Soil formation is a complex process influenced by various factors and processes. Understanding these elements is crucial for grasping how different soils develop and their properties.
This section explores the CLORPT factors (Climate , Organisms, Relief, Parent material , and Time) that shape soil development. We'll also dive into weathering processes, soil horizons, and key soil-forming mechanisms that create diverse soil types worldwide.
CLORPT Factors
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Five main factors influence soil formation known as CLORPT factors
Parent material
Climate
Topography
Organisms
Time
Parent material constitutes original geologic or organic matter soil forms from (bedrock, sediments, organic deposits)
Climate affects soil formation through temperature and precipitation patterns
Influences weathering rates
Impacts chemical reactions in soil
Topography impacts soil formation by affecting:
Drainage
Erosion
Deposition processes
Organisms contribute to soil formation through:
Decomposition
Nutrient cycling
Physical alteration of soil structure
Includes both macro and microorganisms (earthworms, bacteria )
Time plays crucial role in soil development
Older soils generally exhibit more developed profiles and characteristics
Can take thousands of years for mature soil profiles to form
Parent Material and Climate Influences
Parent material determines initial soil composition and texture
Igneous rocks (granite) produce coarse-textured soils
Sedimentary rocks (limestone) create fine-textured soils
Climate strongly influences rate of weathering and soil formation
Warm, humid climates accelerate chemical weathering (tropical regions)
Cold, dry climates slow soil formation processes (arctic tundra)
Precipitation affects leaching and mineral translocation
High rainfall leads to more nutrient leaching and acidic soils
Low rainfall results in less leaching and potentially alkaline soils
Temperature impacts organic matter decomposition rates
Higher temperatures increase microbial activity and organic matter breakdown
Lower temperatures preserve organic matter, leading to accumulation (peat bogs)
Topography, Organisms, and Time Effects
Slope angle influences soil depth and erosion rates
Steep slopes have thinner soils due to increased erosion
Gentle slopes allow for deeper soil development
Aspect affects soil moisture and temperature regimes
North-facing slopes in Northern Hemisphere tend to be cooler and moister
South-facing slopes receive more direct sunlight, often warmer and drier
Vegetation types shape soil characteristics
Forests contribute more organic matter to soil surface (leaf litter)
Grasslands develop deep, organic-rich topsoil layers
Soil fauna impact soil structure and nutrient cycling
Earthworms improve soil aeration and mixing
Termites in tropical soils create complex tunnel systems
Time allows for development of distinct soil horizons
Young soils (alluvial deposits) may lack clear horizon differentiation
Ancient soils (parts of Australia) can have highly weathered, deep profiles
Weathering's Role in Soil
Physical Weathering Processes
Physical weathering breaks down rocks without changing chemical composition
Temperature fluctuations cause thermal expansion and contraction
Leads to rock fracturing and exfoliation
Frost action in cold climates breaks apart rocks
Water expands when freezing, widening cracks
Plant root growth exerts pressure on rocks
Roots penetrate cracks and gradually widen them
Abrasion by wind-blown particles or moving water erodes rock surfaces
Salt crystallization in arid environments can fracture rocks
Salt wedging occurs as salts expand in rock pores
Chemical and Biological Weathering
Chemical weathering alters rock composition through various reactions
Hydrolysis breaks down minerals in presence of water
Feldspar in granite decomposes to form clay minerals
Oxidation occurs when minerals react with oxygen
Iron-bearing minerals rust, weakening rock structure
Carbonation dissolves carbonate rocks
Limestone dissolves in carbonic acid formed by CO2 in rainwater
Biological weathering involves living organisms
Lichens secrete acids that dissolve rock surfaces
Bacteria accelerate mineral breakdown through metabolic processes
Plant roots release organic acids that enhance chemical weathering
Burrowing animals expose fresh rock surfaces to weathering agents
Weathering Factors and Soil Development
Climate strongly influences weathering intensity
Tropical climates promote rapid chemical weathering
Arid climates favor physical weathering processes
Rock type affects susceptibility to different weathering processes
Granite resists chemical weathering but is vulnerable to physical processes
Limestone easily dissolves through chemical weathering
Topography impacts exposure to weathering agents
Steep slopes experience more intense physical weathering
Depressions may accumulate water, enhancing chemical weathering
Weathering produces smaller particles incorporated into developing soil
Sand-sized particles result from physical weathering of quartz
Clay minerals form through chemical weathering of feldspars
Weathering releases nutrients essential for plant growth
Potassium from feldspar weathering
Calcium and magnesium from carbonate rock dissolution
Rate of weathering influences soil texture and fertility
Rapid weathering in tropics can lead to nutrient-poor, clay-rich soils
Slow weathering in temperate regions often results in fertile loam soils
Soil Profiles and Horizons
Major Soil Horizons
Soil profile reveals distinct layers called horizons from surface to bedrock
O horizon forms topmost layer
Consists primarily of organic matter from plant and animal residues
Commonly found in forest soils, may be absent in grasslands
A horizon , or topsoil, lies below O horizon
Rich in organic matter
Zone of maximum biological activity and nutrient cycling
Often dark in color due to humus content
E horizon , when present, occurs below A horizon
Zone of maximum leaching
Light-colored due to loss of clay, iron, and aluminum compounds
B horizon , or subsoil, characterized by accumulation
Receives clay, iron oxides, and other materials leached from upper horizons
Often reddish or yellowish due to iron oxide accumulation
C horizon consists of partially weathered parent material
Transition between soil and bedrock
Retains some characteristics of original parent material
R horizon represents underlying bedrock
Unweathered parent material from which soil has developed
Horizon Development and Characteristics
Horizon formation results from soil-forming processes over time
A horizon development:
Organic matter accumulation from plant roots and leaf litter
Mixing by soil organisms (bioturbation )
Typically has granular or crumb structure
E horizon formation:
Intense leaching in humid climates
Common in forest soils, particularly under coniferous vegetation
May be absent in young or dry soils
B horizon characteristics:
Clay accumulation creates blocky or prismatic structure
Iron oxide coatings give distinct color (rubification)
May contain lime accumulations in arid climates (calcic horizon)
C horizon features:
Lacks soil structure found in upper horizons
May contain rock fragments or saprolite (chemically weathered bedrock)
Horizon boundaries vary in distinctness and shape
Abrupt boundaries indicate rapid changes in soil properties
Gradual boundaries suggest more uniform soil development
Horizon thickness varies with soil age and formation factors
Young soils may have thin or absent B horizons
Mature soils in stable landscapes can have very thick B horizons
Special Horizon Types and Variations
Buried horizons indicate past soil surfaces covered by new material
Denoted by adding "b" to horizon symbol (Ab, Bb)
Common in alluvial or volcanic ash deposits
Calcic horizons form in arid and semi-arid climates
Accumulation of calcium carbonate
May form a hard, cemented layer called caliche
Argillic horizons result from clay illuviation
Significant increase in clay content compared to overlying horizons
Indicates advanced soil development
Spodic horizons form in humid, acidic environments
Accumulation of organic matter, aluminum, and iron compounds
Typical of Spodosols in coniferous forests
Fragipans are dense, brittle subsurface layers
Restrict root growth and water movement
Common in some temperate region soils
Plinthite forms in tropical and subtropical soils
Iron-rich, humus-poor mixture that hardens irreversibly when exposed
Indicator of seasonal waterlogging and intense weathering
Additions and Losses
Additions to soil profile enhance soil volume and nutrient content
Organic matter accumulation from plant and animal residues
Atmospheric deposition of dust and dissolved substances in precipitation
Sediment deposition through erosion and flooding (alluvial soils)
Losses from soil profile reduce soil volume or alter composition
Leaching removes soluble materials, moving them to lower horizons or groundwater
Erosion by wind or water removes surface particles
Volatilization releases gaseous compounds (ammonia from fertilizers)
Balance between additions and losses influences soil development
Net accumulation leads to soil thickening over time
Net loss results in soil thinning or complete removal (badlands topography)
Translocation moves materials within soil profile without chemical change
Clay particles move downward through eluviation and illuviation
Organic matter transported by water or soil fauna
Dissolved substances move with soil water flow
Transformation alters physical and chemical properties of soil components
Organic matter decomposition by microorganisms
Mineral weathering produces secondary clay minerals
Oxidation-reduction reactions in waterlogged soils
Pedoturbation mixes soil materials through various processes
Freeze-thaw cycles in cold climates
Animal burrowing (gophers, earthworms)
Tree uprooting creates pit and mound topography
Soil structure formation involves aggregation of soil particles
Influenced by clay content, organic matter, and biological activity
Creates peds of various shapes and sizes (granular, blocky, prismatic)
Gleization occurs in waterlogged environments
Reduction of iron compounds creates characteristic gray colors
Mottling patterns form due to fluctuating water tables
Common in wetland soils and poorly drained areas
Laterization dominates in tropical environments
Intense weathering removes silica and bases
Accumulation of iron and aluminum oxides
Results in deep, red soils (Oxisols)
Podzolization occurs in cool, humid climates under acidic vegetation
Organic acids leach iron and aluminum from surface horizons
Accumulation of these elements in B horizon creates spodic horizons
Typical of coniferous forest soils
Calcification characterizes soil formation in arid and semi-arid regions
Accumulation of calcium carbonate in subsoil
Can form hardpans that impede drainage and root growth
Salinization results from salt accumulation in soil profile
Common in arid regions with high evaporation rates
Can severely limit plant growth and soil productivity
Argillation involves clay formation and movement within the soil
Weathering of primary minerals produces clay particles
Illuviation creates clay-enriched B horizons (argillic horizons)