Proposal for geological classification and nomenclature of soils: both genetic-descriptive and compositional- mineralogical

Numerous systems with detailed classification of soil are in existence. Most of them are based on a variety of complex criteria, such as material type and properties like the amount of organic material, presence of clay layers, and the presence of oxidation or reduction iron-rich horizons, as well as depositional characteristics, its landform morphology and depositional formation processes. Many of these have been developed for use in fields such as agronomy and geotechnics. This paper focuses on the classification of the soil by determining its materials, their origin and the geological processes that shape them, following these basic assumptions: (1) The soil initially comes from the weathering of a parent substrate that can be either sedimentary deposits (for example, alluvial or fluvial) or of any type of rock (igneous, metamorphic or sedimentary), (2) the parent substrate structure is composed by original sequential facies (e.g. foliation, igneous cumulates or stratigraphic intercalation of sedimentary layers), (3) the physical and chemical weathering and the biogenic activity and productivity processes that occur in the soil modify both the original structure and the constituents of the parental substrate, resulting in the formation of new materials, the conservation of others, and the overprint of the sequential facies of the soil (horizons A, B and C) developed on the original parental sequential facies, additionally (4) some materials will be lost from the system and others will be incorporated into it. Finally, a strictly compositional-mineralogical classification of soil is also proposed, which corresponds essentially to the main groups of minerals: silicates, carbonates, phosphates, oxides and hydroxides, sulfates, organic rich matter, nitrates, sulphides, borates, native elements and halides, named in sedimentology as monomaterials, plus the polymaterials or rock fragments (RF). This classification offers an advantage when examining materials that are not genetically linked to the parent substrates, making each soil profile unique, by highlighting the role played by the parental materials in this process. This classification is intended to complement, but not replace any existing soil classification.


INTRODUCTION
The study of the soil is a growing field for multidisciplinary assessment, given its connections with crucial aspects, it is important for the sustainability of life on Earth (Scott and Pain, 2008). Critical zone, in reference to soil, is considered as the delicate skin of the planet (Brantley et al., 2007). It is composed of loose porous materials which store water, atmospheric air and nutrients, creating the best conditions to maintain roots and fauna (FAO, 2015a).
Thanks to a growing research interest, numerous systems of detailed classification of soils have been created, all of them proposed for agrological or geotechnical applications: Casagrande (1948), Birkeland (1999), Soil Survey Staff (1999, Eswaran et al. (2003), Kew and Gilkes (2006), Jahn et al. (2006), The Unified Soil Classification System (USCS) (ASTM D2487-06), Baize and Girard (2008), Geological Survey of Western Australia (2013). Given the complexity of the soils, it is also necessary to analyze them from the geological point of view, studying the relationship that exists between the parent material and the soil that is formed from it.
This document summarizes our efforts to propose a nomenclature for soil descriptions both in field and laboratory, based on their component materials. This paper establishes the baseline for the development of a conceptual framework of genetic-descriptive classification of soils, and a complementary compositional-mineralogical classification. Here we have pointed to a system that is simple but as inclusive as possible. This work uses the existing terms, addresses some clarifications and proposes new ones that aim to complement rather than replace more commonly used nomenclatures. This brief and generalized proposal of soil classification is designed only for interested readers, searchers and students inquiring in characterizing a soil in a different way, which considers the geological characteristics that the researchers in the subject are almost not taken into account, and to be able to quantify the transformations that the parental substratum have suffered to form the soil.

THEORETICAL FRAMEWORK
Regolith, term introduced by Merrill (1897), is frequently defined by geologists, engineers and agrologists as a layer of loose materials present on the external lithosphere of the Earth, they are a mixed heterogeneous deposit covering solid rock, which include dust, soil, broken rock, organic matter, minerals, gases, liquids, biogenic remains, and other related materials (Merrill, 1897;Scott and Pain, 2008;Chesworth, 2007). Most authors include any sedimentary or recently formed deposits in formation in earth regolith because they are integrated by loose and not consolidated materials, for instance, glacial deposits, colluvium, alluvium, evaporitic sediments, or aeolian deposits present on external lithospheric surface. Additionally, they also state that if earthy regolith contains a significant proportion of biological activity and productivity, they are more conventionally referred to as soil (Chesworth, 2007).
Soil deposits are defined as a coverage-mantle formed in the interface of external lithosphere of the earth and composed of altered and unconsolidated weathering materials, or materials produced as a result of the interaction between the external lithosphere of earth with any atmospheric conditions or fresh or marine water. The soil is the external part of the regolith and does not includes sedimentary deposits, by the contrary the soil is formed from sedimentary deposits, as well as igneous, sedimentary or metamorphic rocks. Moreover, we consider that it is also convenient to separate soil from other sedimentary deposits in formation or recently formed. Soils are a mixture of different materials (organic matter, rock fragments, minerals, elements, ions, gases, liquids, and living organisms, integrated into soil sequential facies (Taylor, 2006) commonly called horizons O, A, B, C). The upper part of soil deposits frequently supports life. Soils are formed depending on the following conditions: climatic (mainly temperature and moisture), biological activity and productivity, topographic (flat or slope), parental material (sequential facies, textures and composition), and incorporated materials, in a place where slowly deposition of new inorganic materials and slowly erosion-deflation processes occurred and the exposition time to weathering condition is long enough to transform some original materials into new ones.
The weathering processes that form soil are characterized by the following processes: compactionreorganization and water loss with release-leaching and denudation of soluble constituents from parental substrate such as calcium, magnesium and silica ions, and clay-layered aluminosilicates materials among others, this was discussed by Kew and Gilkes (2006); dissolution-collapse was described by Al-Amoundi and Abduljauwad (1995); erosion caused by swiftly moving water can scoop out scour holes or irregular erosion surfaces named scoured structures, this was discussed by Dvorak and Novak (1994); dehydration-hydration of materials like aluminophillosilicates, gypsum, limonite or other minerals was discussed by Middleton (2003); deposition-incorporation of inorganic materials, for example, formation of layer-clay-aluminosilicates by weathering alteration, was shown by Wilson (1975Wilson ( , 2013; conservation of physical and chemical resistant rocks and minerals (Kew and Gilkes, 2006), named here as inherited and conserved parental materials; deposition-incorporation of inorganic materials was treated by Chesworth (2007) that include e.g. aerosol (cloud and water suspension solid fine materials), sand, and gravel detritus, also of biodetritic materials (reworked organic compounds); deteriorationreorganization-transformation of inorganic materials like nucleic acids, proteins, carbohydrates, lignins, lipids and resins was shown by Pariente and Lavee (2003); incorporation-reorganization of new and preexisting materials by the biological productivity and activity was discussed by Buol et al. (1997), Retallack (1977), Birkeland (1999), and Boggs (2006); transformation of new and preexisting materials by chemical-biological processes (bacterial activity materials) was shown by Chesworth (2007); redistribution of materials (ions and clay) with formation-concentration-coating of isolated clay aggregates or structural clay and fine silt bridging materials between grains and clay layers was treated by Kew and Gilkes (2006); new crystal-precipitationcementation (iron oxides) was described by Ko (2008); formation of some structures (vadose pisolites isolated or forming layers) was shown by Peryt (1983); and finally those fissuring materials on soils induced by ice wedging and/or frost and freezing were treated by Udden (1918), Dylik and Maarleveld (1967) and Benedict (1979).

METHODOLOGY
To develop our genetic-descriptive classification and compositional-mineralogical classification of soil deposits and rocks, we analyzed and reviewed the methodology and the theoretical foundations of existing soil classifications to identify their strengths and possible contributions based on geological conditions, particularly the substrate on which the soils develops their sequential facies and the mineral compositions of the soil. Among others the classifications consulted are: Unified soil classification system (ASTM D2487-06), AASHTO soil classification system (ASTM D3282-93(2004)e1), cone penetration test (Robertson and Cabal, 2015), standard penetration test (Soil Survey Staff, 1999), genetic classification of soil horizons (Soil Survey Staff, 2014), international world reference base (WRB) soil classification system (IUSS Working Group WRB, 2015), Canadian system of soil classification (Soil Classification Working Group, 1998), classification of organic soils (Huang et al., 2009), revised classification system for regolith (Geological Survey of Western Australia, 2013). In addition to the classifications consulted, Millot (1964) proposal for clay materials in soils was analyzed. Then, we genetically defined the groups of materials that make up the soils into three types: inherited, incorporated and transformed materials. We listed the processes that vary the proportions of these materials in the soil profile, and generated a nomenclature using the variation of these materials in the composition of soil. Additionally, we applied this proposition to study five modern soil places with different kinds of parental substratum: quartz sandstone from Los Santos Formation of Lower Cretaceous, Limestones from Rosablanca Formation of Lower Cretaceous, Sienogranite from Pescadero Granite, Feldesphaticbiotite-quartz Gneiss from Bucaramanga Neis, and Recent unconsolidated fluvio torrential deposits, see Avendaño-Sánchez and Cruz-Ceballos (2017). Soil developed on quartz sandstone lithology form Los Santos Formation used here as example is located on "El Duende" cascade -"La Purnia" secondary road (La Mesa de Los Santos-Santander-Colombia, South America), coordinates with datum Bogotá X: 1'111590,048m, Y:1'252370,546m, and 1656 m.a.s.l. This sampling place corresponds geomorphologically to the upper part of a structural plateau (Mesa de Los Santos) with sub horizontal to horizontal strata (dips smaller than 5°), the geomorphological slope is smooth (inclination from 0 to 4°) according to the slope map generated from a Digital Elevation Model (DEM), the climate classification of the site is temperate semihumid (Tsh) based on climate classification Caldas-Lang 2012 (IDEAM, 2017), more detailed information in Avendaño-Sánchez and Cruz-Ceballos (2017).

General classification of soil deposits
The geological parameters that must be taken into account when studying and classifying soils are as follows: (1) The structure and the materials that integrate de soil: the structural parameters include the inherited sequence facies (Isf) from parental substratum and the soil sequence facies (Ssf) (Figure 1). The Isf, integrated by either: sedimentary stratigraphic bed sequences, metamorphic foliation, schistosity and gneissosity, or igneous homogeneous or heterogeneous cumulates. The Ssf that correspond to A, B, C horizon, the later Ssf are overprinted on the original parental substratum sequential facies (Pssf). The following 2 to 6 parameters which should be specifically considered in each of the sequence facies (Pssf, Isf, Ssf) separately, (2) the three dimensional (3D) geometric shape of the parental substratum (mantle, tabular, lenticular, etc.), (3) the internal structural characteristics (homogeneity vs heterogeneity) in terms of lamination, graded bed, or sedimentary deformation structures, or igneous or metamorphic cumulus etc., (4) the genetic materials that make up the soil deposit includes the inheritedconserved materials from parental substratum, the incorporated materials into the soil deposit and finally the transformed materials from both inherited and incorporated materials (Cruz-Guevara et al., 2017), for more specific details see Table 1, (5) the textural categories (framework, matrix, cement, pores, and clast, seudoclast and crystal size), (6) the compositionalmineralogical characteristic (Rock fragment (RF), siliceous, calcareous, organic rich, etc.).

Figure 1.
Flow chart showing the sequence of events and entities in the formation of soil, since the parental substratum is exposed to weathering process, and the different sequential facies (Sf) involved in the process.
The study of soils implies the consideration also of (7) the diagenetic factor, which involves early diagenesis (weathering and soil formation, bioperturbation, soft sedimentary deformation (SSD), early cementation and early dissolution, etc.), late diagenesis (cementation, dissolution-cavity formation, dissolutionneomorphism, dissolution-collapse, etc.), and finally also includes aspects of retrodiagenesis (Do Campo et al., 2017), (8) the tectonic factor (tectonically ductile deformations such as folds, fragile disruptions, lineations of penetrative cracks, shear zones and faults present in the soil profile), (9) Epigenesis factor, any material that has been formed by crystalline precipitation after lithification at low temperature and pressure, and located along structural elements such as faults and fractures, it includes crystalline precipitation structures and materials, veins of quartz, calcite, gypsum, etc., and excludes hydrothermal and related veins, and finally (10) the inferential time factor (succession of events).
Sequential facies is a term proposed by Taylor (2006) for the sequential intercalation of facies that characterize a soil, for the purpose of this paper, this term will be used also for the rest of sedimentary deposits, and for igneous, metamorphic or sedimentary rocks.
Sequence facies (Sf) are fundamental in soil formation, they involve some 3D shape and some lineation of mineral in any size with rhythmic intercalation. In metamorphic rocks Sf are foliation, schistosity, gneissosity, and relatives, in sedimentary deposits or rocks Sf are intercalation of beds of any composition and texture, and in igneous rocks Sf are commonly homogeneous and isotropic structures, or moderately layered plutonic structures named igneous cumulates. Igneous cumulates were described by Wager et al. (1960), for alignment of crystals with intercalation of mantles of different lavic events by differential crystallization of minerals.
The Ssf and Isf contribute significantly to the behavior of soils, for agricultural purposes and also in engineering, specifically in terms of geotechnical uses, for stability and threat, vulnerability and risk of natural slope (Patton, 1966;Patton and Deere, 1971). For example, a parental rock composed of an intercalation of very thick layers of quartz sandstone cemented by quartz, with any structural condition, offers the worst scenario for soil development regardless of weather conditions, because it does not have enough space to store water, oxygenated atmospheric air and nutrients, additionally, there is limited probability that weathering can degrade their materials. In conclusion, a soil with the above mentioned characteristics presents the worst conditions for agricultural purposes, but the best geotechnical conditions for foundation of engineering structures like buildings, bridges, etc.
If the parental rock is composed by an intercalation of clay argillosilicates, these materials develop fissility, cracks and fractures by decompression or by weathering; these conditions allow the penetration of the roots and the easy development of soil. Soils with these characteristics are good as substrate for agricultural purposes and lack the conditions necessary for the foundation of engineering structures.
The soil has different and particular facies with a sequential relationship (O, A, B, C, horizons), the geometry of the different parts of the soil, the horizons, have an irregular layered mantle shape, integrated with different kinds of materials, and positioning one part on another, with uniform or variable thickness and variable lateral extension as well. In general, there are three or four horizons integrating the soil (Bridges, 1990;Jahn et al., 2006), here referred as the term "Typical sedimentary soil sequence (Tsss)": 1) the uppermost part named O horizon, frequently correspond to the organic soil, which is mainly composed by biogenic and abiogenic incorporate materials, which are frequently transformed or degraded due to the weathering conditions; 2) the underlying of O level integrated by altered parental substratum, frequently subdivided into A, B and C horizons, characterized by each presenting a different intensity of transformation by weathering, a different amount of both incorporated and loss materials, and 3) the underlying are unaltered parental substratum (any sedimentary deposit or any type of rock). The Pssf exposed to weathering process during a prolonged space of time, and slow erosiondeflation of materials, results on the develop of an overprint of the soil horizon A, B and C over the initial Pssf (one example of this situation is presented in Figure 2).
The first approximation to the geologic and genetic classification of soil refers to the determination of their parental substratum, a parental rock soils (Prs) or a parental deposit soil (Pds), in consequence Prs overlies bedrock and Pds overlies unconsolidated sedimentary deposits. Specific examples that use this genetic classification proposal are: Parental gneiss soil, parental quartz sandstone soil, parental limestone soil, etc. It is necessary that the description of the parental substrate and their Pssf be as specific and complete.
As a complement to the genetic classification presented above, the second genetic approach to soil classification is based on the three types of genetic materials that form the soils (Cruz-Guevara et al., 2017), this proposition follows in part the scheme proposed by Millot (1964) "clay minerals in a sedimentary basin can be neoformed, inherited or transformed". In this work we also used the Birkeland (1999) scheme presented in Boggs (2006), the processes that modify the characteristics of the soil are: 1) addition to the ground, 2) transformation, 3) transfers, 4) removals, and 5) bioturbation of soil. Agreeing with this, soil materials and structures can be integrated into three types of genetic materials, see Table 1: 1) inherited and conserved materials (Icm), those biogenic and inorganic materials released by the degradation of the parent substrate caused by weathering. They are resistant materials such as rock fragments, amber, kerogen materials, and mono materials like quartz, zircon, ilmenite, among others. 2) incorporated materials (Im), those biogenic or abiogenic materials incorporated into the soil by any of the following processes: clastic deposition, chemical precipitation accumulation, biogenic productivity or activity, also the material incorporated during diagenesis; and 3) transformed, deteriorate or redistributed materials (Tdrm), those materials formed inside the soil by transformation, deterioration or redistribution process of original materials whatever inherited or incorporated. The specific materials of the soil of each of the three groups, materials inherited, conserved, incorporated and transformed, deteriorated or redistributed are presented in the Table 1. One of the most important parameters used in the classification of the soil is the intensity of the transformations they have had, this depends on: deposition rates of the sediments, the deflation intensity of the materials, the temporary exposure to the weathering conditions and the specific climatic conditions (humidity and temperature mainly). The genetic classification of the soil using TDRM, ICM and IM, and a ternary diagram is shown in Figure  3, the exposure time conditions, brief or prolonged to the weather conditions, the type of climate (arid and/or cold, humid and warm), and erosion intensity denudation (green arrow), are expressed to show their relationship with the inherited, incorporated and transformed materials and the intensity of the transformations of these materials. Light and heavy "Crystals" pseudoparticles of quartz, zircon, ilmenite, etc., inherited-conserved from igneous or metamorphic rocks.
Inherited and conserved particles (Icp): gravel, sand and mud particles inherited and conserved from clastic sedimentary parental rocks or sedimentary deposits.

Incorporated materials (Im),
those biogenic or abiogenic materials incorporated into the soil by any clastic sedimentation, chemical precipitation accumulation, biogenic productivity and activity, or by diagenetic process that include authigenic materials.
Particles (Ip): isolated deposition of gravel, sand and mud particles transported by gravity, water or wind; mud materials include clay bond aggregates formed in aerosol, water, cloud and snow, e.g. tropolites and relatives.
Natural liquids and gases materials (Inlgm): that include "atmospheric water and gas" in their natural state.
"Leaked and infilling materials" (Ilm) or younger materials piped down mechanically into the deposits through cavities (burrows or fissures) (Kidwell et al., 1986), and infilling particulate materials (mud-sand-gravel) fine or coarse grained inside of the empty natural space (poral or biological cavities). Authigenic materials (Iam): any kind of new mineral precipitation that is form or grown inside the soil deposits, include cement and relatives like silicates (quartz, feldspar, layer aluminosilicates, amorphous silica, among others), carbonates, phosphates, iron, manganese, aluminium and titanium oxide and hydroxide, sulfates and salts, nitrates and ammonium, sulphides, borates, and native elements.
Transformed-deteriorated and redistributed materials (Tdrm), those materials that formed inside the soil by TDR process of original inherited materials.
Weathering alteration materials (Wam): those materials formed by weathering transformed-deteriorated process of labile materials (e.g. feldspar, pyroxenes etc.), include layer-clay aluminosilicates minerals (e.g. kaolinite, among others), materials that look like clay particles but are not, they are pseudoparticles.

Dissolution and dissolution-collapse materials and structures (Jddcms): obliteration of unstable materials and consequently
formation of dissolution structures like, poral and cavities, stylolites and/or collapse pseudobreccias (collapse breccias of Friedman, 1997).

Ion remobilization and segregation materials and structures (Jirsms): intraestratal dissolution of unstable materials, with remobilization, segregation and precipitation of materials to form nodules, concretions and relatives
Neomorphism materials and structures (Mms): any kind of mineral that is transformed by chemical recrystallization or mineral inversion or replacement of original materials.

Mixed biological and weathering materials and structures (Mxjbwms):
any material formed by a mixed biological-weathering process, e.g, microbial-desiccation-weathering materials and structures.
Degraded biogenic-organic compounds materials and structures (Dbocms): materials formed by chemical-biogenic deteriorationreorganization-transformation of organic materials like nucleic acids, proteins, carbohydrates, lignin, lipids and resins, into gases, liquids and solids hydrocarbons and relatives.
According to the transformations suffered by the materials that make up the soil, presented in the TDRM-ICM-IC diagram (Figure 3), these systematic that partly resembles the classification for the rocks of weathering of Lavaut (2018) and saprock term (rocks with light weathering) of Trescases (1975), these four soil types are proposed: 1) Totally transformeddeteriorated and redistributed soil deposits (Tts), in which the original materials inherited or incorporated were totally transformed-deteriorated and/or redistributed; 2) heavily transformed-deteriorated and redistributed soil deposits (Hts), in which more than 66,6% original materials inherited or incorporated were transformed-deteriorated and/or redistributed; 3) moderately transformed-deteriorated and redistributed soil deposits (Mts), in which between 33,3 to 66,6% original materials inherited or incorporated were transformed-deteriorated and redistributed; and, 4) slightly transformed soil deposits (Sts), in which less than 33,3% original materials inherited or incorporated that were transformed-deteriorated and redistributed, in this type of deposits, the main materials are the materials incorporated and/or the materials inherited and conserved, in quantities from moderately to heavily. Table 2 shows the denominations for specific types of soils that appear in the ternary diagram of Figure 3.

Compositional-mineralogical classification and naming of soil deposits
The mineral composition contributes significantly to the behavior of soils, minerals and organic matter present in soils, maintains and stores nutrients, and is an important aspect of nutrient management. For example, parental substrate of the soil is integrated mainly by silicate minerals, they are 90% of the minerals present in the earth's crust, and the silicateweathering reactions do not follow the rhythm of the highest acid deposition load. Acid deposition of soil has been implicated as a factor contributing to forest decline, increase leaching of plant nutrients, decrease levels of nutrient cation, increase concentration of potentially toxic metals, alter the solubility of organic compounds, and impose changes in population of soil  Table 2. Terms applied for specific genetic classification of soil deposits, according to the transformation-deterioration and redistribution of the original materials. Delimited in the triangular diagram Figure 3.

Generic genetic classification Specific genetic classification
Totally transformed soil (Tts) Where original inherited and/or incorporated materials was totally transformed-deteriorated and/or redistributed.

Heavily transformed soil (Hts)
Ht si. Heavily transformed soil deposits with slightly original incorporated materials that are still conserved.
Ht sic si. Heavily transformed soil deposits with slightly original inherited and/or incorporated materials that are still conserved.
Ht sic. Heavily transformed soil deposits with slightly inherited-conserved parent rocks materials that are still conserved.

Moderately transformed soil (Mts)
Mt mi. Moderately transformed soil deposits with moderately incorporated materials that are still conserved.

Mt mi sic.
Moderately transformed soil deposits with moderately incorporated that are still conserved and slightly inherited-conserved parent rock materials.

Mt sic si.
Moderately transformed soil deposits with slightly inherited-conserved parent rock and slightly incorporated materials that are still conserved.

Mt mic si.
Moderately transformed soil deposits with moderately inherited-conserved parent rock and slightly incorporated materials that are still conserved.

Mt mic.
Moderately transformed soil deposits with moderately inherited-conserved parent rock materials.

Heavily and moderately incorporated
Hi st. Heavily incorporated soil deposits slightly transformed.

Hi sic st.
Heavily incorporated soil deposits with slightly inherited-conserved parent rock materials, slightly transformed.

Mi sic st.
Moderately incorporated soil deposits with slightly inherited-conserved parent rock materials, slightly transformed.

Heavily and moderately inheritedconserved
Mic si st. Moderately inherited-conserved soil deposits, with slightly incorporated materials that are still conserved, slightly transformed.

Hic si st.
Heavily inherited-conserved with slightly incorporated materials that are still conserved soil deposits, slightly transformed.

Hic st.
Heavily inherited-conserved materials soil deposits, slightly transformed.
organisms (Chesworth, 2007). There are different mineral components in the soils, many of them are very common in the other types of sedimentary deposits and rocks, the definition of the mineral classes that we took into account for the classification are based on the main mineralogical groups proposed by Dana and Ford (1922) and Dana and Hurlbut (1959). In addition, silicates, carbonates, phosphates, etc., are present in soils and other deposits and sedimentary rocks in the form of mono-materials, but are also present as rock fragments (RF), which are considered also as polymaterials. The compositional classification of soils is presented in Table 3.
Lithic rich soils: The soil rich in rock fragments (RF) or lithic, RF is a term of sedimentology which refers to any sedimentary material that retains the original characteristics of its parent rocks. The fragments of rock form in the soil both particles and also materials preserved after weathering that do not have any type of transport (pseudo-particles). Many soils are rich in RF (Bornemann et al., 2011).
Silicate rich soils: The silicates are any member of a family of minerals that contain silicon and oxygen anions, such as quartz, amorphous silica (chalcedony, glass), feldspar, zircon, mica group minerals (biotite, muscovite, etc.). Soils rich in silicate include siliceous rich soil (Silcrete), argillaceous soil formed by argillaceous weathering materials (kaolinite, montmorillonite-smectite, illite, sericite). The silicates form in the soil the following sedimentary materials: particles, pseudo particles, and authigenic materials. Particularly amorphous silica (opaline) form in the soil the following sedimentary materials: particles, biogenic, bioclastic, sedimentary crystals, weathering microcrystalline alteration, and authigenic materials. Notes: Soil has natural air and gases filling their porous space, include atmospheric air, methane and relatives, and other natural gases. Soil also has natural water and liquid filling their porous space, include meteoric water, organic liquid and relatives, and other natural liquid.
The last 8 to 11 groups of deposits or rocks are less abundant but economically important.
Carbonate rich soils: The carbonates are minerals that contain carbonate ion ( ) combined with divalent cations. Soils rich in carbonates include socalled calcrete soils, which contain calcite, aragonite, dolomite, magnesite, siderite. The carbonates form in the soil the following sedimentary materials: particles, biogenic, bioclastic, pseudo particles, sedimentary crystals, weathering alteration and precipitation microcrystalline and authigenic materials.
Phosphate rich soils: The phosphates are minerals that contains phosphate ion ( ). Soils rich in phosphate have apatite, fluorapatite, wavellite. They form in soil the following sedimentary materials: particles, biogenic, bioclastic, pseudo particles, and authigenic materials (francolite, collophanite). Soil weathering causes dissolved phosphate from primary minerals (especially as apatite, calcium phosphate, Tiessen et al., 1984) to precipitate with some cations and lead, for example, to the neo-formation of calcium phosphate in alkaline soils (Beck and Sanchez, 1994), adsorbed by functional groups of iron or aluminium oxides to form thermodynamically stable complexes (Bortoluzzi et al., 2015;Fink et al., 2016) or form biologically active organic compounds that remain as organic phosphate in soil (Conte et al., 2002;Martinazzo et al., 2007;Dodd and Sharpley, 2015).
Iron, manganese, aluminium and titanium oxide and hydroxide rich soils: They are soils with iron oxide and hydroxide materials (goethite, limonite, ferrihydrite), manganese oxides (lithiophorite, hollandite, and birnessite), aluminium hydroxide (gibbsite), and titanium oxides and hydroxides (less common). All of them form in the soil the following sedimentary materials: sedimentary crystals, weathering alteration microcrystalline materials, pseudo particles, and authigenic materials. Goethite and hematite are the most common pedogenic iron oxides, accompanied by maghemite and ferrihydrite in small amounts (Kämpf and Schwertmann, 1982;Schaefer et al., 2008;Carvalho-Filho et al., 2015). Pedogenic aluminium oxides contain mainly gibbsite found near the equatorial line. Ferrihydrite and lepidocrocite are found in poorly drained soils (Wang et al., 2013). A laterite is a soil layer that is rich in iron oxide (goethite, HFeO 2 ; lepidocrocite, FeO(OH); and hematite, Fe 2 O 3 ), also contains titanium oxides and hydrated oxides of aluminum (gibbsite, Al 2 O 3 ·3H 2 O, and bauxite). Lateritic soils may contain clay minerals, but they tend to be silica-poor. Laterites are derived from a wide variety of rocks weathering under strongly oxidizing and leaching conditions, in tropical and subtropical regions where the climate is humid.
Sulfate and salts rich soils: The sulfates are minerals that contain the anion . A salt is a chemical compound formed by cations (positively charged ions) linked to anions (negatively charged ions) by an ionic bond. Include soils with sulfates (gypsum) and salts (halite). They form in soil the following sedimentary materials: particles, weathering alteration microcrystalline materials, pseudo particles, and authigenic microcrystalline to mega-crystalline materials.
Organic rich soils: The organic compounds refer to materials with the large pool of carbon-based compounds (CHON), the basic structure of them are created directly by secretion of organisms: cellulose, Boletín de Geología -Vol. 42 Num. 1 tannin, cutin, and lignin, along with other various proteins, lipids, and carbohydrates. Soil with organic compounds include histosoil (FAO, 2015b), organic compounds form in the soils the following materials: coal, kerogen, wax, paraffin, petroleum, methane, etc. They form in soil the following sedimentary materials: particles, biogenic, bioclastic, pseudo particles, weathering alteration and diagenetic materials.
Nitrates rich soils: The nitrates are minerals with the ion with chemical formula NO 2− , they are the least common materials in sediments: nitrates and ammonium (nitratine, nitre, etc.), or organically bound nitrogen associated with sediment, also forming nitrate deposits accumulated in arid and semi-arid regions, and elevated nitrogen concentrations in soil (Holloway and Dahlgren, 2002). They form in soil the following sedimentary materials: particles, pseudo particles, weathering alteration and diagenetic materials.
Sulphides rich soils: The sulphides are minerals with inorganic anions of sulfur chemical formula S 2− . Soil rich in sulphides have pyrite and pyrrhotite. They are materials formed by biological sulfate reduction in marine anoxic environments (Trudinger, 1981). They form in soil the following sedimentary materials: particles, pseudo particles, weathering alteration and diagenetic materials.
Native elements rich soils: The native elements occur in nature in uncombined form and with a distinct mineral structure. Native elements in soil are metallic and nonmetallic minerals (gold, diamond, silver, sulphur, uranium, among others). They form in soil the following sedimentary materials: particles, pseudo particles, and diagenetic materials.

Feldsphatic quartz sandstone lithology example of Los Santos Formation
One example of the use of general terminology that combines the proposed characterizations is presented below (see Table 4 and Figure 2, 3 and 4) (Avendaño-Sánchez and Cruz-Ceballos, 2017): genetic based on the parental substrate (Prs or Pds), the genetic materials (TDRM, ICM and IM), the amount of transformation that the three types of genetic components that make up the soil have (Tts, Hts, Mts or Sts), and the compositionalmineralogical one (Lithic rich soil, silicate rich soil, carbonate rich soil, etc.).
Soil profile developed on parental feldsphatic quartz arenite of Los Santos Formation (Prs), with Ipsf 1 to 7, slight transformed (8 to 29.65%) evidenced by the presence of argillaceous matrix (kaolinite) and iron cement, moderately to heavy Icm (34 to 80%) of very fine to medium qtz slight feldspathic sand, to slight granule size particles (Ipsf 1 to 5 and 7), heavy Icm (70.614%) of argillaceous claystone (Illite) with very fine qtz sand (4.9%), with slight to moderately Im (11.386 to 30%) of coarse sand to granule-size agglutinate soil blades-shape pseudo-particles, sand-size plant fragments, roots, pores and water with TOC 3.02 to 0.386.

Inheritedconserved 50%
Very fine to medium sand-size slightly granule-size qtz particles

Inheritedconserved 34%
Very fine to medium qtz sand-size particles

TDR 18%
Argillaceous matrix and iron oxides cement

Inheritedconserved 51%
Fine to medium sand lightly silty qtz particles

TDR 19%
Argillaceous matrix and iron oxides cement 4 th Fine to medium sandstone slight feldsphatic quartzose

CONCLUSIONS
The weathering process overprint the new soil facies sequence structure of the soil (Ssf) (horizon A, B and C) over the parental facies sequence (Pssf) (e.g., bed intercalation, etc.), both facies sequence Ssf and Pssf need their recognition in the genetic geological classifications of the soil.
The Isf and the overprints Ssf contributes significantly to the behavior of soils, both for agricultural purposes, also in engineering-geotechnical soil uses, or for natural slope stability and threat, vulnerability and risk.
The genetic classification of soil has two different approaches, the first is the relationship of the soil with the parent substrate, and the second one, is based on the specific genetic materials and structures that form the soil. According to parental substratum there are Prs and Pds.
The soil has three kinds of specific genetic materials and structures, first are the inherited-conserved materials (ICM), those that come from the parental material without having undergone modifications, second are the transformed materials (TDRM), they would be those parts of the parent substratum that were altered, and three, the incorporated materials (IM), they would be all those biogenic or abiogenic materials introduced to the soil system, which were not part of the original parent material, nor of its possible transformations.
The soils can be classified according to the intensity of the transformation, which can be quantified from the percentages of the three constituents, TDRM, ICM and IM, as totally, heavy, moderately and slightly transformed, or heavily inherited or conserved soils.
As a complement to the genetic classification and because the mineral composition contributes significantly to the behavior of soils, it is necessary to propose the use of compositional-mineralogical classification of the soil as well: soil rich in lithics, or silicates, or carbonates, or mixed like silicate and organic, or organic shale rich soil.
Finally, it is convenient to use in the genetic classification of soils, and integrate it into a complete classification, genetic-textural with compositional-mineralogical.