Soil horizon

A soil horizon is a layer parallel to the soil surface, also the decaying matter on it (plant litter), whose physical, chemical and biological characteristics differ from the layers above and beneath. Horizons are defined in many cases by obvious physical features, mainly colour and texture. These may be described both in absolute terms (particle size distribution for texture, for instance) and in terms relative to the surrounding material, i.e. ‘coarser’ or ‘sandier’ than the horizons above and below.

The identified horizons are indicated with symbols, which are mostly used in a hierarchical way. Master horizons (main horizons) are indicated by capital letters. Suffixes, in form of lowercase letters and figures, further differentiate the master horizons. There are many different systems of horizon symbols in the world. No one system is more correct – as artificial constructs, their utility lies in their ability to accurately describe local conditions in a consistent manner. Due to the different definitions of the horizon symbols, the systems cannot be mixed.

In most soil classification systems, horizons are used to define soil types. The German system uses entire horizon sequences for definition.[1] Other systems pick out certain horizons, the “diagnostic horizons”, for the definition; examples are the World Reference Base for Soil Resources (WRB),[2] the USDA soil taxonomy[3] and the Australian Soil Classification.[4] Diagnostic horizons are usually indicated with names, e.g. the “cambic horizon” or the “spodic horizon”. The WRB lists 37 diagnostic horizons. In addition to these diagnostic horizons, some other soil characteristics may be needed to define a soil type. Some soils do not have a clear development of horizons.

A soil horizon sensu stricto is a result of soil-forming processes (pedogenesis).[5] Layers that do not have undergone such processes may be simply called “layers”. Some soil scientists use the word layer in a more general way, including the horizons sensu stricto.

Horizon sequence

Many soils have an organic surface layer, which is denominated with a capital letter (different letters, depending from the system). The mineral soil usually starts with an A horizon. If a well-developed subsoil horizon as a result of soil formation exists, it is generally called a B horizon. An underlying loose, but poorly developed horizon is called a C horizon. Hard bedrock is mostly denominated R. Most individual systems defined more horizons and layers than just these five. In the following, the horizons and layers are listed more or less by their position from top to bottom within the soil profile. Not all of them are present in every soil.

Soils with a history of human interference, for instance through major earthworks or regular deep ploughing, may lack distinct horizons almost completely. When examining soils in the field, attention must be paid to the local geomorphology and the historical uses, to which the land has been put, in order to ensure that the appropriate names are applied to the observed horizons.

Example of a soil profile

O) Organic surface layer: Litter layer of plant residues, the upper part often relatively undecomposed, but the lower part may be strongly humified.

A) Surface soil: Layer of mineral soil with most organic matter accumulation and soil life. Additionally, due to weathering, oxides (mainly iron oxides) and clay minerals are formed and accumulated. It has a pronounced soil structure. But in some soils, clay minerals, iron, aluminum, organic compounds, and other constituents are soluble and move downwards. When this eluviation is pronounced, a lighter coloured E subsurface soil horizon is apparent at the base of the A horizon. The A horizon may also be the result of a combination of soil bioturbation and surface processes that winnow fine particles from biologically mounded topsoil. In this case, the A horizon is regarded as a "biomantle".

B) Subsoil: This layer has normally less organic matter than the A horizon, so its colour is mainly derived from iron oxides. Iron oxides and clay minerals accumulate as a result of weathering. In soil, where substances move down from the topsoil, this is the layer where they accumulate. The process of accumulation of clay minerals, iron, aluminum, and organic compounds, is referred to as illuviation. The B horizon has generally a soil structure.

C) Substratum: Layer of non-indurated poorly weathered or unweathered rocks. This layer may accumulate more soluble compounds like CaCO3. Soils formed in situ from non-indurated material exhibit similarities to this C layer.

R) Bedrock: R horizons denote the layer of partially weathered or unweathered bedrock at the base of the soil profile. Unlike the above layers, R horizons largely comprise continuous masses (as opposed to boulders) of hard rock that cannot be excavated by hand. Soils formed in situ from bedrock will exhibit strong similarities to this bedrock layer.

Horizons according to the Australian Soil and Land Survey Field Handbook (2009)



O horizon

The "O" stands for organic matter. It is a surface layer, dominated by the presence of large amounts of organic matter in varying stages of decomposition. In the Australian system, the O horizon should be considered distinct from the layer of leaf litter covering many heavily vegetated areas, which contains no weathered mineral particles and is not part of the soil itself. O horizons may be divided into O1 and O2 categories, whereby O1 horizons contain undecomposed matter whose origin can be spotted on sight (for instance, fragments of leaves), and O2 horizons contain organic debris in various stages of decomposition, the origin of which is not readily visible. O horizons contain ≥ 20% organic carbon.

P horizon

These horizons are also heavily organic, but are distinct from O horizons in that they form under waterlogged conditions. The “P” designation comes from their common name, peats. They may be divided into P1 and P2 in the same way as O horizons. P horizons contain ≥ 12 to 18% organic carbon, depending on the clay content.

A horizon

The A horizon is the top layer of the mineral soil horizons, often referred to as 'topsoil'. This layer contains dark decomposed organic matter, which is called "humus". The technical definition of an A horizon may vary between the systems, but it is most commonly described in terms relative to deeper layers. "A" horizons may be darker in colour than deeper layers and contain more organic matter, or they may be lighter but contain less clay or pedogenic oxides. The A is a surface horizon, and as such is also known as the zone in which most biological activity occurs. Soil organisms such as earthworms, potworms (enchytraeids), arthropods, nematodes, fungi, and many species of bacteria and archaea are concentrated here, often in close association with plant roots. Thus, the A horizon may be referred to as the biomantle.[7][8] However, since biological activity extends far deeper into the soil, it cannot be used as a chief distinguishing feature of an A horizon. The A horizon may be further subdivided into A1 (dark, maximum biologic activity), A2 (paler) and A3 (transitional to the B horizon).

E horizon (not used in the Australian system)

"E", being short for eluviated, is most commonly used to label a horizon that has been significantly leached of its mineral and/or organic content, leaving a pale layer largely composed of silicates or silica. These are present only in older, well-developed soils, and generally occur between the A and B horizons. In systems where (like in the Australian system) this designation is not employed, leached layers are classified firstly as an A or B according to other characteristics, and then appended with the designation “e” (see the section below on horizon suffixes). In soils that contain gravels, due to animal bioturbation, a stonelayer commonly forms near or at the base of the E horizon.

B horizon

The B horizon is commonly referred to as "subsoil" and consists of mineral layers which are significantly altered by pedogenesis, mostly with the formation of iron oxides and clay minerals. It is usually brownish or reddish due to the iron oxides, which increases the chroma of the subsoil to a degree that it can be distinguished from the other horizons. The weathering may be biologically mediated. In addition, the B horizon is defined as having a distinctly different structure or consistency than the horizon(s) above and the horizon(s) below.

The B horizon can also accumulate minerals and organic matter that are migrating downwards from the A and E horizons. If so, this layer is also known as the illuviated or illuvial horizon.

As with the A horizon, the B horizon may be divided into B1, B2, and B3 types under the Australian system. B1 is a transitional horizon of the opposite nature to an A3 – dominated by the properties of the B horizons below it, but containing some A-horizon characteristics. B2 horizons have a high concentration of clay minerals or oxides. B3 horizons are transitional between the overlying B layers and the material beneath it, whether C or D horizon.

The A3, B1, and B3 horizons are not tightly defined, and their use is generally at the discretion of the individual worker.

Plant roots penetrate throughout this layer, but it has very little humus.

The A/E/B horizons are referred to collectively as the "solum", the surface depth of the soil where biologically activity and climate effects drives pedogenesis. The layers below the solum have no collective name but are distinct in that they are noticeably less affected by surface soil-forming processes.

C horizon

The C horizon is below the solum horizons. This layer is little affected by pedogenesis. Clay illuviation, if present, is not significant. The absence of solum-type development (pedogenesis) is one of the defining attributes. The C horizon forms either in deposits (e.g., loess, flood deposits, landslides) or it formed from weathering of residual bedrock. The C horizon may be enriched with carbonates carried below the solum by leaching. If there is no lithologic discontinuity between the solum and the C horizon and no underlying bedrock present, the C horizon resembles the parent material of the solum.

D horizon

D horizons are not universally distinguished, but in the Australian system refer to "any soil material below the solum that is unlike the solum in its general character, is not C horizon, and cannot be given reliable horizon designation… [it] may be recognized by the contrast in pedologic organization between it and the overlying horizons" (National Committee on Soil and Terrain, 2009, p. 151).

R horizon

R horizons denote the layer of partially weathered or unweathered bedrock at the base of the soil profile. Unlike the above layers, R horizons largely comprise continuous masses (as opposed to boulders) of hard rock that cannot be excavated by hand. If there is no lithologic discontinuity between the solum and the R horizon, the R horizon resembles the parent material of the solum.

L horizon (not used in the Australian system)

L (Limnic) horizons or layers indicate mineral or organic material that has been deposited in water by precipitation or through the actions of aquatic organisms. Included are coprogenous earth (sedimentary peat), diatomaceous earth, and marl; and is usually found as a remnant of past bodies of standing water.

Transitional horizons

A horizon that combines the characteristics of two horizons is indicated with both capital letters, the dominant one written first. Example: AB and BA. If distinct parts have properties of two kinds of horizons, the horizon symbols are combined using a slash (/). Example: A/B and B/A.

Horizon suffixes

In addition to the main descriptors above, several modifiers exist to add necessary detail to each horizon. Firstly, each major horizon may be divided into sub-horizons by the addition of a numerical subscript, based on minor shifts in colour or texture with increasing depth (e.g., B21, B22, B23 etc.). While this can add necessary depth to a field description, workers should bear in mind that excessive division of a soil profile into narrow sub-horizons should be avoided. Walking as little as ten metres in any direction and digging another hole can often reveal a very different profile in regards to the depth and thickness of each horizon. Over-precise description can be a waste of time. In the Australian system, as a rule of thumb, layers thinner than 5 cm (2 inches) or so are best described as pans or segregations within a horizon rather than as a distinct layer.

Suffixes describing particular features of a horizon may also be added. The Australian system provides the following suffixes:

  • b: buried horizon.
  • c: presence of mineral concretions or nodules, perhaps of iron, aluminium, or manganese.
  • d: root restricting layer.
  • e: conspicuously bleached.
  • f: faunal accumulations in A horizons.
  • g: gleyed horizon.
  • h: accumulation of organic matter.
  • j: sporadically bleached.
  • k: accumulation of carbonates, commonly calcium carbonate.
  • m: strong cementation or induration.
  • p: disturbed by ploughing or other tillage practices (A horizons only).
  • q: accumulation of secondary silica.
  • r: weathered, digable rock.
  • s: sesquioxide accumulation.
  • t: accumulation of clay minerals.
  • w: weak development.
  • x: fragipan.
  • y: accumulation of calcium sulfate (gypsum).
  • z: accumulation of salts more soluble than calcium sulfate.

Buried soils

Soil formation is often described as occurring in situ: Rock breaks down, weathers and is mixed with other materials, or loose sediments are transformed by weathering. But the process is often far more complicated. For instance, a fully formed profile may have developed in an area only to be buried by wind- or water-deposited sediments which later formed into another soil profile. This sort of occurrence is most common in coastal areas, and descriptions are modified by numerical prefixes. Thus, a profile containing a buried sequence could be structured O, A1, A2, B2, 2A2, 2B21, 2B22, 2C with the buried profile commencing at 2A2.

Horizons and layers according to the USDA Field Book for Describing and Sampling Soils


Master horizons and layers

O: Organic soil materials (not limnic).

A: Mineral; organic matter (humus) accumulation.

E: Mineral; some loss of Fe, Al, clay, or organic matter.

B: Subsurface accumulation of clay, Fe, Al, Si, humus, CaCO3, CaSO4; or loss of CaCO3; or accumulation of sesquioxides; or subsurface soil structure.

C: Little or no pedogenic alteration, unconsolidated earthy material, soft bedrock.

L: Limnic soil materials.

W: A layer of liquid water (W) or permanently frozen water (Wf) within or beneath the soil (excludes water/ice above soil).

M: Root-limiting subsoil layers of human-manufactured materials.

R: Bedrock, strongly cemented to indurated.

Transitional horizons and layers

A horizon that combines the characteristics of two master horizons is indicated with both capital letters, the dominant one written first. Example: AB and BA. If discrete, intermingled bodies of two master horizons occur together, the horizon symbols are combined using a slash (/). Example: A/B and B/A.

Horizon suffixes

  • a: Highly decomposed organic matter (used only with O).
  • aa: (proposed) Accumulation of anhydrite (CaSO4).
  • b: Buried genetic horizon (not used with C horizons).
  • c: Concretions or nodules.
  • co: Coprogenous earth (used only with L).
  • d: Densic layer (physically root restrictive).
  • di: Diatomaceous earth (used only with L).
  • e: Moderately decomposed organic matter (used only with O).
  • f: Permanently frozen soil or ice (permafrost); continuous subsurface ice; not seasonal ice.
  • ff: Permanently frozen soil (“dry” permafrost); no continuous ice; not seasonal ice.
  • g: Strong gley.
  • h: Illuvial organic matter accumulation.
  • i: Slightly decomposed organic matter (used only with O).
  • j: Jarosite accumulation.
  • jj: Evidence of cryoturbation.
  • k: Pedogenic CaCO3 accumulation (<50% by vol.).
  • kk: Major pedogenic CaCO3 accumulation (≥50% by vol.).
  • m: Continuous cementation (pedogenic).
  • ma: Marl (used only with L).
  • n: Pedogenic, exchangeable sodium accumulation.
  • o: Residual sesquioxide accumulation (pedogenic).
  • p: Plow layer or other artificial disturbance.
  • q: Secondary (pedogenic) silica accumulation.
  • r: Weathered or soft bedrock.
  • s: Illuvial sesquioxide and organic matter accumulation.
  • se: Presence of sulfides (in mineral or organic horizons).
  • ss: Slickensides.
  • t: Illuvial accumulation of silicate clay.
  • u: Presence of human-manufactured materials (artifacts).
  • v: Plinthite.
  • w: Weak color or structure within B (used only with B).
  • x: Fragipan characteristics.
  • y: Accumulation of gypsum.
  • yy: Dominance of gypsum (≈≥50% by vol.).
  • z: Pedogenic accumulation of salt more soluble than gypsum.

Other horizon modifiers

Numerical prefixes are used to denote lithologic discontinuities. By convention, 1 is not shown. Numerical suffixes are used to denote subdivisions within a master horizon. Example: A, E, Bt1, 2Bt2, 2BC, 3C1, 3C2.

Horizons and layers according to the FAO Guidelines for Soil Description (2006)


The World Reference Base for Soil Resources (WRB) recommends the use of these horizon denominations.

Master horizons and layers

H horizons or layers: These are layers of organic material. Organic material is defined by having a certain minimum content of soil organic carbon. In the WRB, this is 20% (by weight). The H horizon is formed from organic residues that are not incorporated into the mineral soil. The residues may be partially altered by decomposition. Contrary to the O horizons, the H horizons are saturated with water for prolonged periods, or were once saturated but are now drained artificially. In many H horizons, the residues are predominantly mosses. Although these horizons form above the mineral soil surface, they may be buried by mineral soil and therefore be found at greater depth. H horizons may be overlain by O horizons that especially form after drainage.

O horizons or layers: These are layers of organic material. Organic material is defined by having a certain minimum content of soil organic carbon. In the WRB, this is 20% (by weight). The O horizon is formed from organic residues that are not incorporated into the mineral soil. The residues may be partially altered by decomposition. Contrary to the H horizons, the O horizons are not saturated with water for prolonged periods and not drained artificially. In many O horizons, the residues are leaves, needles, twigs, moss, and lichens. Although these horizons form above the mineral soil surface, they may be buried by mineral soil and therefore be found at greater depth.

A horizons: These are mineral horizons that formed at the surface or below an O horizon. All or much of the original rock structure has been obliterated. Additionally, they are characterized by one or more of the following:

  • an accumulation of humified organic matter, intimately mixed with the mineral fraction, and not displaying properties characteristic of E or B horizons (see below);
  • properties resulting from cultivation, pasturing, or similar kinds of disturbance;
  • a morphology that is different from the underlying B or C horizon, resulting from processes related to the surface.

If a surface horizon has properties of both A and E horizons but the dominant feature is an accumulation of humified organic matter, it is designated an A horizon.

E horizons: These are mineral horizons in which the main feature is loss of clay minerals, iron, aluminium, organic matter or some combination of these, leaving a concentration of sand and silt particles. However, pedogenesis is advanced, because the lost substances first have been formed or accumulated there. All or much of the original rock structure is obliterated. An E horizon is usually, but not necessarily, lighter in colour than an underlying B horizon. In some soils, the colour is that of the sand and silt particles. An E horizon is most commonly differentiated from an underlying B horizon: by colour of higher value or lower chroma, or both; by coarser texture; or by a combination of these properties. An E horizon is commonly near to the surface, below an O or A horizon and above a B horizon. However, the symbol E may be used without regard to the position in the profile for any horizon that meets the requirements and that has resulted from soil genesis.

B horizons: These are horizons that formed below an A, E, H or O horizon, and in which the dominant features are the obliteration of all or much of the original rock structure, together with one or a combination of the following:

  • residual concentration of oxides (especially iron oxides) and/or clay minerals;
  • evidence of removal of carbonates or gypsum;
  • illuvial concentration, alone or in combination, of clay minerals, iron, aluminium, organic matter, carbonates, gypsum or silica;
  • coatings of oxides that make the horizon conspicuously lower in value, higher in chroma, or redder in hue than overlying and underlying horizons without apparent illuviation of iron;
  • alteration that forms clay minerals or liberates oxides or both and that forms a granular, blocky or prismatic structure if volume changes accompany changes in moisture content;
  • brittleness.

All kinds of B horizons are, or were originally, subsurface horizons.

Examples of layers that are not B horizons are: layers in which clay films either coat rock fragments or are found on finely stratified unconsolidated sediments, whether the films were formed in place or by illuviation; layers into which carbonates have been illuviated but that are not contiguous to an overlying genetic horizon; and layers with gleying but no other pedogenic changes.

C horizons or layers: These are horizons or layers, excluding hard bedrock, that are little affected by pedogenic processes and lack properties of H, O, A, E or B horizons. Most are mineral layers, but some siliceous and calcareous layers, such as shells, coral and diatomaceous earth, are included. The material of C layers may be either like or unlike that from which the overlying solum presumably formed. Plant roots can penetrate C horizons, which provide an important growing medium. Included as C layers are sediments, saprolite, non-indurated bedrock and other geological materials that commonly slake within 24 hours, when air-dry or drier chunks are placed in water, and that, when moist, can be dug with a spade. Some soils form in material that is already highly weathered, and if such material does not meet the requirements of A, E or B horizons, it is designated C. Changes not considered pedogenic are those not related to overlying horizons. Layers having accumulations of silica, carbonates or gypsum, even if indurated, may be included in C horizons, unless the layer is obviously affected by pedogenic processes; then it is a B horizon.

R layers: These consist of hard bedrock underlying the soil. Granite, basalt, quartzite and indurated limestone or sandstone are examples of bedrock that are designated R. Air-dry or drier chunks of an R layer, when placed in water, will not slake within 24 hours. The R layer is sufficiently coherent when moist to make hand digging with a spade impractical. The bedrock may contain cracks, but these are so few and so small that few roots can penetrate. The cracks may be coated or filled with soil material.

I layers: These are ice lenses and wedges that contain at least 75 percent ice (by volume) and that distinctly separate layers (organic or mineral) in the soil.

L layers: These are sediments deposited in a body of water. They may be organic or mineral. Limnic material is either: (i) deposited by precipitation or through action of aquatic organisms, such as algae, especially diatoms; or (ii) derived from underwater and floating aquatic plants and subsequently modified by aquatic animals. L layers include coprogenous earth or sedimentary peat (mostly organic), diatomaceous earth (mostly siliceous), and marl (mostly calcareous).

W layers: These are either water layers in soils or water layers submerging soils. The water is present either permanently or cyclic within the time frame of 24 hours. Some organic soils float on water. In other cases, shallow water (i.e. water not deeper than 1 m) may cover the soil permanently, as in the case of shallow lakes, or cyclic, as in tidal flats. The occurrence of tidal water can be indicated by the letter W in brackets: (W).

Transitional horizons and layers

A horizon that combines the characteristics of two master horizons is indicated with both capital letters, the dominant one written first. Example: AB and BA. If discrete, intermingled bodies of two master horizons occur together, the horizon symbols are combined using a slash (/). Example: A/B and B/A. The master horizon symbols may be followed by the lowercase letters indicating subordinate characteristics (see below). Example: AhBw. The I, L and W symbols are not used in transitional horizon designations.

Subordinate characteristics

This is the list of suffixes to the master horizons. After the hyphen, it is indicated to which master horizons the suffixes can be added.

  • a: Highly decomposed organic material—H and O horizons.
  • b: Buried genetic horizon—mineral horizons, not cryoturbated.
  • c: Concretions or nodules—mineral horizons.
  • c: Coprogenous earth—L horizon.
  • d: Dense layer (physically root restrictive)—mineral horizons, not with m.
  • d: Diatomaceous earth—L horizon.
  • e: Moderately decomposed organic material—H and O horizons.
  • f: Frozen soil—not in I and R horizons.
  • g: Stagnic conditions—no restriction.
  • h: Accumulation of organic matter—mineral horizons.
  • i: Slickensides—mineral horizons.
  • i: Slightly decomposed organic material—H and O horizons.
  • j: Jarosite accumulation—no restriction.
  • k: Accumulation of pedogenic carbonates—no restriction.
  • l: Mottling due to upmoving groundwater (gleying)—no restriction.
  • m: Strong cementation or induration (pedogenic, massive)—mineral horizons.
  • m: Marl—L horizon.
  • n: Pedogenic accumulation of exchangeable sodium—no restriction.
  • o: Residual accumulation of sesquioxides (pedogenic)—no restriction.
  • p: Ploughing or other human disturbance—no restriction; ploughed E, B, or C horizons are referred to as Ap.
  • q: Accumulation of pedogenic silica—no restriction.
  • r: Strong reduction—no restriction.
  • s: Illuvial accumulation of sesquioxides—B horizons.
  • t: Illuvial accumulation of clay minerals—B and C horizons.
  • u: Urban and other human-made materials (artefacts—H, O, A, E, B and C horizons.
  • v: Occurrence of plinthite—no restriction.
  • w: Development of colour or structure—B horizons.
  • x: Fragipan characteristics—no restriction.
  • y: Pedogenic accumulation of gypsum—no restriction.
  • z: Pedogenic accumulation of salts more soluble than gypsum—no restriction.
  • @: Evidence of cryoturbation—no restriction.

Discontinuities and vertical subdivisions

Numerical prefixes are used to denote lithic discontinuities. By convention, 1 is not shown. Numerical suffixes are used to denote subdivisions within a horizon. The horizons in a profile are combined using a hyphen (-). Example: Ah-E-Bt1-2Bt2-2BwC-3C1-3C2.

Diagnostic soil horizons

Many soil classification systems have diagnostic horizons. A diagnostic horizon is a horizon used to define soil taxonomic units (e.g. to define soil types). The presence or absence of one or more diagnostic horizons in a required depth is used for the definition of a taxonomic unit. In addition, most classification systems use some other soil characteristics for the definition of taxonomic units. The diagnostic horizons need to be thoroughly defined by a set of criteria. When allocating a soil (a pedon, a soil profile) to a taxonomic unit, one has to check every horizon of this soil and decide, whether or not the horizon fulfils the criteria of a diagnostic horizon. Based on the identified diagnostic horizons, one can proceed with the allocation of the soil to a taxonomic unit. In the following, the diagnostic horizons of two soil classification systems are listed.

Diagnostic horizons in the World Reference Base for Soil Resources (WRB)


  • Anthraquic horizon
  • Argic horizon
  • Calcic horizon
  • Cambic horizon
  • Chernic horizon
  • Cryic horizon
  • Duric horizon
  • Ferralic horizon
  • Ferric horizon
  • Folic horizon
  • Fragic horizon
  • Fulvic horizon
  • Gypsic horizon
  • Histic horizon
  • Hortic horizon
  • Hydragric horizon
  • Irragric horizon
  • Melanic horizon
  • Mollic horizon
  • Natric horizon
  • Nitic horizon
  • Petrocalcic Horizon
  • Petroduric horizon
  • Petrogypsic horizon
  • Petroplinthic horizon
  • Pisoplinthic horizon
  • Plaggic horizon
  • Plinthic horizon
  • Pretic horizon
  • Protovertic horizon
  • Salic horizon
  • Sombric horizon
  • Spodic horizon
  • Terric horizon
  • Thionic horizon
  • Umbric horizon
  • Vertic horizon

Diagnostic horizons in the USDA soil taxonomy (ST)


Diagnostic surface horizons
  • Anthropic epipedon
  • Folistic epipedon
  • Histic epipedon
  • Melanic epipedon
  • Mollic epipedon (see Mollisols)
  • Ochric epipedon
  • Plaggen epipedon
  • Umbric epidpedon
Diagnostic subsurface horizons
  • Agric horizon
  • Albic horizon
  • Anhydric horizon
  • Argillic horizon
  • Calcic horizon
  • Cambic horizon
  • Duripan layer
  • Fragipan layer
  • Glossic horizon
  • Gypsic horizon
  • Kandic horizon
  • Natric horizon
  • Nitic horizon
  • Ortstein layer
  • Oxic horizon
  • Petrocalcic Horizon
  • Petrogypsic horizon
  • Petroplinthic horizon
  • Placic horizon
  • Salic horizon
  • Sombric horizon
  • Spodic horizon

See also



  1. Ad-hoc-AG Boden (2005). Bodenkundliche Kartieranleitung, 5. Auflage. Stuttgart: Schweizerbart.
  2. IUSS Working Group WRB (2015). "World Reference Base for Soil Resources 2014, Update 2015" (PDF). World Soil Resources Reports 106, FAO, Rome.
  3. Soil Survey Staff (2014). "Keys to Soil Taxonomy" (12th ed.). Natural Resources Conservation Service, United States Department of Agriculture.,
  4. R.F. Isbell; et al. (National Committee on Soil and Terrain) (2016). "Australian Soil Classification" (2nd ed.). CSIRO. Archived from the original on 2019-04-16. Retrieved 11 February 2016.
  5. W.E.H. Blum; P. Schad; S. Nortcliff (2018). Essentials of soil science. Stuttgart: Borntraeger Science Publishers.
  6. National Committee on Soil and Terrain (2009). Australian soil and land survey field handbook. Third edition. CSIRO, Melbourne.
  7. Johnson, D.L., J.E.J. Domier, and D.N. Johnson. 2005. Reflections on the nature of soil and its biomantle. Annals, Association of American Geographers, v. 95 (1), pp. 11-31.
  8. Wilkinson, M.T. and G.S. Humphreys. 2005. Exploring pedogenesis via nuclide-based soil production rates and OSL-based bioturbation rates. Australian Journal of Soil Research, v. 43, pp. 767-779.
  9. P.J. Schoeneberger; D.A. Wysocki; E.C. Benham; Soil Survey Staff (2012). "Field Book for describing and sampling soils. Version 3.0" (PDF). Lincoln, Nebraska: NRCS, NSSC.
  10. FAO (2006). "Guidelines for Soil Description. Fourth Edition" (PDF). FAO, Rome.

General sources

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