Soil

For other uses, see Soil (disambiguation).

Soil, commonly referred to as dirt, or earth, is a mixture of organic matter, minerals, gases, liquids, and organisms that together support life of plants and soil organisms. Some scientific definitions distinguish dirt from soil by restricting the former term specifically to displaced soil.

Surface-water-gley developed in glacial till in Northern Ireland

Soil consists of a solid phase of minerals and organic matter (the soil matrix), as well as a porous phase that holds gases (the soil atmosphere) and water (the soil solution).^[1][2] Accordingly, soil is a three-state system of solids, liquids, and gases.^[3] Soil is a product of several factors: the influence of climate, relief (elevation, orientation, and slope of terrain), organisms, and the soil's parent materials (original minerals) interacting over time.^[4] It continually undergoes development by way of numerous physical, chemical and biological processes, which include weathering with associated erosion.^[5] Given its complexity and strong internal connectedness, soil ecologists regard soil as an ecosystem.^[6]

Most soils have a dry bulk density (density of soil taking into account voids when dry) between 1.1 and 1.6 g/cm³, though the soil particle density is much higher, in the range of 2.6 to 2.7 g/cm³.^[7] Little of the soil of planet Earth is older than the Pleistocene and none is older than the Cenozoic,^[8] although fossilized soils are preserved from as far back as the Archean.^[9]

Collectively the Earth's body of soil is called the pedosphere. The pedosphere interfaces with the lithosphere, the hydrosphere, the atmosphere, and the biosphere.^[10] Soil has four important functions:

• as a medium for plant growth
• as a means of water storage, supply and purification
• as a modifier of Earth's atmosphere
• as a habitat for organisms

All of these functions, in their turn, modify the soil and its properties.

Soil science has two basic branches of study: edaphology and pedology. Edaphology studies the influence of soils on living things.^[11] Pedology focuses on the formation, description (morphology), and classification of soils in their natural environment.^[12] In engineering terms, soil is included in the broader concept of regolith, which also includes other loose material that lies above the bedrock, as can be found on the Moon and other celestial objects.^[13]

Processes

Soil is a major component of the Earth's ecosystem. The world's ecosystems are impacted in far-reaching ways by the processes carried out in the soil, with effects ranging from ozone depletion and global warming to rainforest destruction and water pollution. With respect to Earth's carbon cycle, soil acts as an important carbon reservoir,^[14] and it is potentially one of the most reactive to human disturbance^[15] and climate change.^[16] As the planet warms, it has been predicted that soils will add carbon dioxide to the atmosphere due to increased biological activity at higher temperatures, a positive feedback (amplification).^[17] This prediction has, however, been questioned on consideration of more recent knowledge on soil carbon turnover.^[18]

Soil acts as an engineering medium, a habitat for soil organisms, a recycling system for nutrients and organic wastes, a regulator of water quality, a modifier of atmospheric composition, and a medium for plant growth, making it a critically important provider of ecosystem services.^[19] Since soil has a tremendous range of available niches and habitats, it contains a prominent part of the Earth's genetic diversity. A gram of soil can contain billions of organisms, belonging to thousands of species, mostly microbial and largely still unexplored.^[20][21] Soil has a mean prokaryotic density of roughly 10⁸ organisms per gram,^[22] whereas the ocean has no more than 10⁷ prokaryotic organisms per milliliter (gram) of seawater.^[23] Organic carbon held in soil is eventually returned to the atmosphere through the process of respiration carried out by heterotrophic organisms, but a substantial part is retained in the soil in the form of soil organic matter; tillage usually increases the rate of soil respiration, leading to the depletion of soil organic matter.^[24] Since plant roots need oxygen, aeration is an important characteristic of soil. This ventilation can be accomplished via networks of interconnected soil pores, which also absorb and hold rainwater making it readily available for uptake by plants. Since plants require a nearly continuous supply of water, but most regions receive sporadic rainfall, the water-holding capacity of soils is vital for plant survival.^[25]

Soils can effectively remove impurities,^[26] kill disease agents,^[27] and degrade contaminants, this latter property being called natural attenuation.^[28] Typically, soils maintain a net absorption of oxygen and methane and undergo a net release of carbon dioxide and nitrous oxide.^[29] Soils offer plants physical support, air, water, temperature moderation, nutrients, and protection from toxins.^[30] Soils provide readily available nutrients to plants and animals by converting dead organic matter into various nutrient forms.^[31]

Composition

 

A, B, and C represent the soil profile, a notation firstly coined by Vasily Dokuchaev (1846–1903), the father of pedology. Here, A is the topsoil; B is a regolith; C is a saprolite (a less-weathered regolith); the bottom-most layer represents the bedrock.

Components of a silt loam soil by percent volume

  Water (25%)

  Gases (25%)

  Sand (18%)

  Silt (18%)

  Clay (9%)

  Organic matter (5%)

A typical soil is about 50% solids (45% mineral and 5% organic matter), and 50% voids (or pores) of which half is occupied by water and half by gas.^[32] The percent soil mineral and organic content can be treated as a constant (in the short term), while the percent soil water and gas content is considered highly variable whereby a rise in one is simultaneously balanced by a reduction in the other.^[33] The pore space allows for the infiltration and movement of air and water, both of which are critical for life existing in soil.^[34] Compaction, a common problem with soils, reduces this space, preventing air and water from reaching plant roots and soil organisms.^[35]

Given sufficient time, an undifferentiated soil will evolve a soil profile which consists of two or more layers, referred to as soil horizons. These differ in one or more properties such as in their texture, structure, density, porosity, consistency, temperature, color, and reactivity.^[8] The horizons differ greatly in thickness and generally lack sharp boundaries; their development is dependent on the type of parent material, the processes that modify those parent materials, and the soil-forming factors that influence those processes. The biological influences on soil properties are strongest near the surface, though the geochemical influences on soil properties increase with depth. Mature soil profiles typically include three basic master horizons: A, B, and C. The solum normally includes the A and B horizons. The living component of the soil is largely confined to the solum, and is generally more prominent in the A horizon.^[36] It has been suggested that the pedon, a column of soil extending vertically from the surface to the underlying parent material and large enough to show the characteristics of all its horizons, could be subdivided in the humipedon (the living part, where most soil organisms are dwelling, corresponding to the humus form), the copedon (in intermediary position, where most weathering of minerals takes place) and the lithopedon (in contact with the subsoil).^[37]

The soil texture is determined by the relative proportions of the individual particles of sand, silt, and clay that make up the soil. The interaction of the individual mineral particles with organic matter, water, gases via biotic and abiotic processes causes those particles to flocculate (stick together) to form aggregates or peds.^[38] Where these aggregates can be identified, a soil can be said to be developed, and can be described further in terms of color, porosity, consistency, reaction (acidity), etc.

Water is a critical agent in soil development due to its involvement in the dissolution, precipitation, erosion, transport, and deposition of the materials of which a soil is composed.^[39] The mixture of water and dissolved or suspended materials that occupy the soil pore space is called the soil solution. Since soil water is never pure water, but contains hundreds of dissolved organic and mineral substances, it may be more accurately called the soil solution. Water is central to the dissolution, precipitation and leaching of minerals from the soil profile. Finally, water affects the type of vegetation that grows in a soil, which in turn affects the development of the soil, a complex feedback which is exemplified in the dynamics of banded vegetation patterns in semi-arid regions.^[40]

Soils supply plants with nutrients, most of which are held in place by particles of clay and organic matter (colloids)^[41] The nutrients may be adsorbed on clay mineral surfaces, bound within clay minerals (absorbed), or bound within organic compounds as part of the living organisms or dead soil organic matter. These bound nutrients interact with soil water to buffer the soil solution composition (attenuate changes in the soil solution) as soils wet up or dry out, as plants take up nutrients, as salts are leached, or as acids or alkalis are added.^[42]

Plant nutrient availability is affected by soil pH, which is a measure of the hydrogen ion activity in the soil solution. Soil pH is a function of many soil forming factors, and is generally lower (more acid) where weathering is more advanced.^[43]

Most plant nutrients, with the exception of nitrogen, originate from the minerals that make up the soil parent material. Some nitrogen originates from rain as dilute nitric acid and ammonia,^[44] but most of the nitrogen is available in soils as a result of nitrogen fixation by bacteria. Once in the soil-plant system, most nutrients are recycled through living organisms, plant and microbial residues (soil organic matter), mineral-bound forms, and the soil solution. Both living soil organisms (microbes, animals and plant roots) and soil organic matter are of critical importance to this recycling, and thereby to soil formation and soil fertility.^[45] Microbial soil enzymes may release nutrients from minerals or organic matter for use by plants and other microorganisms, sequester (incorporate) them into living cells, or cause their loss from the soil by volatilisation (loss to the atmosphere as gases) or leaching.^[46]

Formation

Main article: Soil formation

Further information: Soil mechanics § Genesis

Soil is said to be formed when organic matter has accumulated and colloids are washed downward, leaving deposits of clay, humus, iron oxide, carbonate, and gypsum, producing a distinct layer called the B horizon. This is a somewhat arbitrary definition as mixtures of sand, silt, clay and humus will support biological and agricultural activity before that time.^[47] These constituents are moved from one level to another by water and animal activity. As a result, layers (horizons) form in the soil profile. The alteration and movement of materials within a soil causes the formation of distinctive soil horizons. However, more recent definitions of soil embrace soils without any organic matter, such as those regoliths that formed on Mars^[48] and analogous conditions in planet Earth deserts.^[49]

An example of the development of a soil would begin with the weathering of lava flow bedrock, which would produce the purely mineral-based parent material from which the soil texture forms. Soil development would proceed most rapidly from bare rock of recent flows in a warm climate, under heavy and frequent rainfall. Under such conditions, plants (in a first stage nitrogen-fixing lichens and cyanobacteria then epilithic higher plants) become established very quickly on basaltic lava, even though there is very little organic material.^[50] Basaltic minerals commonly weather relatively quickly, according to the Goldich dissolution series.^[51] The plants are supported by the porous rock as it is filled with nutrient-bearing water that carries minerals dissolved from the rocks. Crevasses and pockets, local topography of the rocks, would hold fine materials and harbour plant roots. The developing plant roots are associated with mineral-weathering mycorrhizal fungi^[52] that assist in breaking up the porous lava, and by these means organic matter and a finer mineral soil accumulate with time. Such initial stages of soil development have been described on volcanoes,^[53] inselbergs,^[54] and glacial moraines.^[55]

How soil formation proceeds is influenced by at least five classic factors that are intertwined in the evolution of a soil: parent material, climate, topography (relief), organisms, and time.^[56] When reordered to climate, relief, organisms, parent material, and time, they form the acronym CROPT.^[57]

Physical properties

Main article: Physical properties of soil

For the academic discipline, see Soil physics.

The physical properties of soils, in order of decreasing importance for ecosystem services such as crop production, are texture, structure, bulk density, porosity, consistency, temperature, colour and resistivity.^[58] Soil texture is determined by the relative proportion of the three kinds of soil mineral particles, called soil separates: sand, silt, and clay. At the next larger scale, soil structures called peds or more commonly soil aggregates are created from the soil separates when iron oxides, carbonates, clay, silica and humus, coat particles and cause them to adhere into larger, relatively stable secondary structures.^[59] Soil bulk density, when determined at standardized moisture conditions, is an estimate of soil compaction.^[60] Soil porosity consists of the void part of the soil volume and is occupied by gases or water. Soil consistency is the ability of soil materials to stick together. Soil temperature and colour are self-defining. Resistivity refers to the resistance to conduction of electric currents and affects the rate of corrosion of metal and concrete structures which are buried in soil.^[61] These properties vary through the depth of a soil profile, i.e. through soil horizons. Most of these properties determine the aeration of the soil and the ability of water to infiltrate and to be held within the soil.^[62]

Soil moisture

Main article: Soil moisture

Soil water content can be measured as volume or weight. Soil moisture levels, in order of decreasing water content, are saturation, field capacity, wilting point, air dry, and oven dry. Field capacity describes a drained wet soil at the point water content reaches equilibrium with gravity. Irrigating soil above field capacity risks percolation losses. Wilting point describes the dry limit for growing plants. During growing season, soil moisture is unaffected by functional groups or specie richness.^[63]

Available water capacity is the amount of water held in a soil profile available to plants. As water content drops, plants have to work against increasing forces of adhesion and sorptivity to withdraw water. Irrigation scheduling avoids moisture stress by replenishing depleted water before stress is induced.^[64][65]

Capillary action is responsible for moving groundwater from wet regions of the soil to dry areas. Subirrigation designs (e.g., wicking beds, sub-irrigated planters) rely on capillarity to supply water to plant roots. Capillary action can result in an evaporative concentration of salts, causing land degradation through salination.

Soil moisture measurement — measuring the water content of the soil, as can be expressed in terms of volume or weight — can be based on in situ probes (e.g., capacitance probes, neutron probes), or remote sensing methods. Soil moisture measurement is an important factor in determining changes in soil activity.^[63]

Soil gas

Main article: Soil gas

The atmosphere of soil, or soil gas, is very different from the atmosphere above. The consumption of oxygen by microbes and plant roots, and their release of carbon dioxide, decreases oxygen and increases carbon dioxide concentration. Atmospheric CO₂ concentration is 0.04%, but in the soil pore space it may range from 10 to 100 times that level, thus potentially contributing to the inhibition of root respiration.^[66] Calcareous soils regulate CO₂ concentration by carbonate buffering, contrary to acid soils in which all CO₂ respired accumulates in the soil pore system.^[67] At extreme levels, CO₂ is toxic.^[68] This suggests a possible negative feedback control of soil CO₂ concentration through its inhibitory effects on root and microbial respiration (also called soil respiration).^[69] In addition, the soil voids are saturated with water vapour, at least until the point of maximal hygroscopicity, beyond which a vapour-pressure deficit occurs in the soil pore space.^[34] Adequate porosity is necessary, not just to allow the penetration of water, but also to allow gases to diffuse in and out. Movement of gases is by diffusion from high concentrations to lower, the diffusion coefficient decreasing with soil compaction.^[70] Oxygen from above atmosphere diffuses in the soil where it is consumed and levels of carbon dioxide in excess of above atmosphere diffuse out with other gases (including greenhouse gases) as well as water.^[71] Soil texture and structure strongly affect soil porosity and gas diffusion. It is the total pore space (porosity) of soil, not the pore size, and the degree of pore interconnection (or conversely pore sealing), together with water content, air turbulence and temperature, that determine the rate of diffusion of gases into and out of soil.^[72][71] Platy soil structure and soil compaction (low porosity) impede gas flow, and a deficiency of oxygen may encourage anaerobic bacteria to reduce (strip oxygen) from nitrate NO₃ to the gases N₂, N₂O, and NO, which are then lost to the atmosphere, thereby depleting the soil of nitrogen, a detrimental process called denitrification.^[73] Aerated soil is also a net sink of methane (CH₄)^[74] but a net producer of methane (a strong heat-absorbing greenhouse gas) when soils are depleted of oxygen and subject to elevated temperatures.^[75]

Soil atmosphere is also the seat of emissions of volatiles other than carbon and nitrogen oxides from various soil organisms, e.g. roots,^[76] bacteria,^[77] fungi,^[78] animals.^[79] These volatiles are used as chemical cues, making soil atmosphere the seat of interaction networks^[80][81] playing a decisive role in the stability, dynamics and evolution of soil ecosystems.^[82] Biogenic soil volatile organic compounds are exchanged with the aboveground atmosphere, in which they are just 1–2 orders of magnitude lower than those from aboveground vegetation.^[83]

Humans can get some idea of the soil atmosphere through the well-known 'after-the-rain' scent, when infiltering rainwater flushes out the whole soil atmosphere after a drought period, or when soil is excavated,^[84] a bulk property attributed in a reductionist manner to particular biochemical compounds such as petrichor or geosmin.

Solid phase (soil matrix)

Main article: Soil matrix

Soil particles can be classified by their chemical composition (mineralogy) as well as their size. The particle size distribution of a soil, its texture, determines many of the properties of that soil, in particular hydraulic conductivity and water potential,^[85] but the mineralogy of those particles can strongly modify those properties. The mineralogy of the finest soil particles, clay, is especially important.^[86]

Chemistry

For the academic discipline, see Soil chemistry.

The chemistry of a soil determines its ability to supply available plant nutrients and affects its physical properties and the health of its living population. In addition, a soil's chemistry also determines its corrosivity, stability, and ability to absorb pollutants and to filter water. It is the surface chemistry of mineral and organic colloids that determines soil's chemical properties.^[87] A colloid is a small, insoluble particle ranging in size from 1 nanometer to 1 micrometer, thus small enough to remain suspended by Brownian motion in a fluid medium without settling.^[88] Most soils contain organic colloidal particles called humus as well as the inorganic colloidal particles of clays. The very high specific surface area of colloids and their net electrical charges give soil its ability to hold and release ions. Negatively charged sites on colloids attract and release cations in what is referred to as cation exchange. Cation-exchange capacity is the amount of exchangeable cations per unit weight of dry soil and is expressed in terms of milliequivalents of positively charged ions per 100 grams of soil (or centimoles of positive charge per kilogram of soil; cmol_c/kg). Similarly, positively charged sites on colloids can attract and release anions in the soil, giving the soil anion exchange capacity.

Cation and anion exchange

Further information: Cation-exchange capacity

The cation exchange, that takes place between colloids and soil water, buffers (moderates) soil pH, alters soil structure, and purifies percolating water by adsorbing cations of all types, both useful and harmful.

The negative or positive charges on colloid particles make them able to hold cations or anions, respectively, to their surfaces. The charges result from four sources.^[89]

1. Isomorphous substitution occurs in clay during its formation, when lower-valence cations substitute for higher-valence cations in the crystal structure.^[90] Substitutions in the outermost layers are more effective than for the innermost layers, as the electric charge strength drops off as the square of the distance. The net result is oxygen atoms with net negative charge and the ability to attract cations.
2. Edge-of-clay oxygen atoms are not in balance ionically as the tetrahedral and octahedral structures are incomplete.^[91]
3. Hydroxyls may substitute for oxygens of the silica layers, a process called hydroxylation. When the hydrogens of the clay hydroxyls are ionised into solution, they leave the oxygen with a negative charge (anionic clays).^[92]
4. Hydrogens of humus hydroxyl groups may also be ionised into solution, leaving, similarly to clay, an oxygen with a negative charge.^[93]

Cations held to the negatively charged colloids resist being washed downward by water and are out of reach of plant roots, thereby preserving the soil fertility in areas of moderate rainfall and low temperatures.^[94][95]

There is a hierarchy in the process of cation exchange on colloids, as cations differ in the strength of adsorption by the colloid and hence their ability to replace one another (ion exchange). If present in equal amounts in the soil water solution:

Al³⁺ replaces H⁺ replaces Ca²⁺ replaces Mg²⁺ replaces K⁺ same as NH⁺
₄ replaces Na^+[96]

If one cation is added in large amounts, it may replace the others by the sheer force of its numbers. This is called law of mass action. This is largely what occurs with the addition of cationic fertilisers (potash, lime).^[97]

As the soil solution becomes more acidic (low pH, meaning an abundance of H⁺), the other cations more weakly bound to colloids are pushed into solution as hydrogen ions occupy exchange sites (protonation). A low pH may cause the hydrogen of hydroxyl groups to be pulled into solution, leaving charged sites on the colloid available to be occupied by other cations. This ionisation of hydroxy groups on the surface of soil colloids creates what is described as pH-dependent surface charges.^[98] Unlike permanent charges developed by isomorphous substitution, pH-dependent charges are variable and increase with increasing pH.^[99] Freed cations can be made available to plants but are also prone to be leached from the soil, possibly making the soil less fertile.^[100] Plants are able to excrete H⁺ into the soil through the synthesis of organic acids and by that means, change the pH of the soil near the root and push cations off the colloids, thus making those available to the plant.^[101]

Cation exchange capacity (CEC)

Cation exchange capacity is the soil's ability to remove cations from the soil water solution and sequester those to be exchanged later as the plant roots release hydrogen ions to the solution.^[102] CEC is the amount of exchangeable hydrogen cation (H⁺) that will combine with 100 grams dry weight of soil and whose measure is one milliequivalents per 100 grams of soil (1 meq/100 g). Hydrogen ions have a single charge and one-thousandth of a gram of hydrogen ions per 100 grams dry soil gives a measure of one milliequivalent of hydrogen ion. Calcium, with an atomic weight 40 times that of hydrogen and with a valence of two, converts to (40 ÷ 2) × 1 milliequivalent = 20 milliequivalents of hydrogen ion per 100 grams of dry soil or 20 meq/100 g.^[103] The modern measure of CEC is expressed as centimoles of positive charge per kilogram (cmol/kg) of oven-dry soil.

Most of the soil's CEC occurs on clay and humus colloids, and the lack of those in hot, humid, wet climates (such as tropical rainforests), due to leaching and decomposition, respectively, explains the apparent sterility of tropical soils.^[104] Live plant roots also have some CEC, linked to their specific surface area.^[105]

Cation exchange capacity for soils; soil textures; soil colloids^[106]

Soil	State	CEC meq/100 g
Charlotte fine sand	Florida	1.0
Ruston fine sandy loam	Texas	1.9
Glouchester loam	New Jersey	11.9
Grundy silt loam	Illinois	26.3
Gleason clay loam	California	31.6
Susquehanna clay loam	Alabama	34.3
Davie mucky fine sand	Florida	100.8
Sands	—	1–5
Fine sandy loams	—	5–10
Loams and silt loams	—	5–15
Clay loams	—	15–30
Clays	—	over 30
Sesquioxides	—	0–3
Kaolinite	—	3–15
Illite	—	25–40
Montmorillonite	—	60–100
Vermiculite (similar to illite)	—	80–150
Humus	—	100–300

Anion exchange capacity (AEC)

Anion exchange capacity is the soil's ability to remove anions (such as nitrate, phosphate) from the soil water solution and sequester those for later exchange as the plant roots release carbonate anions to the soil water solution.^[107] Those colloids which have low CEC tend to have some AEC. Amorphous and sesquioxide clays have the highest AEC,^[108] followed by the iron oxides.^[109] Levels of AEC are much lower than for CEC, because of the generally higher rate of positively (versus negatively) charged surfaces on soil colloids, to the exception of variable-charge soils.^[110] Phosphates tend to be held at anion exchange sites.^[111]

Iron and aluminum hydroxide clays are able to exchange their hydroxide anions (OH⁻) for other anions.^[107] The order reflecting the strength of anion adhesion is as follows:

H
₂PO⁻
₄ replaces SO²⁻
₄ replaces NO⁻
₃ replaces Cl⁻

The amount of exchangeable anions is of a magnitude of tenths to a few milliequivalents per 100 g dry soil.^[106] As pH rises, there are relatively more hydroxyls, which will displace anions from the colloids and force them into solution and out of storage; hence AEC decreases with increasing pH (alkalinity).^[112]

Reactivity (pH)

Main articles: Soil pH and Soil pH § Effect of soil pH on plant growth

Soil reactivity is expressed in terms of pH and is a measure of the acidity or alkalinity of the soil. More precisely, it is a measure of hydronium concentration in an aqueous solution and ranges in values from 0 to 14 (acidic to basic) but practically speaking for soils, pH ranges from 3.5 to 9.5, as pH values beyond those extremes are toxic to life forms.^[113]

At 25 °C an aqueous solution that has a pH of 3.5 has 10^−3.5 moles H₃O⁺ (hydronium ions) per litre of solution (and also 10^−10.5 moles per litre OH⁻). A pH of 7, defined as neutral, has 10⁻⁷ moles of hydronium ions per litre of solution and also 10⁻⁷ moles of OH⁻ per litre; since the two concentrations are equal, they are said to neutralise each other. A pH of 9.5 has 10^−9.5 moles hydronium ions per litre of solution (and also 10^−2.5 moles per litre OH⁻). A pH of 3.5 has one million times more hydronium ions per litre than a solution with pH of 9.5 (9.5 − 3.5 = 6 or 10⁶) and is more acidic.^[114]

The effect of pH on a soil is to remove from the soil or to make available certain ions. Soils with high acidity tend to have toxic amounts of aluminium and manganese.^[115] As a result of a trade-off between toxicity and requirement most nutrients are better available to plants at moderate pH,^[116] although most minerals are more soluble in acid soils. Soil organisms are hindered by high acidity, and most agricultural crops do best with mineral soils of pH 6.5 and organic soils of pH 5.5.^[117] Given that at low pH toxic metals (e.g. cadmium, zinc, lead) are positively charged as cations and organic pollutants are in non-ionic form, thus both made more available to organisms,^[118][119] it has been suggested that plants, animals and microbes commonly living in acid soils are pre-adapted to every kind of pollution, whether of natural or human origin.^[120]

In high rainfall areas, soils tend to acidify as the basic cations are forced off the soil colloids by the mass action of hydronium ions from usual or unusual rain acidity against those attached to the colloids. High rainfall rates can then wash the nutrients out, leaving the soil inhabited only by those organisms which are particularly efficient to uptake nutrients in very acid conditions, like in tropical rainforests.^[121] Once the colloids are saturated with H₃O⁺, the addition of any more hydronium ions or aluminum hydroxyl cations drives the pH even lower (more acidic) as the soil has been left with no buffering capacity.^[122] In areas of extreme rainfall and high temperatures, the clay and humus may be washed out, further reducing the buffering capacity of the soil.^[123] In low rainfall areas, unleached calcium pushes pH to 8.5 and with the addition of exchangeable sodium, soils may reach pH 10.^[124] Beyond a pH of 9, plant growth is reduced.^[125] High pH results in low micro-nutrient mobility, but water-soluble chelates of those nutrients can correct the deficit.^[126] Sodium can be reduced by the addition of gypsum (calcium sulphate) as calcium adheres to clay more tightly than does sodium causing sodium to be pushed into the soil water solution where it can be washed out by an abundance of water.^[127][128]

Base saturation percentage

There are acid-forming cations (e.g. hydronium, aluminium, iron) and there are base-forming cations (e.g. calcium, magnesium, sodium). The fraction of the negatively-charged soil colloid exchange sites (CEC) that are occupied by base-forming cations is called base saturation. If a soil has a CEC of 20 meq and 5 meq are aluminium and hydronium cations (acid-forming), the remainder of positions on the colloids (20 − 5 = 15 meq) are assumed occupied by base-forming cations, so that the base saturation is 15 ÷ 20 × 100% = 75% (the compliment 25% is assumed acid-forming cations). Base saturation is almost in direct proportion to pH (it increases with increasing pH).^[129] It is of use in calculating the amount of lime needed to neutralise an acid soil (lime requirement). The amount of lime needed to neutralize a soil must take account of the amount of acid forming ions on the colloids (exchangeable acidity), not just those in the soil water solution (free acidity).^[130] The addition of enough lime to neutralize the soil water solution will be insufficient to change the pH, as the acid forming cations stored on the soil colloids will tend to restore the original pH condition as they are pushed off those colloids by the calcium of the added lime.^[131]

Buffering

Further information: Soil conditioner

The resistance of soil to change in pH, as a result of the addition of acid or basic material, is a measure of the buffering capacity of a soil and (for a particular soil type) increases as the CEC increases. Hence, pure sand has almost no buffering ability, though soils high in colloids (whether mineral or organic) have high buffering capacity.^[132] Buffering occurs by cation exchange and neutralisation. However, colloids are not the only regulators of soil pH. The role of carbonates should be underlined, too.^[133] More generally, according to pH levels, several buffer systems take precedence over each other, from calcium carbonate buffer range to iron buffer range.^[134]

The addition of a small amount of highly basic aqueous ammonia to a soil will cause the ammonium to displace hydronium ions from the colloids, and the end product is water and colloidally fixed ammonium, but little permanent change overall in soil pH.

The addition of a small amount of lime, Ca(OH)₂, will displace hydronium ions from the soil colloids, causing the fixation of calcium to colloids and the evolution of CO₂ and water, with little permanent change in soil pH.

The above are examples of the buffering of soil pH. The general principal is that an increase in a particular cation in the soil water solution will cause that cation to be fixed to colloids (buffered) and a decrease in solution of that cation will cause it to be withdrawn from the colloid and moved into solution (buffered). The degree of buffering is often related to the CEC of the soil; the greater the CEC, the greater the buffering capacity of the soil.^[135]

Redox

Main article: Redox § Redox_reactions_in_soils

See also: Table of standard reduction potentials for half-reactions important in biochemistry

Soil chemical reactions involve some combination of proton and electron transfer. Oxidation occurs if there is a loss of electrons in the transfer process while reduction occurs if there is a gain of electrons. Reduction potential is measured in volts or millivolts. Soil microbial communities develop along electron transport chains, forming electrically conductive biofilms, and developing networks of bacterial nanowires.

Redox factors in soil development, where formation of redoximorphic color features provides critical information for soil interpretation. Understanding the redox gradient is important to managing carbon sequestration, bioremediation, wetland delineation, and soil-based microbial fuel cells.

Nutrients

Plant nutrients, their chemical symbols, and the ionic forms common in soils and available for plant uptake^[136]

Element	Symbol	Ion or molecule
Carbon	C	CO2 (mostly through leaves)
Hydrogen	H	H^+, H2O (water)
Oxygen	O	O^2−, OH^−, CO^2− 3, SO^2− 4, CO2
Phosphorus	P	H 2PO^− 4, HPO^2− 4 (phosphates)
Potassium	K	K^+
Nitrogen	N	NH^+ 4, NO^− 3 (ammonium, nitrate)
Sulfur	S	SO^2− 4
Calcium	Ca	Ca^2+
Iron	Fe	Fe^2+, Fe^3+ (ferrous, ferric)
Magnesium	Mg	Mg^2+
Boron	B	H3BO3, H 2BO^− 3, B(OH)^− 4
Manganese	Mn	Mn^2+
Copper	Cu	Cu^2+
Zinc	Zn	Zn^2+
Molybdenum	Mo	MoO^2− 4 (molybdate)
Chlorine	Cl	Cl^− (chloride)

Main articles: Plant nutrients in soil, Plant nutrition, and Soil pH § Effect of soil pH on plant growth

Seventeen elements or nutrients are essential for plant growth and reproduction. They are carbon (C), hydrogen (H), oxygen (O), nitrogen (N), phosphorus (P), potassium (K), sulfur (S), calcium (Ca), magnesium (Mg), iron (Fe), boron (B), manganese (Mn), copper (Cu), zinc (Zn), molybdenum (Mo), nickel (Ni) and chlorine (Cl).^{[137][138][139]} Nutrients required for plants to complete their life cycle are considered essential nutrients. Nutrients that enhance the growth of plants but are not necessary to complete the plant's life cycle are considered non-essential. With the exception of carbon, hydrogen and oxygen, which are supplied by carbon dioxide and water, and nitrogen, provided through nitrogen fixation,^[139] the nutrients derive originally from the mineral component of the soil. The Law of the Minimum expresses that when the available form of a nutrient is not in enough proportion in the soil solution, then other nutrients cannot be taken up at an optimum rate by a plant.^[140] A particular nutrient ratio of the soil solution is thus mandatory for optimizing plant growth, a value which might differ from nutrient ratios calculated from plant composition.^[141]

Plant uptake of nutrients can only proceed when they are present in a plant-available form. In most situations, nutrients are absorbed in an ionic form from (or together with) soil water. Although minerals are the origin of most nutrients, and the bulk of most nutrient elements in the soil is held in crystalline form within primary and secondary minerals, they weather too slowly to support rapid plant growth. For example, the application of finely ground minerals, feldspar and apatite, to soil seldom provides the necessary amounts of potassium and phosphorus at a rate sufficient for good plant growth, as most of the nutrients remain bound in the crystals of those minerals.^[142]

The nutrients adsorbed onto the surfaces of clay colloids and soil organic matter provide a more accessible reservoir of many plant nutrients (e.g. K, Ca, Mg, P, Zn). As plants absorb the nutrients from the soil water, the soluble pool is replenished from the surface-bound pool. The decomposition of soil organic matter by microorganisms is another mechanism whereby the soluble pool of nutrients is replenished – this is important for the supply of plant-available N, S, P, and B from soil.^[143]

Gram for gram, the capacity of humus to hold nutrients and water is far greater than that of clay minerals, most of the soil cation exchange capacity arising from charged carboxylic groups on organic matter.^[144] However, despite the great capacity of humus to retain water once water-soaked, its high hydrophobicity decreases its wettability.^[145] All in all, small amounts of humus may remarkably increase the soil's capacity to promote plant growth.^[146][143]

Soil organic matter

Main article: Soil organic matter

The organic material in soil is made up of organic compounds and includes plant, animal and microbial material, both living and dead. A typical soil has a biomass composition of 70% microorganisms, 22% macrofauna, and 8% roots. The living component of an acre of soil may include 900 lb of earthworms, 2400 lb of fungi, 1500 lb of bacteria, 133 lb of protozoa and 890 lb of arthropods and algae.^[147]

A few percent of the soil organic matter, with small residence time, consists of the microbial biomass and metabolites of bacteria, molds, and actinomycetes that work to break down the dead organic matter.^[148][149] Were it not for the action of these micro-organisms, the entire carbon dioxide part of the atmosphere would be sequestered as organic matter in the soil. However, in the same time soil microbes contribute to carbon sequestration in the topsoil through the formation of stable humus.^[150] In the aim to sequester more carbon in the soil for alleviating the greenhouse effect it would be more efficient in the long-term to stimulate humification than to decrease litter decomposition.^[151]

The main part of soil organic matter is a complex assemblage of small organic molecules, collectively called humus or humic substances. The use of these terms, which do not rely on a clear chemical classification, has been considered as obsolete.^[152] Other studies showed that the classical notion of molecule is not convenient for humus, which escaped most attempts done over two centuries to resolve it in unit components, but still is chemically distinct from polysaccharides, lignins and proteins.^[153]

Most living things in soils, including plants, animals, bacteria, and fungi, are dependent on organic matter for nutrients and/or energy. Soils have organic compounds in varying degrees of decomposition which rate is dependent on temperature, soil moisture, and aeration. Bacteria and fungi feed on the raw organic matter, which are fed upon by protozoa, which in turn are fed upon by nematodes, annelids and arthropods, themselves able to consume and transform raw or humified organic matter. This has been called the soil food web, through which all organic matter is processed as in a digestive system.^[154] Organic matter holds soils open, allowing the infiltration of air and water, and may hold as much as twice its weight in water. Many soils, including desert and rocky-gravel soils, have little or no organic matter. Soils that are all organic matter, such as peat (histosols), are infertile.^[155] In its earliest stage of decomposition, the original organic material is often called raw organic matter. The final stage of decomposition is called humus.

In grassland, much of the organic matter added to the soil is from the deep, fibrous, grass root systems. By contrast, tree leaves falling on the forest floor are the principal source of soil organic matter in the forest. Another difference is the frequent occurrence in the grasslands of fires that destroy large amounts of aboveground material but stimulate even greater contributions from roots. Also, the much greater acidity under any forests inhibits the action of certain soil organisms that otherwise would mix much of the surface litter into the mineral soil. As a result, the soils under grasslands generally develop a thicker A horizon with a deeper distribution of organic matter than in comparable soils under forests, which characteristically store most of their organic matter in the forest floor (O horizon) and thin A horizon.^[156]

Humus

Humus refers to organic matter that has been decomposed by soil microflora and fauna to the point where it is resistant to further breakdown. Humus usually constitutes only five percent of the soil or less by volume, but it is an essential source of nutrients and adds important textural qualities crucial to soil health and plant growth.^[157] Humus also feeds arthropods, termites and earthworms which further improve the soil.^[158] The end product, humus, is suspended in colloidal form in the soil solution and forms a weak acid that can attack silicate minerals by chelating their iron and aluminum atoms.^[159] Humus has a high cation and anion exchange capacity that on a dry weight basis is many times greater than that of clay colloids. It also acts as a buffer, like clay, against changes in pH and soil moisture.^[160]

Humic acids and fulvic acids, which begin as raw organic matter, are important constituents of humus. After the death of plants, animals, and microbes, microbes begin to feed on the residues through their production of extra-cellular soil enzymes, resulting finally in the formation of humus.^[161] As the residues break down, only molecules made of aliphatic and aromatic hydrocarbons, assembled and stabilized by oxygen and hydrogen bonds, remain in the form of complex molecular assemblages collectively called humus.^[153] Humus is never pure in the soil, because it reacts with metals and clays to form complexes which further contribute to its stability and to soil structure.^[160] Although the structure of humus has in itself few nutrients (with the exception of constitutive metals such as calcium, iron and aluminum) it is able to attract and link, by weak bonds, cation and anion nutrients that can further be released into the soil solution in response to selective root uptake and changes in soil pH, a process of paramount importance for the maintenance of fertility in tropical soils.^[162]

Lignin is resistant to breakdown and accumulates within the soil. It also reacts with proteins,^[163] which further increases its resistance to decomposition, including enzymatic decomposition by microbes.^[164] Fats and waxes from plant matter have still more resistance to decomposition and persist in soils for thousand years, hence their use as tracers of past vegetation in buried soil layers.^[165] Clay soils often have higher organic contents that persist longer than soils without clay as the organic molecules adhere to and are stabilised by the clay.^[166] Proteins normally decompose readily, to the exception of scleroproteins, but when bound to clay particles they become more resistant to decomposition.^[167] As for other proteins clay particles absorb the enzymes exuded by microbes, decreasing enzyme activity while protecting extracellular enzymes from degradation.^[168] The addition of organic matter to clay soils can render that organic matter and any added nutrients inaccessible to plants and microbes for many years.^[169] A study showed increased soil fertility following the addition of mature compost to a clay soil.^[170] High soil tannin content can cause nitrogen to be sequestered as resistant tannin-protein complexes.^[171][172]

Humus formation is a process dependent on the amount of plant material added each year and the type of base soil. Both are affected by climate and the type of organisms present.^[156] Soils with humus can vary in nitrogen content but typically have 3 to 6 percent nitrogen. Raw organic matter, as a reserve of nitrogen and phosphorus, is a vital component affecting soil fertility.^[155] Humus also absorbs water, and expands and shrinks between dry and wet states to a higher extent than clay, increasing soil porosity.^[173] Humus is less stable than the soil's mineral constituents, as it is reduced by microbial decomposition, and over time its concentration diminishes without the addition of new organic matter. However, humus in its most stable forms may persist over centuries if not millennia.^[174] Charcoal is a source of highly stable humus, called black carbon,^[175] which had been used traditionally to improve the fertility of nutrient-poor tropical soils. This very ancient practice, as ascertained in the genesis of Amazonian dark earths, has been renewed and became popular under the name of biochar. It has been suggested that biochar could be used to sequester more carbon in the fight against the greenhouse effect.^[176]

Climatological influence

The production, accumulation and degradation of organic matter are greatly dependent on climate. For example, when a thawing event occurs, the flux of soil gases with atmospheric gases is significantly influenced.^[177] Temperature, soil moisture and topography are the major factors affecting the accumulation of organic matter in soils. Organic matter tends to accumulate under wet or cold conditions where decomposer activity is impeded by low temperature^[178] or excess moisture which results in anaerobic conditions.^[179] Conversely, excessive rain and high temperatures of tropical climates enables rapid decomposition of organic matter and leaching of plant nutrients. Forest ecosystems on these soils rely on efficient recycling of nutrients and plant matter by the living plant and microbial biomass to maintain their productivity, a process which is disturbed by human activities.^[180] Excessive slope, in particular in the presence of cultivation for the sake of agriculture, may encourage the erosion of the top layer of soil which holds most of the raw organic material that would otherwise eventually become humus.^[181]

Plant residue

Typical types and percentages of plant residue components

  Cellulose (45%)

  Lignin (20%)

  Hemicellulose (18%)

  Protein (8%)

  Sugars and starches (5%)

  Fats and waxes (2%)

Cellulose and hemicellulose undergo fast decomposition by fungi and bacteria, with a half-life of 12–18 days in a temperate climate.^[182] Brown rot fungi can decompose the cellulose and hemicellulose, leaving the lignin and phenolic compounds behind. Starch, which is an energy storage system for plants, undergoes fast decomposition by bacteria and fungi. Lignin consists of polymers composed of 500 to 600 units with a highly branched, amorphous structure, linked to cellulose, hemicellulose and pectin in plant cell walls. Lignin undergoes very slow decomposition, mainly by white rot fungi and actinomycetes; its half-life under temperate conditions is about six months.^[182]

Horizons

Main article: Soil horizon

A horizontal layer of the soil, whose physical features, composition and age are distinct from those above and beneath, is referred to as a soil horizon. The naming of a horizon is based on the type of material of which it is composed. Those materials reflect the duration of specific processes of soil formation. They are labelled using a shorthand notation of letters and numbers which describe the horizon in terms of its colour, size, texture, structure, consistency, root quantity, pH, voids, boundary characteristics and presence of nodules or concretions.^[183] No soil profile has all the major horizons. Some, called entisols, may have only one horizon or are currently considered as having no horizon, in particular incipient soils from unreclaimed mining waste deposits,^[184] moraines,^[185] volcanic cones^[186] sand dunes or alluvial terraces.^[187] Upper soil horizons may be lacking in truncated soils following wind or water ablation, with concomitant downslope burying of soil horizons, a natural process aggravated by agricultural practices such as tillage.^[188] The growth of trees is another source of disturbance, creating a micro-scale heterogeneity which is still visible in soil horizons once trees have died.^[189] By passing from a horizon to another, from the top to the bottom of the soil profile, one goes back in time, with past events registered in soil horizons like in sediment layers. Sampling pollen, testate amoebae and plant remains in soil horizons may help to reveal environmental changes (e.g. climate change, land use change) which occurred in the course of soil formation.^[190] Soil horizons can be dated by several methods such as radiocarbon, using pieces of charcoal provided they are of enough size to escape pedoturbation by earthworm activity and other mechanical disturbances.^[191] Fossil soil horizons from paleosols can be found within sedimentary rock sequences, allowing the study of past environments.^[192]

The exposure of parent material to favourable conditions produces mineral soils that are marginally suitable for plant growth, as is the case in eroded soils.^[193] The growth of vegetation results in the production of organic residues which fall on the ground as litter for plant aerial parts (leaf litter) or are directly produced belowground for subterranean plant organs (root litter), and then release dissolved organic matter.^[194] The remaining surficial organic layer, called the O horizon, produces a more active soil due to the effect of the organisms that live within it. Organisms colonise and break down organic materials, making available nutrients upon which other plants and animals can live.^[195] After sufficient time, humus moves downward and is deposited in a distinctive organic-mineral surface layer called the A horizon, in which organic matter is mixed with mineral matter through the activity of burrowing animals, a process called pedoturbation. This natural process does not go to completion in the presence of conditions detrimental to soil life such as strong acidity, cold climate or pollution, stemming in the accumulation of undecomposed organic matter within a single organic horizon overlying the mineral soil^[196] and in the juxtaposition of humified organic matter and mineral particles, without intimate mixing, in the underlying mineral horizons.^[197]

Classification

Main article: Soil classification

One of the first soil classification systems was developed by Russian scientist Vasily Dokuchaev around 1880.^[198] It was modified a number of times by American and European researchers and was developed into the system commonly used until the 1960s. It was based on the idea that soils have a particular morphology based on the materials and factors that form them. In the 1960s, a different classification system began to emerge which focused on soil morphology instead of parental materials and soil-forming factors. Since then, it has undergone further modifications. The World Reference Base for Soil Resources^[199] aims to establish an international reference base for soil classification.

Uses

Soil is used in agriculture, where it serves as the anchor and primary nutrient base for plants. The types of soil and available moisture determine the species of plants that can be cultivated. Agricultural soil science was the primeval domain of soil knowledge, long time before the advent of pedology in the 19th century. However, as demonstrated by aeroponics, aquaponics and hydroponics, soil material is not an absolute essential for agriculture, and soilless cropping systems have been claimed as the future of agriculture for an endless growing mankind.^[200]

Soil material is also a critical component in mining, construction and landscape development industries.^[201] Soil serves as a foundation for most construction projects. The movement of massive volumes of soil can be involved in surface mining, road building and dam construction. Earth sheltering is the architectural practice of using soil for external thermal mass against building walls. Many building materials are soil based. Loss of soil through urbanization is growing at a high rate in many areas and can be critical for the maintenance of subsistence agriculture.^[202]

Soil resources are critical to the environment, as well as to food and fibre production, producing 98.8% of food consumed by humans.^[203] Soil provides minerals and water to plants according to several processes involved in plant nutrition. Soil absorbs rainwater and releases it later, thus preventing floods and drought, flood regulation being one of the major ecosystem services provided by soil.^[204] Soil cleans water as it percolates through it.^[205] Soil is the habitat for many organisms: the major part of known and unknown biodiversity is in the soil, in the form of earthworms, woodlice, millipedes, centipedes, snails, slugs, mites, springtails, enchytraeids, nematodes, protists), bacteria, archaea, fungi and algae; and most organisms living above ground have part of them (plants) or spend part of their life cycle (insects) below-ground.^[206] Above-ground and below-ground biodiversities are tightly interconnected,^[156][207] making soil protection of paramount importance for any restoration or conservation plan.

The biological component of soil is an extremely important carbon sink since about 57% of the biotic content is carbon. Even in deserts, cyanobacteria, lichens and mosses form biological soil crusts which capture and sequester a significant amount of carbon by photosynthesis. Poor farming and grazing methods have degraded soils and released much of this sequestered carbon to the atmosphere. Restoring the world's soils could offset the effect of increases in greenhouse gas emissions and slow global warming, while improving crop yields and reducing water needs.^{[208][209][210]}

Waste management often has a soil component. Septic drain fields treat septic tank effluent using aerobic soil processes. Land application of waste water relies on soil biology to aerobically treat BOD. Alternatively, landfills use soil for daily cover, isolating waste deposits from the atmosphere and preventing unpleasant smells. Composting is now widely used to treat aerobically solid domestic waste and dried effluents of settling basins. Although compost is not soil, biological processes taking place during composting are similar to those occurring during decomposition and humification of soil organic matter.^[211]

Organic soils, especially peat, serve as a significant fuel and horticultural resource. Peat soils are also commonly used for the sake of agriculture in Nordic countries, because peatland sites, when drained, provide fertile soils for food production.^[212] However, wide areas of peat production, such as rain-fed sphagnum bogs, also called blanket bogs or raised bogs, are now protected because of their patrimonial interest. As an example, Flow Country, covering 4,000 square kilometres of rolling expanse of blanket bogs in Scotland, is now candidate for being included in the World Heritage List. Under present-day global warming peat soils are thought to be involved in a self-reinforcing (positive feedback) process of increased emission of greenhouse gases (methane and carbon dioxide) and increased temperature,^[213] a contention which is still under debate when replaced at field scale and including stimulated plant growth.^[214]

Geophagy is the practice of eating soil-like substances. Both animals and humans occasionally consume soil for medicinal, recreational, or religious purposes.^[215] It has been shown that some monkeys consume soil, together with their preferred food (tree foliage and fruits), in order to alleviate tannin toxicity.^[216]

Soils filter and purify water and affect its chemistry. Rain water and pooled water from ponds, lakes and rivers percolate through the soil horizons and the upper rock strata, thus becoming groundwater. Pests (viruses) and pollutants, such as persistent organic pollutants (chlorinated pesticides, polychlorinated biphenyls), oils (hydrocarbons), heavy metals (lead, zinc, cadmium), and excess nutrients (nitrates, sulfates, phosphates) are filtered out by the soil.^[217] Soil organisms metabolise them or immobilise them in their biomass and necromass,^[218] thereby incorporating them into stable humus.^[219] The physical integrity of soil is also a prerequisite for avoiding landslides in rugged landscapes.^[220]

Degradation

Main articles: Soil retrogression and degradation and Soil conservation

Land degradation is a human-induced or natural process which impairs the capacity of land to function.^[221] Soil degradation involves acidification, contamination, desertification, erosion or salination.^[222]

Acidification

Soil acidification is beneficial in the case of alkaline soils, but it degrades land when it lowers crop productivity, soil biological activity and increases soil vulnerability to contamination and erosion. Soils are initially acid and remain such when their parent materials are low in basic cations (calcium, magnesium, potassium and sodium). On parent materials richer in weatherable minerals acidification occurs when basic cations are leached from the soil profile by rainfall or exported by the harvesting of forest or agricultural crops. Soil acidification is accelerated by the use of acid-forming nitrogenous fertilizers and by the effects of acid precipitation. Deforestation is another cause of soil acidification, mediated by increased leaching of soil nutrients in the absence of tree canopies.^[223]

Contamination

Soil contamination at low levels is often within a soil's capacity to treat and assimilate waste material. Soil biota can treat waste by transforming it, mainly through microbial enzymatic activity.^[224] Soil organic matter and soil minerals can adsorb the waste material and decrease its toxicity,^[225] although when in colloidal form they may transport the adsorbed contaminants to subsurface environments.^[226] Many waste treatment processes rely on this natural bioremediation capacity. Exceeding treatment capacity can damage soil biota and limit soil function. Derelict soils occur where industrial contamination or other development activity damages the soil to such a degree that the land cannot be used safely or productively. Remediation of derelict soil uses principles of geology, physics, chemistry and biology to degrade, attenuate, isolate or remove soil contaminants to restore soil functions and values. Techniques include leaching, air sparging, soil conditioners, phytoremediation, bioremediation and Monitored Natural Attenuation. An example of diffuse pollution with contaminants is copper accumulation in vineyards and orchards to which fungicides are repeatedly applied, even in organic farming.^[227]

Microfibres from synthetic textiles are another type of plastic soil contamination, 100% of agricultural soil samples from southwestern China contained plastic particles, 92% of which were microfibres. Sources of microfibres likely included string or twine, as well as irrigation water in which clothes had been washed.^[228]

The application of biosolids from sewage sludge and compost can introduce microplastics to soils. This adds to the burden of microplastics from other sources (e.g. the atmosphere). Approximately half the sewage sludge in Europe and North America is applied to agricultural land. In Europe it has been estimated that for every million inhabitants 113 to 770 tonnes of microplastics are added to agricultural soils each year.^[228]

Desertification

 

Desertification

Desertification, an environmental process of ecosystem degradation in arid and semi-arid regions, is often caused by badly adapted human activities such as overgrazing or excess harvesting of firewood. It is a common misconception that drought causes desertification.^[229] Droughts are common in arid and semiarid lands. Well-managed lands can recover from drought when the rains return. Soil management tools include maintaining soil nutrient and organic matter levels, reduced tillage and increased cover.^[230] These practices help to control erosion and maintain productivity during periods when moisture is available. Continued land abuse during droughts, however, increases land degradation. Increased population and livestock pressure on marginal lands accelerates desertification.^[231] It is now questioned whether present-day climate warming will favour or disfavour desertification, with contradictory reports about predicted rainfall trends associated with increased temperature, and strong discrepancies among regions, even in the same country.^[232]

Erosion

 

Erosion control

Erosion of soil is caused by water, wind, ice, and movement in response to gravity. More than one kind of erosion can occur simultaneously. Erosion is distinguished from weathering, since erosion also transports eroded soil away from its place of origin (soil in transit may be described as sediment). Erosion is an intrinsic natural process, but in many places it is greatly increased by human activity, especially unsuitable land use practices.^[233] These include agricultural activities which leave the soil bare during times of heavy rain or strong winds, overgrazing, deforestation, and improper construction activity. Improved management can limit erosion. Soil conservation techniques which are employed include changes of land use (such as replacing erosion-prone crops with grass or other soil-binding plants), changes to the timing or type of agricultural operations, terrace building, use of erosion-suppressing cover materials (including cover crops and other plants), limiting disturbance during construction, and avoiding construction during erosion-prone periods and in erosion-prone places such as steep slopes.^[234] Historically, one of the best examples of large-scale soil erosion due to unsuitable land-use practices is wind erosion (the so-called dust bowl) which ruined American and Canadian prairies during the 1930s, when immigrant farmers, encouraged by the federal government of both countries, settled and converted the original shortgrass prairie to agricultural crops and cattle ranching.

A serious and long-running water erosion problem occurs in China, on the middle reaches of the Yellow River and the upper reaches of the Yangtze River. From the Yellow River, over 1.6 billion tons of sediment flow each year into the ocean. The sediment originates primarily from water erosion (gully erosion) in the Loess Plateau region of northwest China.^[235]

Soil piping is a particular form of soil erosion that occurs below the soil surface.^[236] It causes levee and dam failure, as well as sink hole formation. Turbulent flow removes soil starting at the mouth of the seep flow and the subsoil erosion advances up-gradient.^[237] The term sand boil is used to describe the appearance of the discharging end of an active soil pipe.^[238]

Salination

Soil salination is the accumulation of free salts to such an extent that it leads to degradation of the agricultural value of soils and vegetation. Consequences include corrosion damage, reduced plant growth, erosion due to loss of plant cover and soil structure, and water quality problems due to sedimentation. Salination occurs due to a combination of natural and human-caused processes. Arid conditions favour salt accumulation. This is especially apparent when soil parent material is saline. Irrigation of arid lands is especially problematic.^[239] All irrigation water has some level of salinity. Irrigation, especially when it involves leakage from canals and overirrigation in the field, often raises the underlying water table. Rapid salination occurs when the land surface is within the capillary fringe of saline groundwater. Soil salinity control involves watertable control and flushing with higher levels of applied water in combination with tile drainage or another form of subsurface drainage.^[240][241]

Reclamation

Main article: Soil regeneration

Soils which contain high levels of particular clays with high swelling properties, such as smectites, are often very fertile. For example, the smectite-rich paddy soils of Thailand's Central Plains are among the most productive in the world. However, the overuse of mineral nitrogen fertilizers and pesticides in irrigated intensive rice production has endangered these soils, forcing farmers to implement integrated practices based on Cost Reduction Operating Principles.^[242]

Many farmers in tropical areas, however, struggle to retain organic matter and clay in the soils they work. In recent years, for example, productivity has declined and soil erosion has increased in the low-clay soils of northern Thailand, following the abandonment of shifting cultivation for a more permanent land use.^[243] Farmers initially responded by adding organic matter and clay from termite mound material, but this was unsustainable in the long-term because of rarefaction of termite mounds. Scientists experimented with adding bentonite, one of the smectite family of clays, to the soil. In field trials, conducted by scientists from the International Water Management Institute (IWMI) in cooperation with Khon Kaen University and local farmers, this had the effect of helping retain water and nutrients. Supplementing the farmer's usual practice with a single application of 200 kilograms per rai (1,300 kg/ha; 1,100 lb/acre) of bentonite resulted in an average yield increase of 73%.^[244] Other studies showed that applying bentonite to degraded sandy soils reduced the risk of crop failure during drought years.^[245]

In 2008, three years after the initial trials, IWMI scientists conducted a survey among 250 farmers in northeast Thailand, half of whom had applied bentonite to their fields. The average improvement for those using the clay addition was 18% higher than for non-clay users. Using the clay had enabled some farmers to switch to growing vegetables, which need more fertile soil. This helped to increase their income. The researchers estimated that 200 farmers in northeast Thailand and 400 in Cambodia had adopted the use of clays, and that a further 20,000 farmers were introduced to the new technique.^[246]

If the soil is too high in clay or salts (e.g. saline sodic soil), adding gypsum, washed river sand and organic matter (e.g.municipal solid waste) will balance the composition.^[247]

Adding organic matter, like ramial chipped wood or compost, to soil which is depleted in nutrients and too high in sand will boost its quality and improve production.^[248][249]

Special mention must be made of the use of charcoal, and more generally biochar to improve nutrient-poor tropical soils, a process based on the higher fertility of anthropogenic pre-Columbian Amazonian Dark Earths, also called Terra Preta de Índio, due to interesting physical and chemical properties of soil black carbon as a source of stable humus.^[250] However, the uncontrolled application of charred waste products of all kinds may endanger soil life and human health.^[251]

History of studies and research

The history of the study of soil is intimately tied to humans' urgent need to provide food for themselves and forage for their animals. Throughout history, civilizations have prospered or declined as a function of the availability and productivity of their soils.^[252]

Studies of soil fertility

Main article: Soil fertility

The Greek historian Xenophon (450–355 BCE) is credited with being the first to expound upon the merits of green-manuring crops: 'But then whatever weeds are upon the ground, being turned into earth, enrich the soil as much as dung.'^[253]

Columella's Of husbandry, circa 60 CE, advocated the use of lime and that clover and alfalfa (green manure) should be turned under,^[254] and was used by 15 generations (450 years) under the Roman Empire until its collapse.^[253][255] From the fall of Rome to the French Revolution, knowledge of soil and agriculture was passed on from parent to child and as a result, crop yields were low. During the European Middle Ages, Yahya Ibn al-'Awwam's handbook,^[256] with its emphasis on irrigation, guided the people of North Africa, Spain and the Middle East; a translation of this work was finally carried to the southwest of the United States when under Spanish influence.^[257] Olivier de Serres, considered the father of French agronomy, was the first to suggest the abandonment of fallowing and its replacement by hay meadows within crop rotations. He also highlighted the importance of soil (the French terroir) in the management of vineyards. His famous book Le Théâtre d'Agriculture et mesnage des champs^[258] contributed to the rise of modern, sustainable agriculture and to the collapse of old agricultural practices such as soil amendment for crops by the lifting of forest litter and assarting, which ruined the soils of western Europe during the Middle Ages and even later on according to regions.^[259]

Experiments into what made plants grow first led to the idea that the ash left behind when plant matter was burned was the essential element but overlooked the role of nitrogen, which is not left on the ground after combustion, a belief which prevailed until the 19th century.^[260] In about 1635, the Flemish chemist Jan Baptist van Helmont thought he had proved water to be the essential element from his famous five years' experiment with a willow tree grown with only the addition of rainwater. His conclusion came from the fact that the increase in the plant's weight had apparently been produced only by the addition of water, with no reduction in the soil's weight.^{[261][262][263]} John Woodward (d. 1728) experimented with various types of water ranging from clean to muddy and found muddy water the best, and so he concluded that earthy matter was the essential element. Others concluded it was humus in the soil that passed some essence to the growing plant. Still others held that the vital growth principal was something passed from dead plants or animals to the new plants. At the start of the 18th century, Jethro Tull demonstrated that it was beneficial to cultivate (stir) the soil, but his opinion that the stirring made the fine parts of soil available for plant absorption was erroneous.^[262][264]

As chemistry developed, it was applied to the investigation of soil fertility. The French chemist Antoine Lavoisier showed in about 1778 that plants and animals must combust oxygen internally to live. He was able to deduce that most of the 165-pound (75 kg) weight of van Helmont's willow tree derived from air.^[265] It was the French agriculturalist Jean-Baptiste Boussingault who by means of experimentation obtained evidence showing that the main sources of carbon, hydrogen and oxygen for plants were air and water, while nitrogen was taken from soil.^[266] Justus von Liebig in his book Organic chemistry in its applications to agriculture and physiology (published 1840), asserted that the chemicals in plants must have come from the soil and air and that to maintain soil fertility, the used minerals must be replaced.^[267] Liebig nevertheless believed the nitrogen was supplied from the air. The enrichment of soil with guano by the Incas was rediscovered in 1802, by Alexander von Humboldt. This led to its mining and that of Chilean nitrate and to its application to soil in the United States and Europe after 1840.^[268]

The work of Liebig was a revolution for agriculture, and so other investigators started experimentation based on it. In England John Bennet Lawes and Joseph Henry Gilbert worked in the Rothamsted Experimental Station, founded by the former, and (re)discovered that plants took nitrogen from the soil, and that salts needed to be in an available state to be absorbed by plants. Their investigations also produced the superphosphate, consisting in the acid treatment of phosphate rock.^[269] This led to the invention and use of salts of potassium (K) and nitrogen (N) as fertilizers. Ammonia generated by the production of coke was recovered and used as fertiliser.^[270] Finally, the chemical basis of nutrients delivered to the soil in manure was understood and in the mid-19th century chemical fertilisers were applied. However, the dynamic interaction of soil and its life forms was still not understood.

In 1856, J. Thomas Way discovered that ammonia contained in fertilisers was transformed into nitrates,^[271] and twenty years later Robert Warington proved that this transformation was done by living organisms.^[272] In 1890 Sergei Winogradsky announced he had found the bacteria responsible for this transformation.^[273]

It was known that certain legumes could take up nitrogen from the air and fix it to the soil but it took the development of bacteriology towards the end of the 19th century to lead to an understanding of the role played in nitrogen fixation by bacteria. The symbiosis of bacteria and leguminous roots, and the fixation of nitrogen by the bacteria, were simultaneously discovered by the German agronomist Hermann Hellriegel and the Dutch microbiologist Martinus Beijerinck.^[269]

Crop rotation, mechanisation, chemical and natural fertilisers led to a doubling of wheat yields in western Europe between 1800 and 1900.^[274]

Studies of soil formation

See also: Pedogenesis

The scientists who studied the soil in connection with agricultural practices had considered it mainly as a static substrate. However, soil is the result of evolution from more ancient geological materials, under the action of biotic and abiotic processes. After studies of the improvement of the soil commenced, other researchers began to study soil genesis and as a result also soil types and classifications.

In 1860, while in Mississippi, Eugene W. Hilgard (1833–1916) studied the relationship between rock material, climate, vegetation, and the type of soils that were developed. He realised that the soils were dynamic, and considered the classification of soil types.^[275] His work was not continued. At about the same time, Friedrich Albert Fallou was describing soil profiles and relating soil characteristics to their formation as part of his professional work evaluating forest and farm land for the principality of Saxony. His 1857 book, Anfangsgründe der Bodenkunde (First principles of soil science) established modern soil science.^[276] Contemporary with Fallou's work, and driven by the same need to accurately assess land for equitable taxation, Vasily Dokuchaev led a team of soil scientists in Russia who conducted an extensive survey of soils, observing that similar basic rocks, climate and vegetation types lead to similar soil layering and types, and established the concepts for soil classifications. Due to language barriers, the work of this team was not communicated to western Europe until 1914 through a publication in German by Konstantin Glinka, a member of the Russian team.^[277]

Curtis F. Marbut, influenced by the work of the Russian team, translated Glinka's publication into English,^[278] and, as he was placed in charge of the U.S. National Cooperative Soil Survey, applied it to a national soil classification system.^[262]

See also

•  Environment portal
•  Geology portal

• Acid sulfate soil
• Agrophysics
• Crust
• Agricultural science
• Factors affecting permeability of soils
• Index of soil-related articles
• Mycorrhizal fungi and soil carbon storage
• Shrink–swell capacity
• Soil biodiversity
• Soil liquefaction
• Soil moisture velocity equation
• Soil zoology
• Tillage erosion
• World Soil Museum
• Red soil

References

1. Voroney, R. Paul; Heck, Richard J. (2007). "The soil habitat". In Paul, Eldor A. (ed.). Soil microbiology, ecology and biochemistry (3rd ed.). Amsterdam, the Netherlands: Elsevier. pp. 25–49. doi:10.1016/B978-0-08-047514-1.50006-8. ISBN 978-0-12-546807-7. (PDF) from the original on 10 July 2018. Retrieved 27 March 2022.
2. Taylor, Sterling A.; Ashcroft, Gaylen L. (1972). Physical edaphology: the physics of irrigated and nonirrigated soils. San Francisco, California: W.H. Freeman. ISBN 978-0-7167-0818-6.
3. McCarthy, David F. (2014). Essentials of soil mechanics and foundations: basic geotechnics (7th ed.). London, United Kingdom: Pearson. ISBN 9781292039398. Retrieved 27 March 2022.
4. Gilluly, James; Waters, Aaron Clement; Woodford, Alfred Oswald (1975). Principles of geology (4th ed.). San Francisco, California: W.H. Freeman. ISBN 978-0-7167-0269-6.
5. Huggett, Richard John (2011). "What is geomorphology?". Fundamentals of geomorphology. Routledge Fundamentals of Physical Geography Series (3rd ed.). London, United Kingdom: Routledge. pp. 148–150. ISBN 978-0-203-86008-3. Retrieved 16 October 2022.
6. Ponge, Jean-François (2015). "The soil as an ecosystem". Biology and Fertility of Soils. 51 (6): 645–648. doi:10.1007/s00374-015-1016-1. S2CID 18251180. Retrieved 3 April 2022.
7. Yu, Charley; Kamboj, Sunita; Wang, Cheng; Cheng, Jing-Jy (2015). "Data collection handbook to support modeling impacts of radioactive material in soil and building structures" (PDF). Argonne National Laboratory. pp. 13–21. (PDF) from the original on 4 August 2018. Retrieved 3 April 2022.
8. Buol, Stanley W.; Southard, Randal J.; Graham, Robert C.; McDaniel, Paul A. (2011). Soil genesis and classification (6th ed.). Ames, Iowa: Wiley-Blackwell. ISBN 978-0-470-96060-8. Retrieved 3 April 2022.
9. Retallack, Gregory J.; Krinsley, David H.; Fischer, Robert; Razink, Joshua J.; Langworthy, Kurt A. (2016). "Archean coastal-plain paleosols and life on land" (PDF). Gondwana Research. 40: 1–20. Bibcode:2016GondR..40....1R. doi:10.1016/j.gr.2016.08.003. (PDF) from the original on 13 November 2018. Retrieved 3 April 2022.
10. Chesworth, Ward, ed. (2008). Encyclopedia of soil science (1st ed.). Dordrecht, The Netherlands: Springer. ISBN 978-1-4020-3994-2. (PDF) from the original on 5 September 2018. Retrieved 27 March 2022.
11. "Glossary of terms in soil science". Agriculture and Agri-Food Canada. 13 December 2013. from the original on 27 October 2018. Retrieved 3 April 2022.
12. Amundson, Ronald. (PDF). CiteSeerX 10.1.1.552.237. Archived from the original (PDF) on 12 June 2018.
13. Küppers, Michael; Vincent, Jean-Baptiste. "Impacts and formation of regolith". Max Planck Institute for Solar System Research. from the original on 4 August 2018. Retrieved 3 April 2022.
14. Amelung, Wulf; Bossio, Deborah; De Vries, Wim; Kögel-Knabner, Ingrid; Lehmann, Johannes; Amundson, Ronald; Bol, Roland; Collins, Chris; Lal, Rattan; Leifeld, Jens; Minasny, Buniman; Pan, Gen-Xing; Paustian, Keith; Rumpel, Cornelia; Sanderman, Jonathan; Van Groeningen, Jan Willem; Mooney, Siân; Van Wesemael, Bas; Wander, Michelle; Chabbi, Abad (27 October 2020). "Towards a global-scale soil climate mitigation strategy" (PDF). Nature Communications. 11 (1): 5427. Bibcode:2020NatCo..11.5427A. doi:10.1038/s41467-020-18887-7. ISSN 2041-1723. PMC 7591914. PMID 33110065. Retrieved 3 April 2022.
15. Pouyat, Richard; Groffman, Peter; Yesilonis, Ian; Hernandez, Luis (2002). "Soil carbon pools and fluxes in urban ecosystems". Environmental Pollution. 116 (Supplement 1): S107–S118. doi:10.1016/S0269-7491(01)00263-9. PMID 11833898. Retrieved 3 April 2022. Our analysis of pedon data from several disturbed soil profiles suggests that physical disturbances and anthropogenic inputs of various materials (direct effects) can greatly alter the amount of C stored in these human "made" soils.
16. Davidson, Eric A.; Janssens, Ivan A. (2006). "Temperature sensitivity of soil carbon decomposition and feedbacks to climate change" (PDF). Nature. 440 (9 March 2006): 165‒73. Bibcode:2006Natur.440..165D. doi:10.1038/nature04514. PMID 16525463. S2CID 4404915. Retrieved 3 April 2022.
17. Powlson, David (2005). "Will soil amplify climate change?". Nature. 433 (20 January 2005): 204‒05. Bibcode:2005Natur.433..204P. doi:10.1038/433204a. PMID 15662396. S2CID 35007042. Retrieved 3 April 2022.
18. Bradford, Mark A.; Wieder, William R.; Bonan, Gordon B.; Fierer, Noah; Raymond, Peter A.; Crowther, Thomas W. (2016). "Managing uncertainty in soil carbon feedbacks to climate change" (PDF). Nature Climate Change. 6 (27 July 2016): 751–758. Bibcode:2016NatCC...6..751B. doi:10.1038/nclimate3071. hdl:20.500.11755/c1792dbf-ce96-4dc7-8851-1ca50a35e5e0. S2CID 43955196. Retrieved 3 April 2022.
19. Dominati, Estelle; Patterson, Murray; Mackay, Alec (2010). "A framework for classifying and quantifying the natural capital and ecosystem services of soils". Ecological Economics. 69 (9): 1858‒68. doi:10.1016/j.ecolecon.2010.05.002. (PDF) from the original on 8 August 2017. Retrieved 10 April 2022.
20. Dykhuizen, Daniel E. (1998). "Santa Rosalia revisited: why are there so many species of bacteria?". Antonie van Leeuwenhoek. 73 (1): 25‒33. doi:10.1023/A:1000665216662. PMID 9602276. S2CID 17779069. Retrieved 10 April 2022.
21. Torsvik, Vigdis; Øvreås, Lise (2002). "Microbial diversity and function in soil: from genes to ecosystems". Current Opinion in Microbiology. 5 (3): 240‒45. doi:10.1016/S1369-5274(02)00324-7. PMID 12057676. Retrieved 10 April 2022.
22. Raynaud, Xavier; Nunan, Naoise (2014). "Spatial ecology of bacteria at the microscale in soil". PLOS ONE. 9 (1): e87217. Bibcode:2014PLoSO...987217R. doi:10.1371/journal.pone.0087217. PMC 3905020. PMID 24489873.
23. Whitman, William B.; Coleman, David C.; Wiebe, William J. (1998). "Prokaryotes: the unseen majority". Proceedings of the National Academy of Sciences of the USA. 95 (12): 6578‒83. Bibcode:1998PNAS...95.6578W. doi:10.1073/pnas.95.12.6578. PMC 33863. PMID 9618454.
24. Schlesinger, William H.; Andrews, Jeffrey A. (2000). "Soil respiration and the global carbon cycle". Biogeochemistry. 48 (1): 7‒20. doi:10.1023/A:1006247623877. S2CID 94252768. Retrieved 10 April 2022.
25. Denmead, Owen Thomas; Shaw, Robert Harold (1962). "Availability of soil water to plants as affected by soil moisture content and meteorological conditions". Agronomy Journal. 54 (5): 385‒90. doi:10.2134/agronj1962.00021962005400050005x. Retrieved 10 April 2022.
26. House, Christopher H.; Bergmann, Ben A.; Stomp, Anne-Marie; Frederick, Douglas J. (1999). "Combining constructed wetlands and aquatic and soil filters for reclamation and reuse of water". Ecological Engineering. 12 (1–2): 27–38. doi:10.1016/S0925-8574(98)00052-4. Retrieved 10 April 2022.
27. Van Bruggen, Ariena H.C.; Semenov, Alexander M. (2000). "In search of biological indicators for soil health and disease suppression". Applied Soil Ecology. 15 (1): 13–24. doi:10.1016/S0929-1393(00)00068-8. Retrieved 10 April 2022.
28. "Community guide to monitored natural attenuation" (PDF). Retrieved 10 April 2022.
29. Linn, Daniel Myron; Doran, John W. (1984). "Effect of water-filled pore space on carbon dioxide and nitrous oxide production in tilled and nontilled soils". Soil Science Society of America Journal. 48 (6): 1267–1272. Bibcode:1984SSASJ..48.1267L. doi:10.2136/sssaj1984.03615995004800060013x. Retrieved 10 April 2022.
30. Gregory, Peter J.; Nortcliff, Stephen (2013). Soil conditions and plant growth. Hoboken, New Jersey: Wiley-Blackwell. ISBN 9781405197700. Retrieved 10 April 2022.
31. Bot, Alexandra; Benites, José (2005). The importance of soil organic matter: key to drought-resistant soil and sustained food and production (PDF). Rome: Food and Agriculture Organization of the United Nations. ISBN 978-92-5-105366-9. Retrieved 10 April 2022.
32. McClellan, Tai. "Soil composition". University of Hawaiʻi at Mānoa, College of Tropical Agriculture and Human Resources. Retrieved 18 April 2022.
33. . Cooperative Extension, College of Agriculture, University of Arizona. 9 November 2017. Archived from the original on 29 May 2016. Retrieved 17 December 2017.
34. Vannier, Guy (1987). "The porosphere as an ecological medium emphasized in Professor Ghilarov's work on soil animal adaptations" (PDF). Biology and Fertility of Soils. 3 (1): 39–44. doi:10.1007/BF00260577. S2CID 297400. Retrieved 18 April 2022.
35. Torbert, H. Allen; Wood, Wes (1992). "Effect of soil compaction and water-filled pore space on soil microbial activity and N losses". Communications in Soil Science and Plant Analysis. 23 (11): 1321‒31. doi:10.1080/00103629209368668. Retrieved 18 April 2022.
36. Simonson 1957, p. 17.
37. Zanella, Augusto; Katzensteiner, Klaus; Ponge, Jean-François; Jabiol, Bernard; Sartori, Giacomo; Kolb, Eckart; Le Bayon, Renée-Claire; Aubert, Michaël; Ascher-Jenull, Judith; Englisch, Michael; Hager, Herbert (June 2019). "TerrHum: an iOS App for classifying terrestrial humipedons and some considerations about soil classification". Soil Science Society of America Journal. 83 (S1): S42–S48. doi:10.2136/sssaj2018.07.0279. hdl:11577/3315165. S2CID 197555747. Retrieved 18 April 2022.
38. Bronick, Carol J.; Lal, Ratan (January 2005). "Soil structure and management: a review" (PDF). Geoderma. 124 (1–2): 3–22. Bibcode:2005Geode.124....3B. doi:10.1016/j.geoderma.2004.03.005. Retrieved 18 April 2022.
39. "Soil and water". Food and Agriculture Organization of the United Nations. Retrieved 18 April 2022.
40. Valentin, Christian; d'Herbès, Jean-Marc; Poesen, Jean (1999). "Soil and water components of banded vegetation patterns". Catena. 37 (1): 1‒24. Bibcode:1999Caten..37....1V. doi:10.1016/S0341-8162(99)00053-3. Retrieved 18 April 2022.
41. Brady, Nyle C.; Weil, Ray R. (2007). "The colloidal fraction: seat of soil chemical and physical activity". In Brady, Nyle C.; Weil, Ray R. (eds.). The nature and properties of soils (14th ed.). London, United Kingdom: Pearson. pp. 310–357. ISBN 978-0132279383. Retrieved 18 April 2022.
42. "Soil colloids: properties, nature, types and significance" (PDF). Tamil Nadu Agricultural University. Retrieved 18 April 2022.
43. Miller, Jarrod O. "Soil pH affects nutrient availability". Retrieved 18 April 2022.
44. Goulding, Keith W.T.; Bailey, Neal J.; Bradbury, Nicola J.; Hargreaves, Patrick; Howe, M.T.; Murphy, Daniel V.; Poulton, Paul R.; Willison, Toby W. (1998). "Nitrogen deposition and its contribution to nitrogen cycling and associated soil processes". New Phytologist. 139 (1): 49‒58. doi:10.1046/j.1469-8137.1998.00182.x.
45. Kononova, M.M. (2013). Soil organic matter: its nature, its role in soil formation and in soil fertility (2nd ed.). Amsterdam, The Netherlands: Elsevier. ISBN 978-1-4831-8568-2. Retrieved 24 April 2022.
46. Burns, Richards G.; DeForest, Jared L.; Marxsen, Jürgen; Sinsabaugh, Robert L.; Stromberger, Mary E.; Wallenstein, Matthew D.; Weintraub, Michael N.; Zoppini, Annamaria (2013). "Soil enzymes in a changing environment: current knowledge and future directions". Soil Biology and Biochemistry. 58: 216‒34. doi:10.1016/j.soilbio.2012.11.009. Retrieved 24 April 2022.
47. Sengupta, Aditi; Kushwaha, Priyanka; Jim, Antonia; Troch, Peter A.; Maier, Raina (2020). "New soil, old plants, and ubiquitous microbes: evaluating the potential of incipient basaltic soil to support native plant growth and influence belowground soil microbial community composition". Sustainability. 12 (10): 4209. doi:10.3390/su12104209.
48. Bishop, Janice L.; Murchie, Scott L.; Pieters, Carlé L.; Zent, Aaron P. (2002). "A model for formation of dust, soil, and rock coatings on Mars: physical and chemical processes on the Martian surface". Journal of Geophysical Research. 107 (E11): 7-1–7-17. Bibcode:2002JGRE..107.5097B. doi:10.1029/2001JE001581.
49. Navarro-González, Rafael; Rainey, Fred A.; Molina, Paola; Bagaley, Danielle R.; Hollen, Becky J.; de la Rosa, José; Small, Alanna M.; Quinn, Richard C.; Grunthaner, Frank J.; Cáceres, Luis; Gomez-Silva, Benito; McKay, Christopher P. (2003). "Mars-like soils in the Atacama desert, Chile, and the dry limit of microbial life". Science. 302 (5647): 1018–1021. Bibcode:2003Sci...302.1018N. doi:10.1126/science.1089143. PMID 14605363. S2CID 18220447. Retrieved 24 April 2022.
50. Guo, Yong; Fujimura, Reiko; Sato, Yoshinori; Suda, Wataru; Kim, Seok-won; Oshima, Kenshiro; Hattori, Masahira; Kamijo, Takashi; Narisawa, Kazuhiko; Ohta, Hiroyuki (2014). "Characterization of early microbial communities on volcanic deposits along a vegetation gradient on the island of Miyake, Japan". Microbes and Environments. 29 (1): 38–49. doi:10.1264/jsme2.ME13142. PMC 4041228. PMID 24463576.
51. Goldich, Samuel S. (1938). "A study in rock-weathering". The Journal of Geology. 46 (1): 17–58. Bibcode:1938JG.....46...17G. doi:10.1086/624619. ISSN 0022-1376. S2CID 128498195. Retrieved 24 April 2022.
52. Van Schöll, Laura; Smits, Mark M.; Hoffland, Ellis (2006). "Ectomycorrhizal weathering of the soil minerals muscovite and hornblende". New Phytologist. 171 (4): 805–814. doi:10.1111/j.1469-8137.2006.01790.x. PMID 16918551.
53. Stretch, Rachelle C.; Viles, Heather A. (2002). "The nature and rate of weathering by lichens on lava flows on Lanzarote". Geomorphology. 47 (1): 87–94. Bibcode:2002Geomo..47...87S. doi:10.1016/S0169-555X(02)00143-5. Retrieved 24 April 2022.
54. Dojani, Stephanie; Lakatos, Michael; Rascher, Uwe; Waneck, Wolfgang; Luettge, Ulrich; Büdel, Burkhard (2007). "Nitrogen input by cyanobacterial biofilms of an inselberg into a tropical rainforest in French Guiana". Flora. 202 (7): 521–529. doi:10.1016/j.flora.2006.12.001. Retrieved 21 March 2021.
55. Kabala, Cesary; Kubicz, Justyna (2012). "Initial soil development and carbon accumulation on moraines of the rapidly retreating Werenskiold Glacier, SW Spitsbergen, Svalbard archipelago". Geoderma. 175–176: 9–20. Bibcode:2012Geode.175....9K. doi:10.1016/j.geoderma.2012.01.025. Retrieved 24 April 2022.
56. Jenny, Hans (1941). Factors of soil formation: a system of qunatitative pedology (PDF). New York: McGraw-Hill. (PDF) from the original on 8 August 2017. Retrieved 24 April 2022.
57. Ritter, Michael E. "The physical environment: an introduction to physical geography" (PDF). Retrieved 24 April 2022.
58. Gardner, Catriona M.K.; Laryea, Kofi Buna; Unger, Paul W. (1999). (PDF) (first ed.). Rome, Italy: Food and Agriculture Organization of the United Nations. Archived from the original (PDF) on 8 August 2017.
59. Six, Johan; Paustian, Keith; Elliott, Edward T.; Combrink, Clay (2000). "Soil structure and organic matter. I. Distribution of aggregate-size classes and aggregate-associated carbon". Soil Science Society of America Journal. 64 (2): 681–689. Bibcode:2000SSASJ..64..681S. doi:10.2136/sssaj2000.642681x. Retrieved 7 August 2022.
60. Håkansson, Inge; Lipiec, Jerzy (2000). "A review of the usefulness of relative bulk density values in studies of soil structure and compaction" (PDF). Soil and Tillage Research. 53 (2): 71–85. doi:10.1016/S0167-1987(99)00095-1. S2CID 30045538. Retrieved 7 August 2022.
61. Schwerdtfeger, William J. (1965). "Soil resistivity as related to underground corrosion and cathodic protection" (PDF). Journal of Research of the National Bureau of Standards. 69C (1): 71–77. doi:10.6028/jres.069c.012. Retrieved 7 August 2022.
62. Tamboli, Prabhakar Mahadeo (1961). The influence of bulk density and aggregate size on soil moisture retention. Ames, Iowa: Iowa State University. Retrieved 7 August 2022.
63. Spehn, Eva M.; Joshi, Jasmin; Schmid, Bernhard; Alphei, Jörn; Körner, Christian (2000). "Plant diversity effects on soil heterotrophic activity in experimental grassland ecosystems". Plant and Soil. 224 (2): 217–230. doi:10.1023/A:1004891807664. S2CID 25639544.
64. "Water holding capacity". Oregon State University. 24 June 2016. Retrieved 9 October 2022. Irrigators must have knowledge of the readily available moisture capacity so that water can be applied before plants have to expend excessive energy to extract moisture
65. "Basics of irrigation scheduling". University of Minnesota Extension. Retrieved 9 October 2022. Only a portion of the available water holding capacity is easily used by the crop before crop water stress develop
66. Qi, Jingen; Marshall, John D.; Mattson, Kim G. (1994). "High soil carbon dioxide concentrations inhibit root respiration of Douglas fir". New Phytologist. 128 (3): 435–442. doi:10.1111/j.1469-8137.1994.tb02989.x. PMID 33874575.
67. Karberg, Noah J.; Pregitzer, Kurt S.; King, John S.; Friend, Aaron L.; Wood, James R. (2005). "Soil carbon dioxide partial pressure and dissolved inorganic carbonate chemistry under elevated carbon dioxide and ozone". Oecologia. 142 (2): 296–306. Bibcode:2005Oecol.142..296K. doi:10.1007/s00442-004-1665-5. PMID 15378342. S2CID 6161016. Retrieved 13 November 2022.
68. Chang, H.T.; Loomis, Walter E. (1945). "Effect of carbon dioxide on absorption of water and nutrients by roots". Plant Physiology. 20 (2): 221–232. doi:10.1104/pp.20.2.221. PMC 437214. PMID 16653979.
69. McDowell, Nate J.; Marshall, John D.; Qi, Jingen; Mattson, Kim (1999). "Direct inhibition of maintenance respiration in western hemlock roots exposed to ambient soil carbon dioxide concentrations". Tree Physiology. 19 (9): 599–605. doi:10.1093/treephys/19.9.599. PMID 12651534.
70. Xu, Xia; Nieber, John L.; Gupta, Satish C. (1992). "Compaction effect on the gas diffusion coefficient in soils". Soil Science Society of America Journal. 56 (6): 1743–1750. Bibcode:1992SSASJ..56.1743X. doi:10.2136/sssaj1992.03615995005600060014x. Retrieved 13 November 2022.
71. Smith, Keith A.; Ball, Tom; Conen, Franz; Dobbie, Karen E.; Massheder, Jonathan; Rey, Ana (2003). "Exchange of greenhouse gases between soil and atmosphere: interactions of soil physical factors and biological processes". European Journal of Soil Science. 54 (4): 779–791. doi:10.1046/j.1351-0754.2003.0567.x. S2CID 18442559. Retrieved 13 November 2022.
72. Russell 1957, pp. 35–36.
73. Ruser, Reiner; Flessa, Heiner; Russow, Rolf; Schmidt, G.; Buegger, Franz; Munch, J.C. (2006). "Emission of N₂O, N₂ and CO₂ from soil fertilized with nitrate: effect of compaction, soil moisture and rewetting". Soil Biology and Biochemistry. 38 (2): 263–274. doi:10.1016/j.soilbio.2005.05.005.
74. Hartmann, Adrian A.; Buchmann, Nina; Niklaus, Pascal A. (2011). "A study of soil methane sink regulation in two grasslands exposed to drought and N fertilization" (PDF). Plant and Soil. 342 (1–2): 265–275. doi:10.1007/s11104-010-0690-x. hdl:20.500.11850/34759. S2CID 25691034. Retrieved 13 November 2022.
75. Moore, Tim R.; Dalva, Moshe (1993). "The influence of temperature and water table position on carbon dioxide and methane emissions from laboratory columns of peatland soils". Journal of Soil Science. 44 (4): 651–664. doi:10.1111/j.1365-2389.1993.tb02330.x. Retrieved 13 November 2022.
76. Hiltpold, Ivan; Toepfer, Stefan; Kuhlmann, Ulrich; Turlings, Ted C.J. (2010). "How maize root volatiles affect the efficacy of entomopathogenic nematodes in controlling the western corn rootworm?". Chemoecology. 20 (2): 155–162. doi:10.1007/s00049-009-0034-6. S2CID 30214059. Retrieved 13 November 2022.
77. Ryu, Choong-Min; Farag, Mohamed A.; Hu, Chia-Hui; Reddy, Munagala S.; Wei, Han-Xun; Paré, Paul W.; Kloepper, Joseph W. (2003). "Bacterial volatiles promote growth in Arabidopsis". Proceedings of the National Academy of Sciences of the United States of America. 100 (8): 4927–4932. Bibcode:2003PNAS..100.4927R. doi:10.1073/pnas.0730845100. PMC 153657. PMID 12684534.
78. Hung, Richard; Lee, Samantha; Bennett, Joan W. (2015). "Fungal volatile organic compounds and their role in ecosystems". Applied Microbiology and Biotechnology. 99 (8): 3395–3405. doi:10.1007/s00253-015-6494-4. PMID 25773975. S2CID 14509047. Retrieved 13 November 2022.
79. Purrington, Foster Forbes; Kendall, Paricia A.; Bater, John E.; Stinner, Benjamin R. (1991). "Alarm pheromone in a gregarious poduromorph collembolan (Collembola: Hypogastruridae)". Great Lakes Entomologist. 24 (2): 75–78. Retrieved 13 November 2022.
80. Badri, Dayakar V.; Weir, Tiffany L.; Van der Lelie, Daniel; Vivanco, Jorge M (2009). "Rhizosphere chemical dialogues: plant–microbe interactions" (PDF). Current Opinion in Biotechnology. 20 (6): 642–650. doi:10.1016/j.copbio.2009.09.014. PMID 19875278. Retrieved 13 November 2022.
81. Salmon, Sandrine; Ponge, Jean-François (2001). "Earthworm excreta attract soil springtails: laboratory experiments on Heteromurus nitidus (Collembola: Entomobryidae)". Soil Biology and Biochemistry. 33 (14): 1959–1969. doi:10.1016/S0038-0717(01)00129-8. S2CID 26647480. Retrieved 13 November 2022.
82. Lambers, Hans; Mougel, Christophe; Jaillard, Benoît; Hinsinger, Philipe (2009). "Plant-microbe-soil interactions in the rhizosphere: an evolutionary perspective". Plant and Soil. 321 (1–2): 83–115. doi:10.1007/s11104-009-0042-x. S2CID 6840457. Retrieved 13 November 2022.
83. Peñuelas, Josep; Asensio, Dolores; Tholl, Dorothea; Wenke, Katrin; Rosenkranz, Maaria; Piechulla, Birgit; Schnitzler, Jörg-Petter (2014). "Biogenic volatile emissions from the soil". Plant, Cell and Environment. 37 (8): 1866–1891. doi:10.1111/pce.12340. PMID 24689847.
84. Buzuleciu, Samuel A.; Crane, Derek P.; Parker, Scott L. (2016). "Scent of disinterred soil as an olfactory cue used by raccoons to locate nests of diamond-backed terrapins (Malaclemys terrapin)" (PDF). Herpetological Conservation and Biology. 11 (3): 539–551. Retrieved 27 November 2022.
85. Saxton, Keith E.; Rawls, Walter J. (2006). "Soil water characteristic estimates by texture and organic matter for hydrologic solutions" (PDF). Soil Science Society of America Journal. 70 (5): 1569–1578. Bibcode:2006SSASJ..70.1569S. doi:10.2136/sssaj2005.0117. S2CID 16826314. (PDF) from the original on 2 September 2018. Retrieved 15 January 2023.
86. College of Tropical Agriculture and Human Resources. "Soil mineralogy". University of Hawaiʻi at Mānoa. Retrieved 15 January 2023.
87. Sposito, Garrison (1984). The surface chemistry of soils. New York: Oxford University Press. Retrieved 15 January 2023.
88. Wynot, Christopher. "Theory of diffusion in colloidal suspensions". Retrieved 15 January 2023.
89. Donahue, Miller & Shickluna 1977, p. 103–106.
90. Sposito, Garrison; Skipper, Neal T.; Sutton, Rebecca; Park, Sung-Ho; Soper, Alan K.; Greathouse, Jeffery A. (1999). "Surface geochemistry of the clay minerals". Proceedings of the National Academy of Sciences of the United States of America. 96 (7): 3358–3364. Bibcode:1999PNAS...96.3358S. doi:10.1073/pnas.96.7.3358. PMC 34275. PMID 10097044.
91. Bickmore, Barry R.; Rosso, Kevin M.; Nagy, Kathryn L.; Cygan, Randall T.; Tadanier, Christopher J. (2003). "Ab initio determination of edge surface structures for dioctahedral 2:1 phyllosilicates: implications for acid-base reactivity" (PDF). Clays and Clay Minerals. 51 (4): 359–371. Bibcode:2003CCM....51..359B. doi:10.1346/CCMN.2003.0510401. S2CID 97428106. Retrieved 15 January 2023.
92. Rajamathi, Michael; Thomas, Grace S.; Kamath, P. Vishnu (2001). "The many ways of making anionic clays". Journal of Chemical Sciences. 113 (5–6): 671–680. doi:10.1007/BF02708799. S2CID 97507578. Retrieved 15 January 2023.
93. Moayedi, Hossein; Kazemian, Sina (2012). "Zeta potentials of suspended humus in multivalent cationic saline solution and its effect on electro-osomosis behavior". Journal of Dispersion Science and Technology. 34 (2): 283–294. doi:10.1080/01932691.2011.646601. S2CID 94333872. Retrieved 15 January 2023.
94. Pettit, Robert E. "Organic matter, humus, humate, humic acid, fulvic acid and humin: their importance in soil fertility and plant health" (PDF). Retrieved 15 January 2023.
95. Diamond, Sidney; Kinter, Earl B. (1965). "Mechanisms of soil-lime stabilization: an interpretive review" (PDF). Highway Research Record. 92: 83–102. Retrieved 15 January 2023.
96. Woodruff, Clarence M. (1955). "The energies of replacement of calcium by potassium in soils" (PDF). Soil Science Society of America Journal. 19 (2): 167–171. Bibcode:1955SSASJ..19..167W. doi:10.2136/sssaj1955.03615995001900020014x. Retrieved 15 January 2023.
97. Fronæus, Sture (1953). "On the application of the mass action law to cation exchange equilibria". Acta Chemica Scandinavica. 7: 469–480. doi:10.3891/acta.chem.scand.07-0469.
98. Bolland, Mike D. A.; Posner, Alan M.; Quirk, James P. (1980). "pH-independent and pH-dependent surface charges on kaolinite". Clays and Clay Minerals. 28 (6): 412–418. Bibcode:1980CCM....28..412B. doi:10.1346/CCMN.1980.0280602. S2CID 12462516. Retrieved 15 January 2023.
99. Chakraborty, Meghna (8 August 2022). "What is cation exchange capacity in soils?". Retrieved 15 January 2023.
100. Silber, Avner; Levkovitch, Irit; Graber, Ellen R. (2010). "pH-dependent mineral release and surface properties of cornstraw biochar: agronomic implications". Environmental Science and Technology. 44 (24): 9318–23. Bibcode:2010EnST...44.9318S. doi:10.1021/es101283d. PMID 21090742. Retrieved 15 January 2023.
101. Dakora, Felix D.; Phillips, Donald D. (2002). "Root exudates as mediators of mineral acquisition in low-nutrient environments". Plant and Soil. 245: 35–47. doi:10.1023/A:1020809400075. S2CID 3330737. (PDF) from the original on 19 August 2019. Retrieved 15 January 2023.
102. Brown, John C. (1978). "Mechanism of iron uptake by plants". Plant, Cell and Environment. 1 (4): 249–257. doi:10.1111/j.1365-3040.1978.tb02037.x. Retrieved 29 January 2023.
103. Donahue, Miller & Shickluna 1977, p. 114.
104. Singh, Jamuna Sharan; Raghubanshi, Akhilesh Singh; Singh, Raj S.; Srivastava, S. C. (1989). "Microbial biomass acts as a source of plant nutrient in dry tropical forest and savanna". Nature. 338 (6215): 499–500. Bibcode:1989Natur.338..499S. doi:10.1038/338499a0. S2CID 4301023. Retrieved 29 January 2023.
105. Szatanik-Kloc, Alicja; Szerement, Justyna; Józefaciuk, Grzegorz (2017). "The role of cell walls and pectins in cation exchange and surface area of plant roots". Journal of Plant Physiology. 215: 85–90. doi:10.1016/j.jplph.2017.05.017. PMID 28600926. Retrieved 29 January 2023.
106. Donahue, Miller & Shickluna 1977, pp. 115–116.
107. Hinsinger, Philippe (2001). "Bioavailability of soil inorganic P in the rhizosphere as affected by root-induced chemical changes: a review". Plant and Soil. 237 (2): 173–95. doi:10.1023/A:1013351617532. S2CID 8562338. Retrieved 29 January 2023.
108. Gu, Baohua; Schulz, Robert K. (1991). "Anion retention in soil: possible application to reduce migration of buried technetium and iodine, a review". doi:10.2172/5980032. S2CID 91359494. Retrieved 29 January 2023. {{cite journal}}: Cite journal requires |journal= (help)
109. Lawrinenko, Michael; Jing, Dapeng; Banik, Chumki; Laird, David A. (2017). "Aluminum and iron biomass pretreatment impacts on biochar anion exchange capacity". Carbon. 118: 422–30. doi:10.1016/j.carbon.2017.03.056. Retrieved 29 January 2023.
110. Sollins, Phillip; Robertson, G. Philip; Uehara, Goro (1988). "Nutrient mobility in variable- and permanent-charge soils" (PDF). Biogeochemistry. 6 (3): 181–99. doi:10.1007/BF02182995. S2CID 4505438. Retrieved 29 January 2023.
111. Sanders, W. M. H. (1964). "Extraction of soil phosphate by anion-exchange membrane". New Zealand Journal of Agricultural Research. 7 (3): 427–31. doi:10.1080/00288233.1964.10416423.
112. Lawrinenko, Mike; Laird, David A. (2015). "Anion exchange capacity of biochar". Green Chemistry. 17 (9): 4628–36. doi:10.1039/C5GC00828J. S2CID 52972476. Retrieved 29 January 2023.
113. Robertson, Bryan. "pH requirements of freshwater aquatic life" (PDF). Retrieved 6 June 2021.
114. Chang, Raymond, ed. (2010). Chemistry. Chemistry - Chang 12Ed (12th ed.). New York, New York: McGraw-Hill. p. 666. ISBN 9780078021510. Retrieved 6 June 2021.
115. Singleton, Peter L.; Edmeades, Doug C.; Smart, R. E.; Wheeler, David M. (2001). "The many ways of making anionic clays". Journal of Chemical Sciences. 113 (5–6): 671–680. doi:10.1007/BF02708799. S2CID 97507578.
116. Läuchli, André; Grattan, Steve R. (2012). "Soil pH extremes". In Shabala, Sergey (ed.). Plant stress physiology (1st ed.). Wallingford, United Kingdom: CAB International. pp. 194–209. doi:10.1079/9781845939953.0194. ISBN 978-1845939953. Retrieved 13 June 2021.
117. Donahue, Miller & Shickluna 1977, pp. 116–117.
118. Calmano, Wolfgang; Hong, Jihua; Förstner, Ulrich (1993). "Binding and mobilization of heavy metals in contaminated sediments affected by pH and redox potential". Water Science and Technology. 28 (8–9): 223–235. doi:10.2166/wst.1993.0622. Retrieved 13 June 2021.
119. Ren, Xiaoya; Zeng, Guangming; Tang, Lin; Wang, Jingjing; Wan, Jia; Liu, Yani; Yu, Jiangfang; Yi, Huan; Ye, Shujing; Deng, Rui (2018). "Sorption, transport and biodegradation: an insight into bioavailability of persistent organic pollutants in soil" (PDF). Science of the Total Environment. 610–611: 1154–1163. Bibcode:2018ScTEn.610.1154R. doi:10.1016/j.scitotenv.2017.08.089. PMID 28847136. Retrieved 13 June 2021.
120. Ponge, Jean-François (2003). "Humus forms in terrestrial ecosystems: a framework to biodiversity". Soil Biology and Biochemistry. 35 (7): 935–945. CiteSeerX 10.1.1.467.4937. doi:10.1016/S0038-0717(03)00149-4. S2CID 44160220. Retrieved 13 June 2021.
121. Fujii, Kazumichi (2003). "Soil acidification and adaptations of plants and microorganisms in Bornean tropical forests". Ecological Research. 29 (3): 371–381. doi:10.1007/s11284-014-1144-3.
122. Kauppi, Pekka; Kämäri, Juha; Posch, Maximilian; Kauppi, Lea (1986). "Acidification of forest soils: model development and application for analyzing impacts of acidic deposition in Europe" (PDF). Ecological Modelling. 33 (2–4): 231–253. doi:10.1016/0304-3800(86)90042-6. Retrieved 13 June 2021.
123. Andriesse, Jacobus Pieter (1969). "A study of the environment and characteristics of tropical podzols in Sarawak (East-Malaysia)". Geoderma. 2 (3): 201–227. Bibcode:1969Geode...2..201A. doi:10.1016/0016-7061(69)90038-X. Retrieved 13 June 2021.
124. Rengasamy, Pichu (2006). "World salinization with emphasis on Australia". Journal of Experimental Botany. 57 (5): 1017–1023. doi:10.1093/jxb/erj108. PMID 16510516.
125. Arnon, Daniel I.; Johnson, Clarence M. (1942). "Influence of hydrogen ion concentration on the growth of higher plants under controlled conditions". Plant Physiology. 17 (4): 525–539. doi:10.1104/pp.17.4.525. PMC 438054. PMID 16653803.
126. Chaney, Rufus L.; Brown, John C.; Tiffin, Lee O. (1972). "Obligatory reduction of ferric chelates in iron uptake by soybeans". Plant Physiology. 50 (2): 208–213. doi:10.1104/pp.50.2.208. PMC 366111. PMID 16658143.
127. Donahue, Miller & Shickluna 1977, pp. 116–119.
128. Ahmad, Sagheer; Ghafoor, Abdul; Qadir, Manzoor; Aziz, M. Abbas (2006). "Amelioration of a calcareous saline-sodic soil by gypsum application and different crop rotations". International Journal of Agriculture and Biology. 8 (2): 142–46. Retrieved 13 June 2021.
129. McFee, William W.; Kelly, J. Michael; Beck, Robert H. (1977). "Acid precipitation effects on soil pH and base saturation of exchange sites". Water, Air, and Soil Pollution. 7 (3): 4014–08. Bibcode:1977WASP....7..401M. doi:10.1007/BF00284134.
130. Farina, Martin Patrick W.; Sumner, Malcolm E.; Plank, C. Owen; Letzsch, W. Stephen (1980). "Exchangeable aluminum and pH as indicators of lime requirement for corn". Soil Science Society of America Journal. 44 (5): 1036–1041. Bibcode:1980SSASJ..44.1036F. doi:10.2136/sssaj1980.03615995004400050033x. Retrieved 20 June 2021.
131. Donahue, Miller & Shickluna 1977, pp. 119–120.
132. Sposito, Garrison; Skipper, Neal T.; Sutton, Rebecca; Park, Sun-Ho; Soper, Alan K.; Greathouse, Jeffery A. (1999). "Surface geochemistry of the clay minerals". Proceedings of the National Academy of Sciences of the United States of America. 96 (7): 3358–3364. Bibcode:1999PNAS...96.3358S. doi:10.1073/pnas.96.7.3358. PMC 34275. PMID 10097044.
133. Sparks, Donald L. "Acidic and basic soils: buffering" (PDF). Davis, California: University of California, Davis, Department of Land, Air, and Water Resources. Retrieved 20 June 2021.
134. Ulrich, Bernhard (1983). "Soil acidity and its relations to acid deposition" (PDF). In Ulrich, Bernhard; Pankrath, Jürgen (eds.). Effects of accumulation of air pollutants in forest ecosystems (1st ed.). Dordrecht, The Netherlands: D. Reidel Publishing Company. pp. 127–146. doi:10.1007/978-94-009-6983-4_10. ISBN 978-94-009-6985-8. Retrieved 21 June 2021.
135. Donahue, Miller & Shickluna 1977, pp. 120–121.
136. Donahue, Miller & Shickluna 1977, p. 125.
137. Dean 1957, p. 80.
138. Russel 1957, pp. 123–125.
139. Brady, Nyle C.; Weil, Ray R. (2008). The nature and properties of soils (15th ed.). Upper Saddle River, New Jersey: Pearson. ISBN 978-0-13-325448-8. Retrieved 27 June 2021.
140. Van der Ploeg, Rienk R.; Böhm, Wolfgang; Kirkham, Mary Beth (1999). "On the origin of the theory of mineral nutrition of plants and the Law of the Minimum". Soil Science Society of America Journal. 63 (5): 1055–1062. Bibcode:1999SSASJ..63.1055V. CiteSeerX 10.1.1.475.7392. doi:10.2136/sssaj1999.6351055x.
141. Knecht, Magnus F.; Göransson, Anders (2004). "Terrestrial plants require nutrients in similar proportions". Tree Physiology. 24 (4): 447–460. doi:10.1093/treephys/24.4.447. PMID 14757584.
142. Dean 1957, pp. 80–81.
143. Roy, R. N.; Finck, Arnold; Blair, Graeme J.; Tandon, Hari Lal Singh (2006). "Soil fertility and crop production" (PDF). Plant nutrition for food security: a guide for integrated nutrient management. Rome, Italy: Food and Agriculture Organization of the United Nations. pp. 43–90. ISBN 978-92-5-105490-1. Retrieved 27 June 2021.
144. Parfitt, Roger L.; Giltrap, Donna J.; Whitton, Joe S. (1995). "Contribution of organic matter and clay minerals to the cation exchange capacity of soil". Communications in Soil Science and Plant Analysis. 26 (9–10): 1343–1355. doi:10.1080/00103629509369376. Retrieved 27 June 2021.
145. Hajnos, Mieczyslaw; Jozefaciuk, Grzegorz; Sokołowska, Zofia; Greiffenhagen, Andreas; Wessolek, Gerd (2003). "Water storage, surface, and structural properties of sandy forest humus horizons". Journal of Plant Nutrition and Soil Science. 166 (5): 625–634. doi:10.1002/jpln.200321161. Retrieved 27 June 2021.
146. Donahue, Miller & Shickluna 1977, pp. 123–131.
147. Pimentel, David; Harvey, Celia; Resosudarmo, Pradnja; Sinclair, K.; Kurz, D.; McNair, M.; Crist, S.; Shpritz, L.; Fitton, L.; Saffouri, R.; Blair, R. (1995). "Environmental and economic costs of soil erosion and conservation benefits". Science. 267 (5201): 1117–23. Bibcode:1995Sci...267.1117P. doi:10.1126/science.267.5201.1117. PMID 17789193. S2CID 11936877. (PDF) from the original on 13 December 2016. Retrieved 4 July 2021.
148. Schnürer, Johan; Clarholm, Marianne; Rosswall, Thomas (1985). "Microbial biomass and activity in an agricultural soil with different organic matter contents". Soil Biology and Biochemistry. 17 (5): 611–618. doi:10.1016/0038-0717(85)90036-7. Retrieved 4 July 2021.
149. Sparling, Graham P. (1992). "Ratio of microbial biomass carbon to soil organic carbon as a sensitive indicator of changes in soil organic matter". Australian Journal of Soil Research. 30 (2): 195–207. doi:10.1071/SR9920195. Retrieved 4 July 2021.
150. Varadachari, Chandrika; Ghosh, Kunal (1984). "On humus formation". Plant and Soil. 77 (2): 305–313. doi:10.1007/BF02182933. S2CID 45102095.
151. Prescott, Cindy E. (2010). "Litter decomposition: what controls it and how can we alter it to sequester more carbon in forest soils?". Biogeochemistry. 101 (1): 133–q49. doi:10.1007/s10533-010-9439-0. S2CID 93834812.
152. Lehmann, Johannes; Kleber, Markus (2015). "The contentious nature of soil organic matter" (PDF). Nature. 528 (7580): 60–68. Bibcode:2015Natur.528...60L. doi:10.1038/nature16069. PMID 26595271. S2CID 205246638. Retrieved 4 July 2021.
153. Piccolo, Alessandro (2002). "The supramolecular structure of humic substances: a novel understanding of humus chemistry and implications in soil science". Advances in Agronomy. 75: 57–134. doi:10.1016/S0065-2113(02)75003-7. ISBN 9780120007936. Retrieved 4 July 2021.
154. Scheu, Stefan (2002). "The soil food web: structure and perspectives". European Journal of Soil Biology. 38 (1): 11–20. doi:10.1016/S1164-5563(01)01117-7. Retrieved 4 July 2021.
155. Foth, Henry D. (1984). Fundamentals of soil science (PDF) (8th ed.). New York, New York: Wiley. p. 139. ISBN 978-0471522799. Retrieved 4 July 2021.
156. Ponge, Jean-François (2003). "Humus forms in terrestrial ecosystems: a framework to biodiversity". Soil Biology and Biochemistry. 35 (7): 935–945. CiteSeerX 10.1.1.467.4937. doi:10.1016/S0038-0717(03)00149-4. S2CID 44160220. from the original on 29 January 2016.
157. Pettit, Robert E. "Organic matter, humus, humate, humic acid, fulvic acid and humin: their importance in soil fertility and plant health" (PDF). Retrieved 11 July 2021.
158. Ji, Rong; Kappler, Andreas; Brune, Andreas (2000). "Transformation and mineralization of synthetic ¹⁴C-labeled humic model compounds by soil-feeding termites". Soil Biology and Biochemistry. 32 (8–9): 1281–1291. CiteSeerX 10.1.1.476.9400. doi:10.1016/S0038-0717(00)00046-8.
159. Drever, James I.; Vance, George F. (1994). "Role of soil organic acids in mineral weathering processes" (PDF). In Pittman, Edward D.; Lewan, Michael D. (eds.). Organic acids in geological processes. Berlin, Germany: Springer. pp. 138–161. doi:10.1007/978-3-642-78356-2_6. ISBN 978-3-642-78356-2. Retrieved 11 July 2021.
160. Piccolo, Alessandro (1996). "Humus and soil conservation". In Piccolo, Alessandro (ed.). Humic substances in terrestrial ecosystems. Amsterdam, The Netherlands: Elsevier. pp. 225–264. doi:10.1016/B978-044481516-3/50006-2. ISBN 978-0-444-81516-3. Retrieved 11 July 2021.
161. Varadachari, Chandrika; Ghosh, Kunal (1984). "On humus formation". Plant and Soil. 77 (2): 305–313. doi:10.1007/BF02182933. S2CID 45102095. Retrieved 11 July 2021.
162. Mendonça, Eduardo S.; Rowell, David L. (1996). "Mineral and organic fractions of two oxisols and their influence on effective cation-exchange capacity". Soil Science Society of America Journal. 60 (6): 1888–1892. Bibcode:1996SSASJ..60.1888M. doi:10.2136/sssaj1996.03615995006000060038x. Retrieved 11 July 2021.
163. Heck, Tobias; Faccio, Greta; Richter, Michael; Thöny-Meyer, Linda (2013). "Enzyme-catalyzed protein crosslinking". Applied Microbiology and Biotechnology. 97 (2): 461–475. doi:10.1007/s00253-012-4569-z. PMC 3546294. PMID 23179622. Retrieved 11 July 2021.
164. Lynch, D. L.; Lynch, C. C. (1958). "Resistance of protein–lignin complexes, lignins and humic acids to microbial attack" (PDF). Nature. 181 (4621): 1478–1479. Bibcode:1958Natur.181.1478L. doi:10.1038/1811478a0. PMID 13552710. S2CID 4193782. Retrieved 11 July 2021.
165. Dawson, Lorna A.; Hillier, Stephen (2010). "Measurement of soil characteristics for forensic applications" (PDF). Surface and Interface Analysis. 42 (5): 363–377. doi:10.1002/sia.3315. S2CID 54213404. Retrieved 18 July 2021.
166. Manjaiah, K.M.; Kumar, Sarvendra; Sachdev, M. S.; Sachdev, P.; Datta, S. C. (2010). "Study of clay–organic complexes". Current Science. 98 (7): 915–921. Retrieved 18 July 2021.
167. Theng, Benny K.G. (1982). "Clay-polymer interactions: summary and perspectives". Clays and Clay Minerals. 30 (1): 1–10. Bibcode:1982CCM....30....1T. CiteSeerX 10.1.1.608.2942. doi:10.1346/CCMN.1982.0300101. S2CID 98176725.
168. Tietjen, Todd; Wetzel, Robert G. (2003). "Extracellular enzyme-clay mineral complexes: enzyme adsorption, alteration of enzyme activity, and protection from photodegradation" (PDF). Aquatic Ecology. 37 (4): 331–339. doi:10.1023/B:AECO.0000007044.52801.6b. S2CID 6930871. Retrieved 18 July 2021.
169. Tahir, Shermeen; Marschner, Petra (2017). "Clay addition to sandy soil: influence of clay type and size on nutrient availability in sandy soils amended with residues differing in C/N ratio". Pedosphere. 27 (2): 293–305. doi:10.1016/S1002-0160(17)60317-5. Retrieved 18 July 2021.
170. Melero, Sebastiana; Madejón, Engracia; Ruiz, Juan Carlos; Herencia, Juan Francisco (2007). "Chemical and biochemical properties of a clay soil under dryland agriculture system as affected by organic fertilization". European Journal of Agronomy. 26 (3): 327–334. doi:10.1016/j.eja.2006.11.004. Retrieved 18 July 2021.
171. Joanisse, Gilles D.; Bradley, Robert L.; Preston, Caroline M.; Bending, Gary D. (2009). "Sequestration of soil nitrogen as tannin–protein complexes may improve the competitive ability of sheep laurel (Kalmia angustifolia) relative to black spruce (Picea mariana)". New Phytologist. 181 (1): 187–198. doi:10.1111/j.1469-8137.2008.02622.x. PMID 18811620.
172. Fierer, Noah; Schimel, Joshua P.; Cates, Rex G.; Zou, Jiping (2001). "Influence of balsam poplar tannin fractions on carbon and nitrogen dynamics in Alaskan taiga floodplain soils". Soil Biology and Biochemistry. 33 (12–13): 1827–1839. doi:10.1016/S0038-0717(01)00111-0. Retrieved 18 July 2021.
173. Peng, Xinhua; Horn, Rainer (2007). "Anisotropic shrinkage and swelling of some organic and inorganic soils". European Journal of Soil Science. 58 (1): 98–107. doi:10.1111/j.1365-2389.2006.00808.x.
174. Wang, Yang; Amundson, Ronald; Trumbmore, Susan (1996). "Radiocarbon dating of soil organic matter" (PDF). Quaternary Research. 45 (3): 282–288. Bibcode:1996QuRes..45..282W. doi:10.1006/qres.1996.0029. S2CID 73640995. Retrieved 18 July 2021.
175. Brodowski, Sonja; Amelung, Wulf; Haumaier, Ludwig; Zech, Wolfgang (2007). "Black carbon contribution to stable humus in German arable soils". Geoderma. 139 (1–2): 220–228. Bibcode:2007Geode.139..220B. doi:10.1016/j.geoderma.2007.02.004. Retrieved 18 July 2021.
176. Criscuoli, Irene; Alberti, Giorgio; Baronti, Silvia; Favilli, Filippo; Martinez, Cristina; Calzolari, Costanza; Pusceddu, Emanuela; Rumpel, Cornelia; Viola, Roberto; Miglietta, Franco (2014). "Carbon sequestration and fertility after centennial time scale incorporation of charcoal into soil". PLOS ONE. 9 (3): e91114. Bibcode:2014PLoSO...991114C. doi:10.1371/journal.pone.0091114. PMC 3948733. PMID 24614647.
177. Kim, Dong Jim; Vargas, Rodrigo; Bond-Lamberty, Ben; Turetsky, Merritt R. (2012). "Effects of soil rewetting and thawing on soil gas fluxes: a review of current literature and suggestions for future research". Biogeosciences. 9 (7): 2459–2483. Bibcode:2012BGeo....9.2459K. doi:10.5194/bg-9-2459-2012. Retrieved 3 October 2021.
178. Wagai, Rota; Mayer, Lawrence M.; Kitayama, Kanehiro; Knicker, Heike (2008). "Climate and parent material controls on organic matter storage in surface soils: a three-pool, density-separation approach". Geoderma. 147 (1–2): 23–33. Bibcode:2008Geode.147...23W. doi:10.1016/j.geoderma.2008.07.010. hdl:10261/82461. Retrieved 25 July 2021.
179. Minayeva, Tatiana Y.; Trofimov, Sergey Ya.; Chichagova, Olga A.; Dorofeyeva, E. I.; Sirin, Andrey A.; Glushkov, Igor V.; Mikhailov, N. D.; Kromer, Bernd (2008). "Carbon accumulation in soils of forest and bog ecosystems of southern Valdai in the Holocene". Biology Bulletin. 35 (5): 524–532. doi:10.1134/S1062359008050142. S2CID 40927739. Retrieved 25 July 2021.
180. Vitousek, Peter M.; Sanford, Robert L. (1986). "Nutrient cycling in moist tropical forest". Annual Review of Ecology and Systematics. 17: 137–167. doi:10.1146/annurev.es.17.110186.001033. S2CID 55212899. Retrieved 25 July 2021.
181. Rumpel, Cornelia; Chaplot, Vincent; Planchon, Olivier; Bernadou, J.; Valentin, Christian; Mariotti, André (2006). "Preferential erosion of black carbon on steep slopes with slash and burn agriculture". Catena. 65 (1): 30–40. Bibcode:2006Caten..65...30R. doi:10.1016/j.catena.2005.09.005. Retrieved 25 July 2021.
182. Paul, Eldor A.; Paustian, Keith H.; Elliott, E. T.; Cole, C. Vernon (1997). Soil organic matter in temperate agroecosystems: long-term experiments in North America. Boca Raton, Florida: CRC Press. p. 80. ISBN 978-0-8493-2802-2.
183. "Horizons". Soils of Canada. from the original on 22 September 2019. Retrieved 1 August 2021.
184. Frouz, Jan; Prach, Karel; Pizl, Václav; Háněl, Ladislav; Starý, Josef; Tajovský, Karel; Materna, Jan; Balík, Vladimír; Kalčík, Jiří; Řehounková, Klára (2008). "Interactions between soil development, vegetation and soil fauna during spontaneous succession in post mining sites". European Journal of Soil Biology. 44 (1): 109–121. doi:10.1016/j.ejsobi.2007.09.002. Retrieved 1 August 2021.
185. Kabala, Cezary; Zapart, Justyna (2012). "Initial soil development and carbon accumulation on moraines of the rapidly retreating Werenskiold Glacier, SW Spitsbergen, Svalbard archipelago". Geoderma. 175–176: 9–20. Bibcode:2012Geode.175....9K. doi:10.1016/j.geoderma.2012.01.025. Retrieved 1 August 2021.
186. Ugolini, Fiorenzo C.; Dahlgren, Randy A. (2002). "Soil development in volcanic ash" (PDF). Global Environmental Research. 6 (2): 69–81. Retrieved 1 August 2021.
187. Huggett, Richard J. (1998). "Soil chronosequences, soil development, and soil evolution: a critical review". Catena. 32 (3): 155–172. Bibcode:1998Caten..32..155H. doi:10.1016/S0341-8162(98)00053-8. Retrieved 1 August 2021.
188. De Alba, Saturnio; Lindstrom, Michael; Schumacher, Thomas E.; Malo, Douglas D. (2004). "Soil landscape evolution due to soil redistribution by tillage: a new conceptual model of soil catena evolution in agricultural landscapes". Catena. 58 (1): 77–100. Bibcode:2004Caten..58...77D. doi:10.1016/j.catena.2003.12.004. Retrieved 1 August 2021.
189. Phillips, Jonathan D.; Marion, Daniel A. (2004). "Pedological memory in forest soil development" (PDF). Forest Ecology and Management. 188 (1): 363–380. doi:10.1016/j.foreco.2003.08.007. Retrieved 1 August 2021.
190. Mitchell, Edward A.D.; Van der Knaap, Willem O.; Van Leeuwen, Jacqueline F.N.; Buttler, Alexandre; Warner, Barry G.; Gobat, Jean-Michel (2001). "The palaeoecological history of the Praz-Rodet bog (Swiss Jura) based on pollen, plant macrofossils and testate amoebae(Protozoa)". The Holocene. 11 (1): 65–80. Bibcode:2001Holoc..11...65M. doi:10.1191/095968301671777798. S2CID 131032169. Retrieved 1 August 2021.
191. Carcaillet, Christopher (2001). "Soil particles reworking evidences by AMS ¹⁴C dating of charcoal". Comptes Rendus de l'Académie des Sciences, Série IIA. 332 (1): 21–28. Bibcode:2001CRASE.332...21C. doi:10.1016/S1251-8050(00)01485-3. Retrieved 1 August 2021.
192. Retallack, Gregory J. (1991). "Untangling the effects of burial alteration and ancient soil formation". Annual Review of Earth and Planetary Sciences. 19 (1): 183–206. Bibcode:1991AREPS..19..183R. doi:10.1146/annurev.ea.19.050191.001151. Retrieved 1 August 2021.
193. Bakker, Martha M.; Govers, Gerard; Jones, Robert A.; Rounsevell, Mark D.A. (2007). "The effect of soil erosion on Europe's crop yields". Ecosystems. 10 (7): 1209–1219. doi:10.1007/s10021-007-9090-3.
194. Uselman, Shauna M.; Qualls, Robert G.; Lilienfein, Juliane (2007). "Contribution of root vs. leaf litter to dissolved organic carbon leaching through soil". Soil Science Society of America Journal. 71 (5): 1555–1563. Bibcode:2007SSASJ..71.1555U. doi:10.2136/sssaj2006.0386. Retrieved 8 August 2021.
195. Schulz, Stefanie; Brankatschk, Robert; Dümig, Alexander; Kögel-Knabner, Ingrid; Schloter, Michae; Zeyer, Josef (2013). "The role of microorganisms at different stages of ecosystem development for soil formation". Biogeosciences. 10 (6): 3983–3996. Bibcode:2013BGeo...10.3983S. doi:10.5194/bg-10-3983-2013.
196. Gillet, Servane; Ponge, Jean-François (2002). "Humus forms and metal pollution in soil". European Journal of Soil Science. 53 (4): 529–539. doi:10.1046/j.1365-2389.2002.00479.x. S2CID 94900982. Retrieved 8 August 2021.
197. Bardy, Marion; Fritsch, Emmanuel; Derenne, Sylvie; Allard, Thierry; do Nascimento, Nadia Régina; Bueno, Guilherme (2008). "Micromorphology and spectroscopic characteristics of organic matter in waterlogged podzols of the upper Amazon basin". Geoderma. 145 (3): 222–230. Bibcode:2008Geode.145..222B. CiteSeerX 10.1.1.455.4179. doi:10.1016/j.geoderma.2008.03.008.
198. Dokuchaev, Vasily Vasilyevich (1967). "Russian Chernozem". Jerusalem, Israel: Israel Program for Scientific Translations. Retrieved 15 August 2021.
199. IUSS Working Group WRB (2022). "World Reference Base for Soil Resources, 4th edition". IUSS, Vienna.
200. Sambo, Paolo; Nicoletto, Carlo; Giro, Andrea; Pii, Youry; Valentinuzzi, Fabio; Mimmo, Tanja; Lugli, Paolo; Orzes, Guido; Mazzetto, Fabrizio; Astolfi, Stefania; Terzano, Roberto; Cesco, Stefano (2019). "Hydroponic solutions for soilless production systems: issues and opportunities in a smart agriculture perspective". Frontiers in Plant Science. 10 (123): 923. doi:10.3389/fpls.2019.00923. PMC 6668597. PMID 31396245.
201. Leake, Simon; Haege, Elke (2014). Soils for landscape development: selection, specification and validation. Clayton, Victoria, Australia: CSIRO Publishing. ISBN 978-0643109650.
202. Pan, Xian-Zhang; Zhao, Qi-Guo (2007). "Measurement of urbanization process and the paddy soil loss in Yixing city, China between 1949 and 2000" (PDF). Catena. 69 (1): 65–73. Bibcode:2007Caten..69...65P. doi:10.1016/j.catena.2006.04.016. Retrieved 15 August 2021.
203. Kopittke, Peter M.; Menzies, Neal W.; Wang, Peng; McKenna, Brigid A.; Lombi, Enzo (2019). "Soil and the intensification of agriculture for global food security". Environment International. 132: 105078. doi:10.1016/j.envint.2019.105078. ISSN 0160-4120. PMID 31400601.
204. Stürck, Julia; Poortinga, Ate; Verburg, Peter H. (2014). "Mapping ecosystem services: the supply and demand of flood regulation services in Europe" (PDF). Ecological Indicators. 38: 198–211. doi:10.1016/j.ecolind.2013.11.010. Retrieved 15 August 2021.
205. Van Cuyk, Sheila; Siegrist, Robert; Logan, Andrew; Masson, Sarah; Fischer, Elizabeth; Figueroa, Linda (2001). "Hydraulic and purification behaviors and their interactions during wastewater treatment in soil infiltration systems". Water Research. 35 (4): 953–964. Bibcode:2001WatRe..35..953V. doi:10.1016/S0043-1354(00)00349-3. PMID 11235891. Retrieved 15 August 2021.
206. Jeffery, Simon; Gardi, Ciro; Arwyn, Jones (2010). European atlas of soil biodiversity. Luxembourg, Luxembourg: Publications Office of the European Union. doi:10.2788/94222. ISBN 978-92-79-15806-3. Retrieved 15 August 2021.
207. De Deyn, Gerlinde B.; Van der Putten, Wim H. (2005). "Linking aboveground and belowground diversity". Trends in Ecology and Evolution. 20 (11): 625–633. doi:10.1016/j.tree.2005.08.009. PMID 16701446. Retrieved 15 August 2021.
208. Hansen, James; Sato, Makiko; Kharecha, Pushker; Beerling, David; Berner, Robert; Masson-Delmotte, Valerie; Pagani, Mark; Raymo, Maureen; Royer, Dana L.; Zachos, James C. (2008). "Target atmospheric CO₂: where should humanity aim?" (PDF). Open Atmospheric Science Journal. 2 (1): 217–231. arXiv:0804.1126. Bibcode:2008OASJ....2..217H. doi:10.2174/1874282300802010217. S2CID 14890013. Retrieved 22 August 2021.
209. Lal, Rattan (11 June 2004). "Soil carbon sequestration impacts on global climate change and food security" (PDF). Science. 304 (5677): 1623–1627. Bibcode:2004Sci...304.1623L. doi:10.1126/science.1097396. PMID 15192216. S2CID 8574723. Retrieved 22 August 2021.
210. Blakeslee, Thomas (24 February 2010). "Greening deserts for carbon credits". Orlando, Florida, USA: Renewable Energy World. from the original on 1 November 2012. Retrieved 22 August 2021.
211. Mondini, Claudio; Contin, Marco; Leita, Liviana; De Nobili, Maria (2002). "Response of microbial biomass to air-drying and rewetting in soils and compost". Geoderma. 105 (1–2): 111–124. Bibcode:2002Geode.105..111M. doi:10.1016/S0016-7061(01)00095-7. Retrieved 22 August 2021.
212. "Peatlands and farming". Stoneleigh, United Kingdom: National Farmers' Union of England and Wales. 6 July 2020. Retrieved 22 August 2021.
213. van Winden, Julia F.; Reichart, Gert-Jan; McNamara, Niall P.; Benthien, Albert; Sinninghe Damste, Jaap S. (2012). "Temperature-induced increase in methane release from peat bogs: a mesocosm experiment". PLoS ONE. 7 (6): e39614. Bibcode:2012PLoSO...739614V. doi:10.1371/journal.pone.0039614. PMC 3387254. PMID 22768100.
214. Davidson, Eric A.; Janssens, Ivan A. (2006). "Temperature sensitivity of soil carbon decomposition and feedbacks to climate change" (PDF). Nature. 440 (7081): 165–173. Bibcode:2006Natur.440..165D. doi:10.1038/nature04514. PMID 16525463. S2CID 4404915. Retrieved 22 August 2021.
215. Abrahams, Pter W. (1997). "Geophagy (soil consumption) and iron supplementation in Uganda". Tropical Medicine and International Health. 2 (7): 617–623. doi:10.1046/j.1365-3156.1997.d01-348.x. PMID 9270729. S2CID 19647911.
216. Setz, Eleonore Zulnara Freire; Enzweiler, Jacinta; Solferini, Vera Nisaka; Amêndola, Monica Pimenta; Berton, Ronaldo Severiano (1999). "Geophagy in the golden-faced saki monkey (Pithecia pithecia chrysocephala) in the Central Amazon". Journal of Zoology. 247 (1): 91–103. doi:10.1111/j.1469-7998.1999.tb00196.x. Retrieved 22 August 2021.
217. Kohne, John Maximilian; Koehne, Sigrid; Simunek, Jirka (2009). "A review of model applications for structured soils: a) Water flow and tracer transport" (PDF). Journal of Contaminant Hydrology. 104 (1–4): 4–35. Bibcode:2009JCHyd.104....4K. CiteSeerX 10.1.1.468.9149. doi:10.1016/j.jconhyd.2008.10.002. PMID 19012994. (PDF) from the original on 7 November 2017. Retrieved 22 August 2021.
218. Diplock, Elizabeth E.; Mardlin, Dave P.; Killham, Kenneth S.; Paton, Graeme Iain (2009). "Predicting bioremediation of hydrocarbons: laboratory to field scale". Environmental Pollution. 157 (6): 1831–1840. doi:10.1016/j.envpol.2009.01.022. PMID 19232804. Retrieved 22 August 2021.
219. Moeckel, Claudia; Nizzetto, Luca; Di Guardo, Antonio; Steinnes, Eiliv; Freppaz, Michele; Filippa, Gianluca; Camporini, Paolo; Benner, Jessica; Jones, Kevin C. (2008). "Persistent organic pollutants in boreal and montane soil profiles: distribution, evidence of processes and implications for global cycling". Environmental Science and Technology. 42 (22): 8374–8380. Bibcode:2008EnST...42.8374M. doi:10.1021/es801703k. hdl:11383/8693. PMID 19068820. Retrieved 22 August 2021.
220. Rezaei, Khalil; Guest, Bernard; Friedrich, Anke; Fayazi, Farajollah; Nakhaei, Mohamad; Aghda, Seyed Mahmoud Fatemi; Beitollahi, Ali (2009). "Soil and sediment quality and composition as factors in the distribution of damage at the December 26, 2003, Bam area earthquake in SE Iran (M (s)=6.6)". Journal of Soils and Sediments. 9: 23–32. doi:10.1007/s11368-008-0046-9. S2CID 129416733. Retrieved 22 August 2021.

May 27, 2023