)6/u2 1 337 TC 1-2 30 P h N S0 B0 R0 1.25 sicl sic 5WD 5WDbs TC7 + RB6/l2 1 1511 TC >2 30 VP h N S0 B0 R0 1.25 sicl sic 7W 6Wbs TC7/u2 1 323 TC >2 30 VP h N S0 B0 R0 1.25 sicl sic 7W 6Wbs TC7/u2 + SM 1 174 TC >2 30 VP h N S0 B0 R0 1.25 sicl sic 7W 6Wbs TF4 + TT5 + PD5/u3 1 3110 TF >2 100 I m N S3 B0 R0 3.5 l l 3P 3Fbs TF(v)1 + JU(v)1/y6 R1 1 7293 TF <1 100 W m N S3 B0 R1 22.5 l l 5TR 4RFbs TF(v)1 + JR(v)1 + PD(b)2/y6-7 1 3439 TF <1 100 W m N S3 B0 R0 30 l l 5T 3Fbs TF(b)2 + TT(b)2 + PD(b)2/m4 1 15088 TF 1-2 100 W m N S3 B0 R0 7 l l 3P 3Fbs TF(v)1 + TT(v)2/r5-6 1 2618 TF <1 100 W m N S3 B0 R0 19.5 l l 5T 3Fbs TF(b)3 + NR(v)3 + JR3(b)/h4-5 1 10446 TF 1-2 100 W m N S3 B0 R0 10 l l 4T 3Fbs TF(v)2 + LL(v)2 + TH(v)1/m5-4 1 2002 TF <1 100 W m N S3 B0 R0 10 l l 4TR 3Fbs TF(v)2 + MG(v)2/h5-6 1 788 TF <1 100 W m N S3 B0 R0 19.5 l l 5T 3Fbs TF(v)1 + NR(v)1/y5 1 1887 TF <1 100 W m N S3 B0 R0 12 l l 4TR 3Fbs Table 5. Selected interpretations of soil map units cont’d

Depth to Depth to Average Surface Parent No. of Area Dominant bedrock compact Drain- Ston- Boulder- Rock- Slope soil material CLI CLI Map Unit Symbol polygons (ha) soil (m) (cm) age Fertility Flooding iness iness iness (%) texture texture Agriculture Forestry TF(v)1 + TT(v)2 + BO(v)2/r6-8 1 2109 TF <1 100 W m N S3 B0 R0 42.5 l l 6T 3Fbs TF(b-v)2 + JU(v)1 + CT(b)2/y6-5 1 6949 TF 1-2 100 W m N S3 B0 R0 19.5 l l 5T 3Fbs TH(b)4 + CB(b)4/u3 1 3067 TH 1-2 100 I h N S2 B0 R0 3.5 l l 3W 3Fbs TH(v)1/m6 R1 + HM(v)3/m5 R1 1 15398 TH <1 100 W h N S2 B0 R1 22.5 l l 5TR 4Rbs TH(v)1/m6 R1 1 3048 TH <1 100 W h N S2 B0 R1 22.5 l l 5TR 4Rbs TH(v)1 + CB(v)2/s6-7 R1 1 1047 TH <1 100 W h N S2 B0 R1 30 l l 5TR 4Rbs TH(v)1 + CR(b)2/s6 1 1178 TH <1 100 W h N S2 B0 R0 22.5 l l 5T 3Fbs TH(v)1 + CR(b)2/s7 1 889 TH <1 100 W h N S2 B0 R0 37.5 l l 6T 3Fbs TH(v)1 + JR(v)1 + TF(v)1/s8 R1 1 12792 TH <1 100 W h N S2 B0 R1 57.5 l l 6T 5Rbs TH(b)3 + MG(v)2/u3 1 2260 TH 1-2 100 W h N S2 B0 R0 3.5 l l 2C 3Fbs TH(b)3 + CB(v)2/u3 1 9079 TH 1-2 100 W h N S2 B0 R0 3.5 l l 2C 3Fbs TH(b)2 + MG(b)2/m5 1 10060 TH 1-2 100 W h N S2 B0 R0 12 l l 4T 3Fbs TH(v)1/s-y9-7 R1 1 14663 TH <1 100 W h N S2 B0 R1 65 l l 7T 5Rbs TH(b)2/m5 1 3337 TH 1-2 100 W h N S2 B0 R0 12 l l 4T 3Fbs TH(v)2 + CR(b)2 + LL(b)2/m5-4 1 9978 TH <1 100 W h N S2 B0 R0 10 l l 4TR 3Fbs TH(v)2 + CR(b)2 + NR(b)2/m4 1 2674 TH <1 100 W h N S2 B0 R0 7 l l 3TR 3Fbs TH(v)1 + CR(b)2 + VO(b)2/y7-8 1 380 TH <1 100 W h N S2 B0 R0 50 l l 6T 5Rbs TH(v)1 + MG(v)1 + CB(v)2/s6-8 R1 1 16047 TH <1 100 W h N S2 B0 R1 42.5 l l 6T 4Rbs TH(v)1 + CB(v)2/s8 R1 1 4100 TH <1 100 W h N S2 B0 R1 57.5 l l 6T 5Rbs TH(v)2 + CR(v)3/r4-5 1 17982 TH <1 100 W h N S2 B0 R0 10 l l 4TR 3Fbs TU(b)5 + LL(b)5/u3 1 2464 TU 1-2 50 I l N S3 B0 R0 3.5 l l 4WD 4DWFbs TU(b)6 + JU(b)5/u3 1 579 TU 1-2 50 P l N S3 B0 R0 3.5 l l 5WD 5WDbs TU(b)2 + JU(b)1 + BM(v)1/y6-7 1 1227 TU 1-2 50 W l N S3 B0 R0 30 l l 5T 4DFbs TU(b)2 + JU(b)1/y5 1 6655 TU 1-2 50 W l N S3 B0 R0 12 l l 4T 4DFbs TU(b)3 + CT(b)3/m4 1 3861 TU 1-2 50 W l N S3 B0 R0 7 l l 3P 4DFbs TU(b)2 + JU(v)3/m5 1 1596 TU 1-2 50 W l N S3 B0 R0 12 l l 4T 4DFbs TU2 + JU2/m5 1 2770 TU >2 50 W l N S3 B0 R0 12 l l 4T 4DFbs TU(b)3 + JU(b)3/m5 1 3927 TU 1-2 50 W l N S3 B0 R0 12 l l 4T 4DFbs TU(v)2/m5-4 1 15176 TU <1 50 W l N S3 B0 R0 10 l l 4TR 4DFbs TU(b)2 + JU(b)3/m4-5 1 3074 TU 1-2 50 W l N S3 B0 R0 10 l l 4T 4DFbs TU(b)3 + JU(b)3/m6 2 3567 TU 1-2 50 W l N S3 B0 R0 22.5 l l 5T 4DFbs TU(b)2 + JU(b)2/m5-6 1 3867 TU 1-2 50 W l N S3 B0 R0 19.5 l l 5T 4DFbs TU(v)1/y5-7 1 343 TU <1 50 W l N S3 B0 R0 27 l l 5T 4DFbs TU(b)2 + JU(b)1/m6 2 8625 TU 1-2 50 W l N S3 B0 R0 22.5 l l 5T 4DFbs TU(b)3 + JU(b)3/m3-4 1 2852 TU 1-2 50 W l N S3 B0 R0 5.5 l l 3P 4DFbs TU(b)2 + JU(v)1/y6 1 2136 TU 1-2 50 W l N S3 B0 R0 22.5 l l 5T 4DFbs Table 5. Selected interpretations of soil map units cont’d

Notes: The depth recorded under “Depth to Compact” assumes that bedrock does not occur within the profile. 127

REFERENCES

Airphoto Analysis Associates Consultants Ltd. 1975. Marshall, I. B. 1977. Soils of Canada: Volume I soil report. Wetlands, peatlands resources, New Brunswick. Report to Research Branch, Agriculture Canada, Ottawa, Ont. 243 pp. New Brunswick Department of Natural Resources, Fredericton, N. B. 106 pp. Colpitts, M. C., Fahmy, S. H., MacDougall, J. E., Ng, T. T. M., McInnis, B. G., and Zelazny, V. F. 1995. Forest soils of Arno, J. R., Struchtemeyer, R. A., Langmaid, K. K. and New Brunswick. CLBRR Contrib. No. 95-38, Timber Millette, J. F. G. ca 1964. A look at the Caribou soils - A Management Branch, New Brunswick Dept of Natural compilation of data on the Caribou soil series. U. S. Resources and Energy, Fredericton, N. B. 51 pp. Department of Agriculture, Soil Conservation Service in cooperation with Maine Agricultural Experiment Station, Dillon, M. J., Rees, H. W., Loro, P. J., Matthews, D. B. and Orono, Maine and Canada Department of Agriculture, New Walker, G. M. 1996. Soil evaluation for agriculture at the Brunswick Soil Survey, Fredericton, New Brunswick. 72 farm, watershed and regional levels in New Brunswick. pp. Pages 55-71 in conference Proceedings, 1996 International CARIS Conference, June 10-11, 1996, Fredericton, New Atlantic Advisory Committee on Soil Survey. 1988. Brunswick, Canada. Compendium of soil survey interpretive guides used in the Atlantic Provinces. 149 pp. Dzikowski, P.A., Kirby, G., Read, G. and Richards, W.G. 1984. The climate for agriculture in Atlantic Canada. Publ. Bostock, H. S. 1970. A provincial physiographic map of No. ACA 84-2-500, Agdex No. 070, Atlantic Advisory Canada. Geol. Surv. Can. Pap. 64-35, 1964; and Geological Committee on Agrometeorology. Survey of Canada Map 1245 A. Expert Committee on Soil Survey. 1982 (revised).The Brady, N. C. 1974. The nature and properties of soils. 8th Canada Soil Information System (CanSIS) Manual for Edition. MacMillan Publ. Co., Inc., New York, New York, describing soils in the field. Edited by J. H. Day. L. R. R. I. U.S.A. 639 pp. Contribution No. 82-52. Research Branch, Agriculture Canada, Ottawa, Ontario. Buol, S. W., Hole, F. D. and McCracken, R. J. 1973. Soil genesis and classification. The Iowa State University Press, Fahmy, S. H. and Rees, H. W. 1996. Soils of the Ames, Iowa, U.S.A. 360 pp. Woodstock-Florenceville Area, Carleton County, New Brunswick. Volume 3. New Brunswick Soil Survey Report Canada Land Inventory. 1965. Soil capability classification No. 14. CLBRR Contribution No. 96-02. Research Branch, for agriculture. Canada Land Inventory Report No. 2. Agriculture Canada. 93 pp. Information Canada, Ottawa, Ont. 16 pp. Fahmy, S. H., Rees, H. W. and Mac Millan, J. K. 1986. Canada Land Inventory. 1967. Land capability Soils of New Brunswick: A first approximation. New classification for forestry. Canada Land Inventory Report Brunswick Department of Agriculture, Fredericton, N. B. No. 4. McCormack, R. J., editor. Information Canada, 105 pp. Ottawa, Ont. 72 pp. Gary, M., McAfee, R. and Wolf, C. L. (eds). 1972. Glossary Canada Soil Survey Committee. 1978. The Canadian system of geology. American Geological Institute, Washington, D. of soil classification. Can. Dep. Agric. Publ. 1646. Supply C. 805 pp. and Services Canada, Ottawa, Ont. 164 pp. Gauthier, R.C. 1983. Surficial materials of northern New Chalmers, R. 1888. Report on the surficial geology of Brunswick. Open File 963. Geol. Surv. Can., Ottawa, Ont. northeastern New Brunswick. Summary Report for 1887-88, V. 3, Part N., Geol. Surv. Can. Ottawa, Ont. Langmaid, K. K. 1964. Some effects of earthworm invasion in virgin podzols. Can. J. Soil Sci. 44: 34-37. Chapman, L. J. and Brown, D. M. 1966. The climates of Canada for agriculture. Report No. 3. The Canada Land Maritime Resource Management Service. 1978. Soils and Inventory, Agriculture and Rural development Act. related developmental interpretations of the Belledune Department of Forestry and Rural Development, Ottawa, Planning District. Prepared for the Belledune Planning Ont. 24 pp. Commission by Maritime Resource Management Service, Amherst, N. S. 218 pp. Clayton, J. S., Ehrlich, W. A., Cann, D. B., Day, J. H. and 128

N. B. Department of Agriculture and Rural Development. Soil Science Society of America. 1978. Glossary of soil 1981. Agricultural Statistics, 1981 ed. Statistics Canada science terms. Soil Science Society of America, Madison, and N. B. Department of Agriculture and Rural Wisconsin. 36 pp. Development, Fredericton, N. B. 59 pp. Stobbe, P. C. 1940. Soil Survey of the Fredericton- N. B. Department of Commerce and Development. No Gagetown Area, New Brunswick.First report of the New date. New Brunswick in profile. N. B. Department of Brunswick Soil Survey. Publ. 709, Tech. Bull. 30, Commerce and Development, Fredericton, N. B. 62 pp. Dominion of Canada-Department of Agriculture, Ottawa, Ont. 51 pp (with map). Olson, G. W. 1981. Soils and the Environment. A guide to soil surveys and their applications. Chapman and Hall, Van Groenewoud, H. 1983. Summary of climatic data New York, New York 178 pp. pertaining to the climatic regions of New Brunswick. Information Report M-X-146. Environment Canada, Potter, R. R., Hamilton, J. B. and Davies, J. L. 1979. Canadian Forestry Service, Maritime Forest Research Geological map of New Brunswick, 2nd edition. Map Centre, Fredericton, N.B. Number N. R. -1. Mineral Resources Branch, New Brunswick Department of Natural Resources, Fredericton, Wang, C, Ross, G. J. and Rees, H. W. 1981. N. B. Characteristics of residual and colluvial soils developed on granite and of the associated pre-Wisconsin landforms Putnam, D. F. 1952. Canadian regions: A geography of in north-central New Brunswick. Can. J. Earth Sci. Canada. J. M. Dent and Sons (Canada) Ltd., 18(3):487-494. Bownamville, Ont. 601 pp. Wang, C. and Rees, H. W. 1983. Soils of the Rampton, V. N., Gauthier, R. C., Thibault, J. and Seaman, Rogersville-Richibucto Region of New Brunswick. Ninth A. A. 1984. Quaternary geology of New Brunswick. Report of the New Brunswick Soil Survey. Research Memoir 416.Geological Survey of Canada, Ottawa, Branch, Agriculture Canada and New Brunswick Ontario. 77 pp (with maps). Department of Agriculture and Rural Development, Fredericton, New Brunswick. 239 pp. Research Branch, Canada Dept of Agriculture. 1976. (Revised). Glossary of terms in soil science. Information Weeks, L. J. 1957. The Appalachian region. Pages 123- Division, Canada Department of Agriculture, Ottawa, 205 in C. H. Stockwell, editor. Geology and economic Ontario. Publication 1459. 44 p. minerals of Canada, 4th edition. Geol. Surv. Can. Econ. Ser. No. 1. Rowe, J. S. 1972. Forest regions of Canada. Publ. No. 1300, Department of the Environment, Canadian Forestry Wein, R. W. and Moore, J. M. 1977. Fire history and Service, Ottawa, Ontario. 172 pp with map. rotations in the New Brunswick Acadian forest. Can. J. For. Res. 7(2):285-294. Smith, B. M. 1982. Selected summaries from 1978 New Brunswick forest inventory. Forest Management Branch, New Brunswick Department of Natural Resources, Fredericton, N. B.

Soil Classification Working Group. 1998. The Canadian system of soil classification. Agric. and Agri-Food Canada Publ. 1646 (Revised). 187 pp. 129

GLOSSARY - GENERAL TERMS* ablation till A surface of loose, permeable somewhat, chroma, color The relative purity, strength, or saturation stratified sandy and stony till usually overlying denser till. of a color (related to grayness). acid soil A soil having a pH of 5.5 or lower (generally pH classification The systematic arrangement of soils into 4.0 to 5.5). categories on the basis of their characteristics. alluvium Material such as clay, silt, sand and gravel clay As a soil separate, the mineral soil particles less than deposited by modern rivers and streams. 0.002 mm in diameter: usually consisting largely of clay minerals. association, soil A natural grouping of soil or landscape segments based on similarities in climatic or physiographic clay films (skins) Coatings of oriented clays on the factors and soil parent materials. surfaces of soil peds (natural unit of soil structure) and mineral grains, and in soil pores. available rooting zone That depth of soil material which is suitable for root growth and penetration. Soil matrix bulk coarse fragments Rock fragments greater than 2 mm in densities of greater than 1.60 g/cm3 are considered a serious diameter, including gravels, cobbles, stones and boulders. limitation to root growth. cobbles Rock fragments 7.5 to 25 cm in diameter. available water The portion of water in a soil that can be readily absorbed by plant roots. It is the water held in the complex, soil A mapping unit used in soil surveys where soil against a pressure of 33 kPa to 1500 kPa, expressed in two or more soil associations are so intimately intermixed in centimetres of water per centimetre of soil, and reported on an area that it is impractical to separate them at the scale of a whole soil basis (soil <2 mm diameter, plus coarse mapping used. fragments). compact Said of any soil that has a firm or dense bedrock exposure When the solid rock that usually consistence and whose particles are closely packed with very underlies soil is exposed at the surface or is covered by less little intervening space. Compact soils typically have a than 10 cm of unconsolidated material. matrix bulk density (particles less than 2 mm diameter) of greater than 1.60 g/cm3. bisequal Two sequa in one soil; that is, two sequences of an eluvial horizon and its related illuvial horizon. compaction (soil) Any process (such as by weight of overburden or dessication) by which a soil mass loses pore bog Sphagnum or forest peat materials formed in an space and achieves a higher density. ombrotrophic environment due to the slightly elevated nature of the bog tending to be disassociated from nutrient- consistence The resistance of a material to deformation or rich ground water or surrounding mineral soils. rupture. The degree of cohesion or adhesion of the soil mass. Terms used for describing consistence are for specific boulders Rock fragments greater than 100 cm in diameter. soil moisture contents, i.e. moist soil: loose, very friable, friable, firm, very firm. bulk density The mass of dry soil per unit bulk volume, 3 often expressed in g/cm . In this report, the bulk density is control section The vertical section of soil upon which reported for the material <2 mm diameter. classification is based. Typically 1 m in mineral soils and 1.6 m in organic soils, but less in cases of shallow to calcareous A material containing sufficient calcium bedrock, and in the case of organic soils, shallow to a carbonate, often with magnesium carbonate, to effervesce mineral soil. visibly when treated with cold 0.1 N hydrochloric acid. coprogenous earth A material in some organic soils that catena A nontaxonomic grouping of a sequence of soils of contains at least 50% by volume of fecal pellets less than 0.5 about the same age, derived from similar parent materials, mm in diameter. and occurring under similar climatic conditions, but having unlike characteristics because of variations in relief and core zone The central regions of raised and blanket bogs. drainage.

* Source of most entries in Glossary - General Terms: Airphoto Analysis Associates Consultants Ltd. (1975); Research Branch, Canada Dept of Agriculture (1976); and Soil Science Society of America (1978). 130 deglaciation The uncovering of a land area from beneath geomorphic Pertaining to the form of the Earth or of its a glacier or ice sheet by the withdrawal of ice due to surface features. shrinkage by melting. glacial drift A general term applied to all rock material deposit Material left in a new position by a natural (clay, silt, sand, gravel, cobbles, boulders) transported by a transporting agent such as water, wind, ice or gravity. glacier and deposited directly by or from the ice, or by running water emanating from the glacier. drainage (soil) The frequency and duration of periods when the soil is free of saturation. glaciation The alteration of a land surface by the massive movement over it of glacier ice. eluviation The transportation of soil material in suspension or in solution within the soil by the downward or lateral glacier A body of ice, consisting mainly of recrystallized movement of water. snow, flowing on a land surface. ericaceous Pertaining to or like heath plants; belonging to glaciofluvial deposits Material moved by glaciers and the heath family of plants. subsequently sorted and deposited by streams flowing from the melting ice. esker A winding ridge of irregularly stratified sand, gravel, and cobbles deposited under the ice by rapidly flowing glaciolacustrine Sediment generally consisting of stratified glacial streams. fine sand, silt, and clay deposited on a lake bed. Glacial ice exerted a strong but secondary control upon the mode of eutrophic Said of an environment characterized by an origin in that glacier ice was close to the site of deposition. abundance of dissolved plant nutrients such as nitrogen, potassium, phosphorus and calcium. glaciomarine Unconsolidated sorted and stratified deposits of clay, silt, sand, or gravel that have settled from evapotranspiration The loss of water by evaporation from suspension in salt or brackish water bodies. Glacial ice the soil and by transpiration from plants. exerted a strong but secondary control upon the mode of origin in that glacier ice was close to the site of deposition. fen Sedge peat materials derived primarily from sedges with inclusions of partially decayed stems of shrubs formed gleysation A soil-forming process, operating under poor in a eutrophic environment due to the close association of drainage conditions, which results in the reduction of iron the material with mineral-rich waters. and other elements and in gray colors, and mottles. fibric Said of an organic soil material containing large gravel Rock fragments 2 mm to 7.5 cm in diameter. amounts of weakly decomposed fiber whose botanical origin is readily identifiable. groundwater Water beneath the soil surface, usually under conditions where the voids are completely filled with water flaggs Thin fragments of sandstone, limestone, slate or (saturation). shale. grus An accumulation of waste consisting of angular, flark zone Found in organic soils, it borders the core zone, coarse-grained fragments resulting from the granular or central regions of raised and blanket bogs. The flark zone disintegration of crystalline rocks (esp. granite). is characterized by large parallel embankments formed by rows of hummocks that surround the peat bog in a step-like horizon, soil A layer in the soil profile approximately manner. Flashets (ponds) occur between the hummocks parallel to the land surface with more or less well-defined oriented at right angles to the direction of the slope. characteristics that have been produced through the operation of soil forming processes. floodplain Land bordering a stream, built up of sediments from overflow of the stream and subject to inundation when humic Said of an organic soil material containing large the stream is at flood stage. amounts of highly decomposed organic materials with little identifiable fiber. fluvial deposits All sediments, past and present, deposited by flowing water, including glaciofluvial deposits. hummocky A very complex sequence of slopes extending from somewhat rounded depressions or kettles of various fragipan A natural subsurface horizon having a higher sizes to irregular to conical knolls and knobs. bulk density than the solum above; seemingly cemented when dry, but showing moderate to weak brittleness when illuviation The process of depositing soil material removed moist. from one horizon in the soil to another, usually from an 131 upper to a lower horizon in the soil profile. Illuviated moraine A mound, ridge or other distinct accumulation of substances include silicate clay, hydrous oxides of iron and unsorted, unstratified glacial drift, predominantly till, aluminum, and organic matter. deposited chiefly by direct action of glacier ice in a variety of topographic landforms that are independent of control by impeded drainage A condition that hinders the movement the surface on which the drift lies. of water by gravity through soils. mottles Irregularly marked spots or streaks, usually yellow inclusion A soil type found within a mapping unit that is or orange but sometimes blue, that indicate poor aeration not extensive enough to be mapped separately or as part of and lack of good drainage. They are described in terms of a complex. abundance, size and contrast. kame An irregular ridge or hill of stratified glacial drift mull A humus form in which there is extensive deposited by glacial meltwater. decomposition of forest litter and intimate association of colloidal organic matter with mineral soil. A forest mull lacustrine Material deposited in lake water and later implies a steady state of faunal activity with regular passage exposed by either lowering of the water level or by uplifting of organic matter and mineral particles through the guts of of the land. These sediments range in texture from sands to earthworms. Diagnostic organic layers are lacking. clays. neutral soil A soil which is neither acid or alkaline in lagg The areas at bog edges adjacent to mineral soil where reaction, typically considered pH 5.5 to 7.5. waters flow or stagnate. nonsoil The collection of soil material or soil-like material land type Natural and man-made units in the landscape that does not meet the definition of soil. Nonsoil includes that are either highly variable in content, have little or no soil displaced by unnatural processes, unconsolidated natural soil, or are excessively wet. material unaffected by soil-forming processes, unconsolidated mineral or organic material thinner than 10 landform The various shapes of the land surface resulting cm overlying bedrock, and soils covered by more than 60 from a variety of actions such as deposition or cm of water. sedimentation, erosion, and earth crust movements. ombrotrophic Said of an environment characterized by a lithology The description of rock fragments on the basis of shortage of plant nutrients due to a disassociation from such characteristics as color, structure, mineralogic nutrient-rich waters. composition and grain size. organic matter The organic fraction of the soil; includes lodgment till Material deposited from rock debris in plant and animal residues at various stages of transport in the base of a glacier. As it is “plastered” into decomposition, cells and tissues of soil organisms, and place, this till is compact and not sorted. substances synthesized by the soil population. mineral soil A soil consisting predominantly of, and organic soil Organic soils consist of peat deposits having its properties determined predominantly by, mineral containing more than 30% organic matter by weight (17% matter. It contains less than 30% organic matter (17% organic carbon) and are usually greater than 40 to 60 cm organic carbon), except for an organic surface layer that may thick. be up to 60 cm thick. outwash Sediments washed out by flowing water beyond mode of deposition The method whereby soil parent the glacier and laid down as stratified beds with particle material has been left in a new position by a natural sizes ranging from boulders to silt. transporting agent such as water or ice. overburden The loose soil or other unconsolidated moder A forest humus form (litter layer), especially under material overlying bedrock. northern hardwoods, where the mixing of organic and mineral particles is purely mechanical with no formation of paludification The process of peat formation. true organomineral complexes. The mixing is due to microarthropod activity. parent material The unconsolidated and more or less chemically weathered mineral or organic matter from which mor A type of forest humus (litter layer) in which the the solum of a soil has developed by soil forming processes. organic forest floor layer is present and there is practically no mixing of the surface organic matter with mineral soil. particle size class Refers to the grain size distribution of The transition from organic to mineral horizon is abrupt. the whole soil including the coarse fraction. It differs from 132 texture, which refers to the fine earth (<2 mm) fraction only. polygon Any delineated area shown on a soil map that is In addition, textural classes are usually assigned to specific identified by a symbol. horizons whereas particle-size classes indicate a composite particle size of all or a part of the control section. See pores, macro Soil voids that are readily drained of free particle size classes triangle below. water, based on water retention at 100 cm of water suction. Herein considered on a whole soil basis (soil <2 mm diameter, plus coarse fragments).

pores, micro Soil voids that are not readily drained of free water, based on water retention at 100 cm of water suction. Herein considered on a whole soil basis (soil <2 mm diameter, plus coarse fragments).

porosity, total The total space not occupied by solid particles in a bulk volume of soil. Herein considered on a whole soil basis (soil <2 mm diameter, plus coarse fragments).

post glacial Pertaining to the time interval since the total disappearance of continental glaciers.

profile, soil A vertical section of the soil through all its horizons and extending into the parent material.

reaction, soil The degree of acidity or alkalinity of a soil, peat Unconsolidated soil material consisting largely of usually expressed as a pH value. organic matter. regolith The unconsolidated mantle of weathered rock and pedogenic Pertaining to soil formation. soil material overlying solid rock. pedology The aspects of soil science dealing with the reworked Descriptive of material modified after its origin, morphology, genesis, distribution, mapping, and preliminary deposition, commonly by water. taxonomy of soils, and classification in terms of their use. rockiness Defined on the basis of the percentage of the perhumid A soil moisture regime that experiences no land surface occupied by bedrock exposures. significant water deficits in the growing season. Water deficits are less than 2.5 cm. sand A soil particle between 0.05 and 2.0 mm in diameter. permeability, soil The ease with which gases and liquids saturated hydraulic conductivity The effective flow penetrate or pass through a bulk mass of soil or a layer of velocity or discharge velocity in saturated soil at a unit soil. hydraulic gradient. An approximation of the permeability of the soil, expressed in centimetres per hour. perviousness See: permeability. seepage The down-slope horizontal movement of water petrology Deals with the origin, occurrence, structure and within the soil profile on top of a layer of restricted history of rocks. permeability. pH, soil The negative logarithm of the hydrogen-ion series, soil The basic unit of soil classification consisting activity of a soil. The degree of acidity or alkalinity of soil of soils that are essentially alike in all major profile expressed in terms of the pH scale. characteristics except surface texture. phase, soil A subdivision of a soil association or other unit silt A soil separate consisting of particles between 0.05 and of classification having characteristics that affect the use and 0.002 mm in diameter. management of the soil, but that do not vary sufficiently to differentiate it as a separate association. soil The unconsolidated material on the immediate surface of the earth that serves as a natural medium for the growth physiography The physical geography of an area dealing of land plants and that has been influenced by soil forming with the nature and origin of topographic features. factors. 133 soil-forming factors Natural agencies that are responsible terric Refers to a mineral layer underlying an organic soil. for the formation of soil: parent rock, climate, organisms, The mineral layer occurs within a depth of 160 cm from the relief (drainage) and time. surface. soil map A map showing the distribution of soil types or texture, soil The relative proportions of the various soil other soil mapping units in relation to the prominent separates (sand, silt and clay) in a soil. See texture classes physical and cultural features of the earth’s surface. triangle below. soil survey The whole procedure involved in making a soil resource inventory. The systematic examination, description, classification, mapping and interpreting of soils and soils data within an area. solum The upper horizons of a soil in which the parent material has been modified and in which most plant roots are contained. It usually consists of the A and B horizons. sorted Said of an unconsolidated sediment consisting of particles of essentially uniform size or of particles lying within the limits of a single grade or class. stones Rock fragments greater than 25 cm in diameter. stoniness, surface Defined on the basis of the percentage of the land surface occupied by fragments coarser than 25 cm in diameter. stratified materials Unconsolidated sand, silt and clay arranged in “strata” or layers. till Unstratified glacial material deposited directly by the structure, soil The combination or arrangement of primary ice and consisting of clay, sand, gravel and boulders soil particles into secondary particles, units or peds. These intermingled in any proportion. peds are characterized and classified on the basis of size, shape and degree of distinctness. value, color The relative lightness or intensity of color. surface expression The form (assemblage of slopes) and veneer A thin layer of soil material from 10 cm to 1 m in pattern of forms in a landscape. thickness which does not mask minor irregularities in the underlying unit’s surface, which is often bedrock. swamp A peat-covered or peat-filled area with the water table at or above the peat surface. The dominant peat materials are mesic to humic forest and fen peat formed in a eutrophic environment resulting from strong water movement from the margins or other mineral sources. 134 135

GLOSSARY - ROCK TYPES* argillite A compact rock derived from either mudstone gneiss A foliated rock formed by regional metamorphism (claystone or siltstone) or shale, that has undergone a in which bands or lenticles or granular minerals alternate somewhat higher degree of induration than is present in with bands and lenticles in which minerals having flaky or mudstone or shale but that is less clearly laminated than, and elongate prismatic habits predominate. without the fissility (either parallel to bedding or otherwise) of shale, or that lacks a cleavage distinctive of slate. granites A term loosely applied to any light-colored coarse-grained plutonic rock (pertaining to igneous rocks arkose A feldspar-rich, typically coarse-grained sandstone, formed at great depth) containing quartz as an essential commonly pink or reddish to pale gray or buff, composed of component, along with feldspar (usually white of nearly angular to subangular grains that may be either poorly or white and clear and translucent) and mafic (dark-colored moderately well sorted, usually derived from the rapid minerals) minerals disintegration of granite or granitic rocks. granite gneiss A gneiss derived from a sedimentary or basalt A dark- to medium-dark colored, commonly igneous rock and having a granite mineralogy. extrusive, mafic igneous rock composed chiefly of calcic plagioclase and clinopyroxene in a glassy or fine-grained granodiorites A group of coarse-grained plutonic rocks groundmass (the extrusive equivalent of gabbro) intermediate in composition between quartz diorite and quartz monzonite. basic Said of an igneous rock having a relatively low silica content, sometimes delimited arbitrarily as less than 54%, greywacke A dark (usually gray or greenish gray, e.g. gabbro, basalt sometimes black) and very hard, tough and firmly indurated, coarse-grained sandstone that has a subconchoidal fracture calcareous Said of a substance that contains calcium and consists of poorly sorted and extremely angular to carbonate (CaCO3). When applied to a rock name it implies subangular grains of quartz and feldspar with an abundant that a considerable percentage (up to 50%) of the rock is variety of small, dark rock and mineral fragments embedded calcium carbonate in a preponderant and compact, partly metamorphosed clayey matrix having the general composition of slate and calcite A common rock-forming mineral: CaCO3; usually containing an abundance of very fine-grained micaceous and white, colorless or pale shades of gray, yellow or blue chloritic minerals. conglomerate A coarse-grained clastic sedimentary rock igneous Rock formed from the cooling and solidification composed of rounded (to subangular) fragments larger than of magma, and that has not been changed appreciably since 2 mm in diameter (granules, pebbles, cobbles, boulders) set its formation in a fine-grained matrix of sand, silt or any of the common natural cementing materials (such as calcium carbonate, iron limestone A sedimentary rock consisting chiefly (more oxide, silica, or hardened clay) (the consolidated equivalent than 50% by weight or by areal percentage under the of gravel). microscope) of calcium carbonate, primarily in the form of mineral calcite, with or without magnesium carbonate. diorites A group of plutonic rocks intermediate in composition between acidic and basic rocks, mafic Said of an igneous rock composed chiefly of one or characteristically composed of dark-colored amphibole (esp. more ferromagnesium, dark-colored minerals in its mode. hornblende), acid plagioclase, pyroxene and sometimes a It is the opposite of felsic. small amount of quartz. meta basalt Metamorposed mafic rock which has lost all felsic Applied to an igneous rock having light-colored traces of original texture and mineralogy due to complete minerals in its mode. It is the opposite of mafic. recrystallization gabbro A group of dark-colored, basis intrusive igneous metagabbro Metamorphosed gabbro rocks composed principally of basic plagioclase and clinopyroxene metagreywacke Metamorphosed greywacke

* Source of most entries in Glossary - Rock Types: Gary, M., McAfee, R. and Wolf, C. L. (eds) (1972). 136 metamorphic Rock derived from pre-existing rocks but that shales A fine-grained, indurated, detrital sedimentary rock differ from them in physical, chemical and mineralogical formed by the consolidation (as by compression or properties as a result of natural geological processes, cementation) of clay, silt or mud, and characterized by finely principally heat and pressure, originating within the earth. stratified (Laminae 0.1-0.4 mm thick) structure and/or The pre-existing rocks may have been igneous, sedimentary fissility that is approximately parallel to the bedding (along or another form of metamorphic rock. which the rock breaks readily into thin layers) quartzite A very hard but unmetamorphosed sandstone siltstone An indurated or somewhat indurated silt having consisting chiefly of sand grains that have been completely the texture and composition, but lacking the fine lamination and solidly cemented with secondary silica that the rock or fissility, of slate; a massive mudstone in which the silt breaks across or through the individual grains rather than predominates over clay (intermediate between sandstone and around them shale) rhyolite A group of extrusive igneous rocks, generally slate A compact fine-grained metamorphic rock formed porphyritic (large crystals) and exhibiting flow texture, with from such rocks as shale and volcanic ash, which possesses phenocrysts of quartz and alkali feldspars (esp. orthoclase) the property of fissility along planes independent of the in a glassy to cryptocrystalline groundmass (the extrusive original bedding (slaty cleavage). equivalent of granite) trachyte A group of fine-grained, generally porphyritic, sandstone A medium-grained clastic sedimentary rock extrusive rocks having alkali feldspar, minor mafic minerals composed of abundant and rounded or angular fragments of (biotite, hornblende or pyroxene) as the main components sand size set in a fine-grained matrix (silt or clay) and more or less firmly united by a cementing material (commonly tuff A compacted deposit of volcanic ash and dust that may silica, iron oxide or calcium carbonate); the consolidated or may not contain up to 50% sediments such as sand or equivalent of sand, intermediate in texture between clay. conglomerate and shale. volcanics A generally finely crystalline or glassy igneous schist A strongly foliated crystalline rock formed by rock resulting from volcanic action at or near the Earth’s dynamic metamorphism which can be readily split into thin surface, either ejected explosively or extruded as lava. flakes or slabs due to the well developed parallelism of more than 50% of the minerals present, particularly those of lamellar or elongate prismatic habit, e.g., mica, hornblende sedimentary Rock formed from materials deposited from suspension or precipitated from solution and usually being more or less consolidated. The principal sedimentary rocks are sandstone, shales, limestones and conglomerates. 137

APPENDIX - COMMON AND SCIENTIFIC NAMES OF TREES alder, speckled Alnus rugosa (D. R.) Spr. ash, black Fraxinus nigra M arsh. ash, mountain (American) Sorbus americana M arsh. ash, w hite Fraxinus americana L. aspen, large-tooth Populus grandidentata M ichx. aspen, trembling Populus tremuloides M ichx. beech, American Fagus grandifolia Ehrh. birch, gray or w ire or fire Betula populifolia M arsh. birch, white or paper Betula papyrifera M arsh. birch, yellow Betula alleghaniensis B ritt. cedar, eastern w hite Thuja occidentalis L. cherry, pin Prunus pensylvanica L. elm , w hite Ulmus americana L. fir, balsam Abies balsamea (L .) M ill. hem lock, eastern Tsuga canadensis (L.) Carr. larch, American Larix laricina (Du Roi) C. Koch. m aple, m ountain Acer spicatum Lam . maple, red Acer rubrum L. maple, striped Acer pensylvanicum L. maple, sugar Acer saccharum L. oak, red Quercus rubra L. pine, eastern w hite Pinus strobus L. pine, jack Pinus banksiana Lamb. pine, red Pinus resinosa A it. poplar Populus L. poplar, balsam Populus balsamifera L. spruce, black Picea mariana (M ill.) BSP. spruce, red Picea rubens Sarg. spruce, w hite Picea glauca (M oench) V oss tamarack Larix laricina (Du Roi) C. Kock. w illow ` Salix L.