Printer Friendly

Interrelationships between soil cover and plant cover depending on land use/Muld- ja taimkatte vastastikused seosed soltuvalt maakasutusest.


Soil cover is a determining factor in the development of plant cover and its diversity (Laasimer 1965; Chertov 1981; Ibanez et al. 1998). In every region of the world the composition and properties of soil cover have certain distinctive regional singularities (Deckers et al. 1998; IUSS 2006; Toth et al. 2008). The composition and properties of each soil type in a soil cover are inherited from soil parent material. The parent material variability (or geodiversity) may be caused by soil texture variations (from sand to clay), mineralogical and chemical composition, calcareousness and acidity. The pattern of soil cover induced by geodiversity (or pedodiversity) in turn plays a decisive role in forming the plant cover of natural areas and its floristic composition. For better understanding of mutual influences of soil cover and plant cover in a geographical region, the feedback influences of their functioning and main components (soil, plant) should be studied at the ecosystem level, on typical-to-region soil types and primarily within the specific management conditions (Fisher et al. 2002; Bazilevich & Titljanova 2008; Paal et al. 2011).

Research on soil-plant relationships is needed for arrangement of land management based on an ecosystem approach and to explain pedo-ecological causes of plant cover diversity. As the character of plant cover is greatly influenced by land management, soil-plant relationships should be studied comparatively in natural and cultivated ecosystems. There is much research in which soil-plant interrelationships (expressed by productivity and biological cycling) are treated systematically in accordance with pedo-climatic conditions and land use (Kolli 1987; Targulian & Krasilnikov 2007; Bazilevich & Titljanova 2008), but we found only a few studies about pedo-diversity as a basis for biodiversity (Karpachevskij 1977; Ibanez et al. 1998; Guo et al. 2003).

In Estonia, many studies deal with soil-plant interrelationships in the pedo-ecological conditions, with adequate emphasis on the role of soils in the formation and functioning of ecosystems (Sepp 1962; Laasimer 1965; Lohmus 1973; Reintam 1997b; Kont et al. 2004; Arold 2005). Additionally, valuable research is available in which soil is treated in complex with other ecological conditions, and which emphasizes the coenological and floristic aspect of system functioning (Krall et al. 1980; Zobel 1992; Laasimer & Masing 1995; Paal 1997; Paal et al. 2010). Both research directions have been of equal value in enlarging our understanding of functional particularities of forest, grassland and agro-ecosystems in the northeastern edge of the European Plain (EC 2005).

Interrelationships between soil cover and plant cover are analysed on the basis of sampled soil groups (or soil associations). For this purpose the four-link cross section or discrete pedo-ecological sequence (PES) of soils, which is composed of key regional soils and characterizes Estonian normal (or postlithogenic) mineral soils (from drought-prone skeletal calcareous rendzinas to wet acid sandy gley-podzols), is used (Kolli et al. 2008). The abnormal (or synlithogenic) mineral soils are not treated in this work.

The main tasks of the soil-plant interrelationships study are (1) to elucidate main pedo-ecological characteristics of the PES soil groups and suitability for plant covers (by species, associations, crops); (2) to compare and evaluate properties of soil groups from the aspect of productivity, sustainability, biodiversity and environment protection ability and (3) to prove the importance of ecologically sound matching of local area soil (soil cover) with suitable plant cover (forests, grasslands, crops) from the environmental protection aspect.

The study of interrelationships on the basis of key soil groups at the ecosystem level enables us (1) to emphasize the importance (or site) of specific biodiversity of soil type in treating soil-related aspects of biodiversity and (2) to characterize the influence of land-use change on soil properties, by means of comparative analysis of natural and cultivated ecosystems formed on the same soil types.


General methodological principles

The basis of the research is an ecosystem approach, with special interest in interrelationships between soil cover and plant cover (as main components of terrestrial ecosystems). The stated problems are treated from the pedo-centric viewpoint: the ecosystems for research were selected on the basis of soil cover as the determining component in the formation and development of an ecosystem. The soil groups selected for comparative analysis are presented in Table 1 and Fig. 1. All four sampling soil groups differentiate substantially from each other by main soil properties (calcareousness, acidity, nutrition conditions, profile fabric and characteristics of humus cover). Therefore, the differences between various soil groups are significant, but the coincidence of their properties is insignificant.

Soil names and their codes in the tables and text are given according to the Estonian Soil Classification (ESC) (ELB 2012). Besides the ESC, for the purpose of harmonization, the internationally recognized World Reference Base for Soils (WRB) was used (IUSS 2006), which also allows comparison of soil groups via widely known soil qualifiers (Table 2). In our databases soil texture is given as a rule after Kachinsky (1965). The accordance of classification systems elaborated for characterization of soil texture (Kachinsky versus WRB) and of different moisture conditions of plant cover, humus cover and soil cover are presented in Table 3.

A PES of soils was used not only for the analysis of soil-plant relationships, but also for the study of changes in interrelationships connected with land use change (Fig. 2). The comparative research into natural and cultivated ecosystem components--soil cover, plant cover and humus cover (formed by the interaction of the first two covers)--was conducted within the limits of adequate four soil groups.


Soil cover (or solum) embraces the superficial earth layer or soil resource influenced by soil-forming processes. Soil cover depth extends from the surface to the unchanged parent material, or the C horizon. In the presence of the BC horizon, the thickness of soil cover was measured to the middle of the BC horizon. Soil cover consists of humus cover (topsoil) and subsoil. Humus cover (topsoil or epipedon) encompasses the most active superficial soil component, which is closely coupled with plant cover and via which the dominant component of carbon cycling takes place. Humus cover consists of the forest floor, humus or raw humus and peat horizons.

The smallest classification unit identified following soil-forming processes (soil genesis) is a soil species, according to the ESC. Soil species are subdivided into varieties on the basis of texture. The PES of soils is formed on the background of certain (optional) soil-forming (pedo-ecological) conditions; its purpose is to provide representative and comparative characterization or cross section of soil cover of a particular region.

Climatic and pedo-ecological conditions of Estonia

Local climatic conditions, with typically warm summers and moderately mild winters, place Estonia in the temperate zone of the Atlantic-continental region. Mean annual air temperature varies within +4.5-6.0[degrees]C and annual precipitation is 600-700 mm (Jaagus 1999).

Estonian soil cover is characteristic of northeastern Europe, where due to relatively cold and humid conditions, gley- and mire soils dominate (Toth et al. 2008). The dominant parent materials are derived from glacial and aquaglacial Quaternary deposits. Pleistocene tills make up approximately half of the parent material of mineral soils. Glaciofluvial, glaciolacustrine, alluvial and aeolian sediments re-worked from tills are distributed throughout the tills (Raukas 1995).

Estonian pedo-ecological conditions are favourable for the formation of soil resulting from organic carbon accumulation in topsoil and the leaching of nutrients by podzolization (Reintam 1998). The mobilization of humus into biological weathering and intensive turnover of substances in the soil-plant system are also induced in these conditions (Reintam 1997a, 2007). The soil cover of Estonia is relatively varied, due to the alternation of carbonate and humus-rich soils with acid soils which are relatively poor in nutrients and organic matter, and, conversely, the interchanging of the soil moisture regime from dry to wet.

Normally developed mineral soils form ca 72% of total Estonian soil cover (Kolli et al. 2009). The decreasing orders of their textures (loam 37%, sand 34%, sandy loam 22%, clay 7%) and moisture regimes (wet 47%, fresh 30%, moist 20%, dry 3%) are given after Kokk (1995). Approximately 53% of soils are formed on calcareous and ca 47% on non-calcareous parent material.

In terms of plant cover, Estonia belongs to the transitional area between south-taiga forest and spruce-hardwood subzones, located in the southern part of the boreal forest zone (Laasimer & Masing 1995). Floristically, Estonia belongs to the boreal mixed-forest sub-region, where plant cover is relatively rich in species (Kull & Zobel 1991). Due to human influence, plant cover may be classified as natural (forest), semi-natural (grasslands, drained wet mineral soils) and cultivated (arable lands). The grassland vegetation is mostly of secondary origin, having been formed under a long-lasting influence of haymaking and pasturing (Laasimer & Masing 1995). In recent decades, intensive afforestation of both grasslands and arable lands has occurred (Astover et al. 2006).

Methods used for assessments and calculations

The analysis is based on qualitative and quantitative parameters of ecosystems. Among qualitative parameters, along with WRB qualifiers, local classification systems (soils, forest site type, humus cover types, soil agro-groups, natural grasslands, environmental protection ability) were used.

Quantitative parameters for characterization of soil groups (soil organic carbon and organic matter pools, agrochemical parameters, pedometrics of soil profiles) were taken from the database 'Pedon' formed mainly on the basis of our research (Kolli 1987), from the serial edition Soils of the Estonian SSR in Numbers (EAP 1989) and other published works on the studied soils (Asi et al. 2004; Kolli et al. 2010).

For estimation of total phytomass and annual phyto-productivity (APP) of forest ecosystems, the methods employed by the International Biological Program were used (Rodin et al. 1968; Kolli 1987). To accumulate the comparative data of soils in the sampling areas, we selected forests of approximately the same age (premature to mature) and stand stock density (0.6-0.9) (Kolli 1987). The phytomass and APP for tree and underwood layers were determined by model trees; the total phytomass of ground vegetation in forests, and of arable and grasslands ecosystems, was found by means of test plots (model plants on cultivated areas). The APP of herbaceous plants was established by the maximum phytomass of the vegetation period. For estimation of productivity level, long-term cereal yields on arable lands and hay yields on grasslands were also used.

Soil quality classes were used for comparative analysis of soil group productivity. The soil quality evaluation tables and formulae may be qualified as particular models elaborated on the basis of large amounts of experimental field data. The forest quality index was found by height of dominant trees at a certain age. The quality of arable soils was determined by soil type, texture, and depth and humus content of the A-horizon, but for grassland soils, according to yield. The instructions for determination of soil quality may be regarded as models, where, given the correct input parameters, the adequate-to-actual soil quality output (point, class) is received (ELB 1992). Suitability of soil for cultivated crops was estimated in a 10 point scale (Kolli 1994). For statistical analysis the program STATISTICA 7 was used.

Organic carbon concentration was determined by wet digestion of carbon with acid dichromate, extractable acidity by titration with 0.1 M NaOH after adding 1 M C[H.sub.3]COONa solution and soil reaction ([pH.sub.KCl]) in 1 M KCl 1 : 2.5 (Vorobyova 1998). The basic cations were determined by 1 M CH3COONa extraction procedure (SPAC 1992). Cation exchange capacity (CEC) and percentage base saturation were calculated according to the sum of bases and extractable acidity. The results of analyses are expressed in pools (or superficial densities) per humus cover and soil cover (or solum) as a whole on the basis of soil bulk density.


Nomenclature, distribution and properties of soil groups

The four soil groups selected for analysis represent ca 1/3 of the total area of Estonian normal mineral soils (Table 1, Fig. 1). The representative pedo-ecological cross section rendzinas [right arrow] brown soils [right arrow] pseudopodzolic soils [right arrow] gley-podzols starts with drought-prone soils rich in calcareous limestone. The next two links of PES are the most broadly acknowledged for wide-range agricultural use (forming ca 44% of arable land), medium-textured high-quality automorphic soils. Brown soils are distributed in the northern and central regions, pseudopodzolic soils, in southern Estonia. The PES ends with permanently wet and strongly acidic, low-productivity sandy soil.

The WRB qualifiers (modifiers) that were used for characterizing and comparing the soil groups are presented in Table 2. By the grouped list of qualifiers, where the main reference soil characteristics are also given (1st part of qualifiers), the significant pedo-genetic difference between sampling soil groups may be asserted. The only overlapping characteristics may be found for qualifiers albic and dystric, which are common for Albeluvisols (pseudopodzolic soils) and Epigleyic and Fibrihistic Podzols (gley-podzols), and luvic, which is common for Luvisols (lessive brown soils) and Albeluvisols.

Soil texture has the basic role in the development of soil properties in natural conditions (Table 3). The sampling soil groups differ substantially in the dominant fine earth textures (sand, loamy sand, loam) and in their gravel (from absent to excessive) stages. Unlike texture, moisture conditions may be profoundly transformed by drainage: the moist soils of group 3 may, in transformation, become similar to fresh soil, and wet and peaty soils (group 4), similar to moist soils. An important qualitative characteristic of soil is its humus cover type (or humus form), which reflects soil humus status, biological activity and textural-mineralogical potential of both topsoil (epipedon) and subsoil, and therefore the entire soil cover.

The generalized characteristics of sampling soil groups are presented in Table 4 and Fig. 3. The thickness of soil cover depends first on the development of eluvial processes in soil. The CEC of soil cover as an integrated parameter depends on both the nature of organic and mineral components and soil cover depth. Of great indicative value is soil texture, which is expressed by physical clay concentration (particles < 0.01 mm by Kachinsky 1965, adequate to which is the sum of particles of fine silt and clay by the WRB) and stock. In ecological research the stock of organic carbon and nitrogen concentration in different soil layers is also very important. With increasing soil acidity and stages of eluviation and gleyification, the accumulation of non-decomposed organic matter constituting the forest floor (exogenous organic carbon) increases considerably. This is accompanied by transforming humus quality, as instead of humic humus, fulvic humus is formed.

Each of the four soil groups may be subdivided into subgroups, according to pedo-genetic differences. These differences are caused by various features (Table 1); in some cases the geographical region of soil distribution (as determinant of soil-forming conditions) is of great importance.

Soil associations of rendzinas (group 1), which are distributed on the undulating till and flat limestone plains of North and Northwest Estonia, and on the islands, differ in terms of parent material fabric (formed on limestone or calcareous pebbles and shingle). Rendzinas are characterized by shallow soil profiles (O-A-R for Kh and O-A-(B)-C for Kr and Kk) in natural areas. The dominant fine earth texture (particles with diameter < 1 mm) of both soils is loam. Therefore, dominant soil varieties in this group are medium-textured (loamy) limestone rendzinas (Kh, 52%) and pebble rendzinas (Kr, 48%). The light-textured shingle rendzinas (Kk) occur only to a reduced extent (< 1%) on coastal ridges.

Rendzinas have a high base saturation stage, due to a high percentage of limestone. The humus cover is shallow and rich in calcareous gravel. These soils are susceptible to drought, which is a limiting factor for plant growth. The properties of Estonian rendzinas and their interrelationships with plant cover have been addressed in numerous studies (Sepp 1960, 1962; Lillema 1962; Lohmus 1974; Laasimer & Masing 1995; Paal 1997; Sammul et al. 2003).

Brown soil associations found in group 2 have a cambi-argic profile formed by argillization in situ or by argi-eluviation in rich non-siliceous sesquioxides and biologically active conditions (Reintam 1998). Brown soils (Ko, KI, Kor) are formed mainly on calcareous yellow-grey till (> 95%), under favourable hydrothermal, redox and biological relationships; the calcareous red-brown till (< 5%) is a parent material only to a reduced extent. By natural drainage, brown soils are classified as well-drained. In the course of soil survey four soil varieties were identified: typical (47%) and lessive (30%) loamy brown soils, and typical (13%) and lessive (10%) brown soils on sandy loam under-layered by calcareous loam. Soils formed on red-brown till soils are also included in the latter textural group. Brown soils have favourable conditions for plant growth (substantial water holding capacity, relatively high CEC, favourable hydrophysical properties, suitable air and water regimes). Classification, properties and soil-plant relationships of Estonian brown soils have been thoroughly investigated (Laasimer 1965; Reintam 1973, 1998; Paal 1997; Paal et al. 2010).

Pseudopodzolic soil associations of group 3 (formed without or with gleyzation) are distributed mostly on undulating reddish-brown till plains in southern Estonia. They were developed on two-layer deposits, where loamy sand (or silt) lay on loamy till. The main soil-forming processes in these soils are ferrolysis with Fe-segregation, deferritization and surface gleying (Reintam 1998). These conditions are favourable for the formation of mobile humus as well as for intensive biological weathering and turnover of substances in the plant-soil system.

Among fresh, moderately well-drained pseudopodzolic soil (LP) associations with normal moisture conditions on red-brown tills, the dominant soil texture is loamy sand on loam. The ratio of soil variety of loamy sand on loam to the variety with loam texture is 9 : 1. If formed on yellow-grey till pseudopodzolic soils, the ratio of the same soil varieties is 2 : 1. The gleyed (moist, somewhat poorly drained) pseudopodzolic soils (LPg) are formed on red-brown till and their texture is loamy sand on loam. Therefore, soils (76%) that formed on red-brown tills dominated over the formed yellow-grey (24%) and normally moist (fresh) soils (75%) dominated over gleyed (moist) pseudopodzolic soils (25%).

In rainy periods, the textural discontinuity of pseudopodzolic soils causes excessive water to persist in a contact layer between the two different materials. The water regime of these soils is relatively unstable as they may dry out in droughty periods. In forests their topsoil is predominantly acid, but their subsoil may have a neutral reaction. The functioning, properties and classification of Estonian pseudopodzolic soils were broadly treated by Reintam (1973, 1997b) and Kolli (1987).

Gley-podzols and peaty podzols (group 4) were developed on acid sands in permanently wet moisture conditions, which cause the formation of a thin peaty forest floor (on LG) or shallow peat horizon (on LG1) instead of a humus horizon. These soils are divided into two varieties according to the degree of paludification, which is reflected in the soil profile by the degree of soil mineral part gleyification and by the extent of peat forming in the epipedon. The percentage ratio of gley-podzols and peaty podzols for their specific area is 58 : 42, but for the overall forest the ratio is 62 : 38. In terms of natural drainage, gley-podzols may be classified as poorly drained and peaty podzols as very poorly drained (SSDS 1993). Although podzolization is an important process in their formation, to divide them according to podzolization degree is not meaningful. But, regarding podzolization, different kinds of iron-sesquioxide and humus accumulation spodic horizons, varying in horizon thickness and degree of cementation (from non-cemented to strongly cemented), may be formed. The interrelationship between gley-podzols and plant cover has been discussed in relation to forests (Lohmus 1973, 1974; Valk & Eilart 1974; Chertov 1981).

The PES soils considered in our work do not characterize the full range of normal mineral soils. For example, the hydromorphic gley-soils are not analysed. These have a sophisticated soil-plant relationship, or the typical podzols and podzolic soils formed on well-drained acid sands, all of which are widely distributed in Estonia.

Characterization of plant covers of soil groups

Soils may be characterized indirectly by forest site type and grassland type, as the floristic composition of aboveground vegetation largely reflects (depending on external influences) the plant growing properties of the soil cover (Krall et al. 1980; Paal 1997; Lohmus 2006). Natural plant associations indicate the soil water regime, nutrient supply and acidity, verifying with this the soil type (Zobel 1992; Zinko et al. 2006). The forest site types distinguished by Lohmus (2006) and grassland types established by Krall et al. (1980) for the studied soils are given in Table 5 and Fig. 2A, C. On cultivated soils approximately the same task is associated with soil agro-groups, which have been created on the basis of soil texture and moisture conditions for characterization of the suitability of soil for agricultural purposes (ELB 2012).

The generalized plant cover characteristics for the studied soils in different management conditions are presented in Table 6. It appears that our selection of the above-ground structure of forest ecosystems (floristic composition, variously functioning layers and the relative role of phytomass of different origin) adequately reflects the main soil properties and differences among soil groups. Of course, in alternative conditions of the tree layer (clearings, young and open stand), the study of the influence of soil properties on plant cover and vice versa is complicated. In the case of forest ecosystems, brown and pseudopodzolic soils have the highest total aboveground phytomass, and rendzinas and gley-podzols, the lowest. Among the number of species within the different ecosystem layers, we counted only those which have at least minimal measurable functional importance. The richest, according to the number of species, are forest ecosystems on brown soils, followed by rendzinas.

The floristic composition of plant cover on rendzinas and gley-podzols differs significantly from all others, but the differences in the composition between brown and pseudopodzolic soils are not as clearly visible. The ground vegetation and underwood are richer in plant species and are more developed on brown soils than on more acid pseudopodzolic soils. The only exception is a more abundant shrub layer on gley-podzols.

In grassland ecosystems with brown lessive and pseudopodzolic (non-gleyed) soils, a substantial extent of overlapping plant associations with key species Agrostis capillaris, Festuca rubra, Trifolium repens and Anthoxantum odoratum is observed. Such associations (Trifolio repentis-Festucetum rubrae, Agrostio capillaries-Trifolietum repentis, Agrostio capillaries-Anthoxanthetum and others) were formed on previous arable land under the influence of cattle grazing (Paal 1997).

A good instrument for determining agro-ecological characteristics of arable soils is the ten-point scale soil suitability rating for crops (Kolli 1994; Table 6). The phytomass of weeds and their floristic composition are an important pedo-ecological indicator for characterizing arable soil properties (as well as cultivated grasslands) (Laasimer 1965; Bender 2006; Older 2007). The weed species which reflect arable land status and site properties are very numerous and ambiguous (Lososova et al. 2004). The presence of certain weed species depends, first of all, on cultivated crops and the agrotechnology applied (Bender 2006; Older 2007). The following weed species indicate arable soil properties: rendzinas--Anthemis tinctoria, Rubus caesius, Sinapis arvensis; brown soils--Thlaspi arvense, Potentilla arvense, Soncjus sp.; pseudopodzolic soils--Viola arvensis, Scleranthus annuus, Raphanus raphanistrum and drained podzolic gley-soils--Ranunculus repens, Polygonum persicaria, Juncus sp., as they may frequently be found in association with other species.

The best characteristics for comparative analysis of the functioning of soil groups are the directly determined productivity parameters formed on their ecosystems (Table 7). The total phytomass of forest and its tree layer may be taken as an indirect parameter, on which the development of above-ground vegetation and underwood (among this re-growth) depends. The best characteristic for the analysis of functioning efficiency of the forest ecosystem is its APP, which correlates strongly with forest quality classes and the annual soil organic carbon balance (Fig. 4). As an indicator of the productivity of arable soils, it is rational to use the phytomass of specific species for testing. We used the above-ground phytomass of barley determined at the time of its maximum development.

Very low productivity is characteristic of natural grasslands formed on wet and peaty podzols. These natural grasslands have relatively good hay yield, when the wet/peaty podzol is transformed into (sod-)podzolic gley-soils. The same level of productivity is also found in semi-natural grasslands formed on set-aside, previously cultivated, sod-podzolic sandy gley-soils.

Estimates (soil quality points and classes) which enable quantitative comparisons of soil groups in the limits of certain land use type, whereas the principles used in these estimations are very different by land use (arable, forest and grasslands), are presented in Table 8. Soil quality (points, classes) of arable land reflects the potential productivity of soils with great accuracy. The actual productivity in agricultural land depends greatly on inputs of mineral and organic fertilizers, as well as on the selection of cultivated plant species. A stronger correlation between soil quality classes and alternative productivity characteristics (total phytomass, APP) may be found in the case of forest ecosystems. Annual phytoproductivity correlates well with soil environmental protection ability, which may treated as integrated indices of ecosystem functioning (Fig. 4D).

Land use and land use change

The best soils have been taken into agricultural use during the last century and in most of Estonia optimum land use is close to its limit. Most of the best soils, in terms of texture, moisture conditions, fertility and absence of constraints, are used for agriculture. However, specific corrections (such as reforestation and amelioration) are needed to use the remaining local land.

The arable land pattern of Estonia was formed almost entirely by cultivation of forest land. The preferred soils for cultivation were thick rendzinas, typical and lessive brown, pseudopodzolic and podzolic soils (Kokk 1995). The dominant textures of arable soils nowadays are loam and loamy sand (totalling 77%). At present, approximately half of the total Estonian soil cover lies under forests, where mire soils, gley-soils and podzols have dominated. The suitability of brown and pseudopodzolic soils (as soils of universal use) for various crops is much higher compared to rendzinas and gley-podzols (Table 6). The pebble rendzinas are suitable for deep-rooted species such as alfalfa (Medicago sativa) and white melilot (Melilotus albus).

Gley-podzols and peaty podzols are classified as typical forest soils because of their unsuitability for cultivation. Yet, to a limited extent (<0.5%), these soils have also been taken into agricultural use, following intense artificial drainage and liming. However, instead of gley-podzols and peaty podzols, podzolic gley-soils with oligotrophic raw humus were formed (Table 3). Such transformation may also occur in the course of natural processes, caused by destruction of the tree layer and development of the grass layer. On arable land and on natural grassland, podzolic gley-soils have formed in > 96% of cases, instead of gley-podzols and peaty podzol. Therefore, in analysing changes in land use of group 4 soils, the properties of gley-podzols (gley-, peaty or LG and LG1) and podzolic gley-soils (LkG) formed on sands are compared (Table 9).

Land use changes in both directions may take place: natural land is cultivated, and arable lands are set aside, although the causes of these changes may vary widely. Common to all these processes, however, is that the subsoil rests practically unchanged (potential fertility remains), and that topsoil functioning should be arranged in accordance with the production capability of soil varieties.

In the land use dynamics of the studied soil groups, the clearly recognizable regularities, which are characteristic of the entire Estonian soil cover, may be followed. As a rule, most of the arable land has been formed from former forested areas. In the establishment of arable lands in northern and central Estonia, brown soils (together with their gleyed species) play the most important role, while in southern Estonia, the pseudopodzolic soil associations predominate. At the present time only a limited area of these soils is under forests and grasslands. The typical forest soils of group 4 are used as arable soils and grasslands only in exceptional situations. The agricultural use of rendzinas depends not so much on their suitability and fertility, as on geographic location and historical situation.

In 1955-1990, massive land reclamation, including the liming of acid arable soils, application of organic and mineral fertilizers and deepening of arable horizons took place. Nowadays, less favourable areas of arable land are set aside and large areas of semi-natural grasslands are abandoned to natural re-afforestation processes (Astover et al. 2006).


Soil type-specific pedo-ecological analysis of soil-plant interrelationships

The influence of soils (on group, type, species or variety level) on plant association and vice versa is the key question in studying soil-plant interrelationships. In natural and semi-natural areas forest and grassland plant covers were developed in accordance with soil properties and local climatic conditions. As a result of this mutual influence plant associations with a specific appearance were formed. Identification of forest site and natural grassland types and the plant-growing capacity of their soils, on the basis of the floristic composition of vegetation, was used successfully in practical forestry and to some extent in grassland husbandry during the last century (Valk & Eilart 1974; Krall et al. 1980; Paal 1997; Lohmus 2006).

Is there a sense to develop more precise, detailed approaches for characterizing soils by means of site, or are there better alternatives? It seems that, at present, the approach described above has run its course, due to its inherent uncertainties. Obviously an attempt to characterize pedo-ecological site conditions on the basis of the floristic composition of ground vegetation in more detail is rather suspicious, in view of the insufficient 'fine tuning capacity' of plant cover. In addition, the floristic composition may be easily influenced by different external conditions (Tamme et al. 2010; Lindborg et al. 2012) and stage of development (e.g. age of the tree layer in forests, vegetation period on grasslands).

On the other hand, available site-specific soil information exists in the form of large-scale soil maps and typical soil profiles (calculated on the basis of hundreds of single profiles) on the soil varieties level (Kolli et al. 2008; ELB 2012). At present it is possible to analyse the soil-plant interrelationships not only on soil groups, but at more detailed (species, variety) taxonomic levels. Therefore, it is best to characterize forest soil (edaphic) conditions directly based on soil variety properties. Data on humus cover properties add precision to this process. Comparison of both kinds of site characterization methods, (1) according to ground vegetation and (2) directly on the basis of soil properties, shows that the former works well only in a certain developmental stage of the tree layer. The latter method works continuously better and gives more reliable results in forecasting.

At the same time we agree that detailed floristic analysis by site types is of utmost importance from the purely botanic (how different plant species are associated and the theoretical aspect of plant diversity) and ecological aspects (Kull & Zobel 1991; Zobel 1992; Sammul et al. 2003; Partel et al. 2004; Zinko et al. 2006).

The base of the common site type of rendzinas (Acrostaphylos-alvar) is characterized by a modest fine earth stock in soil cover, high calcareousness and skeleton content, excessive natural drainage, low water holding capacity and an unstable water regime (Fig. 5). Their humus cover is classified as dry calci-mull, with a high concentration, but low stock of soil organic carbon in A horizon and biologically active unlayered detritic O horizon. The Acrostaphylos-alvar site type can be clearly distinguished from site types contiguous to it, from Sesleria-alvar by soil water regime and from (Cladonia) by differences in soil varieties. Some interference is obtained with the Calamagrostis-alvar site type. Spruce and pine forest, and juniper woodlands are dominant among forest ecosystems on this soil group.

The most important plant associations on alvar grasslands are Ditricho-Sedo-Thymetum, Filipendulo-Trifolietum montani, Agrosteto(vineale)-Caricetum caryophyUeae and Alchemillo-Festucetum (Krall et al. 1980). These coincide to some extent with the plant associations proposed by Paal (1997): Ditricho-Thymetum, Arrhenatheretum, Trifolio montani-Filipenduletum vulgaris and Helictotricho-Callunetum. The extent of agricultural use of group 1 soils is limited (totalling < 20%).

Hepatica (Fig. 5) is the most common site type for all brown soils (Ko, KI, Kor), but humus cover for more calcareous typical brown soils is fresh mull, and for lessive brown soils, and to a greater extent eluviated soils, fresh moder-mull type. The main plant associations forming grassland ecosystems are Filipendulo-Seslerietum coerulea, Seslerio-Caricetum montanae, Scorzonero-Melampyretum, Cynesureo-Festucetum rubrae with their numerous variants (Krall et al. 1980; Paal 1997). Brown soils are suitable for a wide range of agricultural uses (Table 6).

Brown (O-A-Baf-Egl-2B-2C) and light (O-A-Egl-2B-2C) pseudopodzolic soils are distinguished among pseudopodzolic soils. The difference between them is the absence or presence of a brown-coloured Baf horizon, formed by the accumulation of amorphous iron in the soil profile (Reintam 1973). However, very often these two varieties of pseudopodzolic soil alternate after a small distance, thus, separation of their pedon contours (patches) is complicated. The joint forest site type for fresh pseudopodzolic soils is Oxalis, but for moist varieties, mainly Oxalis-Myrtillus. The site type Aegopodium may also occur.

The dominant plant associations on natural grasslands with pseudopodzolic soils are Agrosteto-Festucetum rubrae, Anthoxantho-Agrostetum, Deschampsietum flexuosae in fresh moisture conditions and Potentillo-Deschampsietum and Caricetum paniceo-nigrae in moist conditions. As pseudopodzolic soils are the best arable soils (Tables 5 and 6) in southeastern Estonia, the extent of their agricultural use is rather high (~64%). For better agricultural management gleyed pseudopodzolic soils should be artificially drained, which is usually not needed in the case of forests and grasslands.

Soil associations of gley-podzols and peaty podzols (soil group 4) may include degraded soil covers consisting of the ortstein cemented spodic horizon. The ortsteinic gley-podzols form altogether < 5% of the soil group 4 area. According to forest site type, these soils are characterized mainly as Vaccinium ulginosum (Fig. 5). The low productivity of these soils is due to acid and wet conditions, in which the activity of soil biota is inhibited and the nutrients are not released by the mineralization of organic matter (Bolin et al. 2000). This results in stagnation of organic matter flow throughout the ecosystem and further paludification of soil cover. These developments are accompanied by soil acidification due to low base content in pine litter (Pritchett & Fisher 1987). The humus cover of wet mor or peaty mor type is formed (Table 3) by the accumulation of extra organic matter on top of these soils.

The characteristic plant cover in grasslands on gleypodzols is Polytricho-Nardetum, a type with very low productivity in spite of its high content of organic matter. On podzolic gley-soils (formed from gley-podzols and peaty podzols), the more productive Caricetum canescentis-elongatae, Potentillo-Deschampsietum, Caricetum flavae, Nardo-Danthonietum types of grassland may occur along with the above-named type.

The causal adequacy between soil and plant covers is clearly visible in circumstances where the interferences in soil cover properties are absent. The estimation of soil type on the basis of ground vegetation may be disturbed by several external factors (age of stand, stock density, cuttings), which causes considerable decrease or loss in the indicator value of ground vegetation.

The geographical aspect is also important in identifying the brown lessive and pseudopodzolic soils. As both soils may be formed either on yellow-grey or red-brown tills, these materials may be either calcareous or non-calcareous. This situation is reflected in joint (common) plant associations of these soils: Cynosureo-Festucetum rubrae, Agrostio capillaris-Trifolietum repentis and Trifolio repentis-Festucetum rubrae on grasslands.

In the analysis of soil-plant interrelationships of brown soils the geomorphological differences in soil-forming conditions should be explained. Brown soils may be distributed alongside the above-treated almost flat (undulating) moraine landscapes as well as in hilly (esker, drumlin, moraine hill) areas, which are distinguished by Masing (1969) as hillock forests. From the geobotanical aspect, these sites are characterized as Fragaria and Corylus forest site types (Paal et al. 2010).

In forests, the floral composition of ground vegetation and its productivity depend on properties of humus cover (forest floor in association with humus horizon) and on processes occurring in these layers. The feedback influence of subsoil is expressed not only via falling litter and stem flow characteristics, but also via tree layer composition and the formation of a particular type of humus cover. The influence of tree species (pine, spruce and some deciduous species) on soil properties is expressed in changes in topsoil pH, organic carbon content, C : N ratio, etc. Trials with Scots pine show the acidifying effect on topsoil if the contribution of nitrate to the N nutrition is [less than or equal to] 70% (Arnold 1992). Tree layers have no substantial effect on the properties of deeper soil horizons (Menyailo et al. 2002), but it should be emphasized that subsoil strongly influences topsoil processes (Kolli 1987).

Paal et al. (2004) indicated the possibility of vegetation convergence or the formation of similar communities on different soils and sites. It may be possible, but it should be mentioned that in such cases, the driving force is the influence of feedback, first, of the tree layer, but also from all biotic factors and characteristics of the formed humus cover.

The soil-plant interrelationships in forests are characterized by highly variable feedback influences compared with both arable and grassland ecosystems (Karpachevskij 1977; Morecroft et al. 2004). For example, there are great differences in humus cover fabric and properties found under tree crowns and in open-to-light patches between trees. Giesler et al. (1998) noted that plant cover productivity and composition in boreal forests is connected to the variability in soil pH and the supply of base cations.

The influence of soils on plant cover is more clearly visible in forests than in natural grasslands, mainly due to the turnover of long-lasting uniform substances in forests. The correlation between soils and plants in seminatural grasslands is frequently lower than in forests, because of disruptive human activity (e.g. mowing, pasturing).

Influence of land use change on soil properties and functioning

Humus cover is a space or contact area of soil-plant interaction, directly bound and significantly influenced by both plants and soils. Both influences are integrated in the properties of humus cover and its type (Table 4). Humus cover results from various accumulation-humification-mineralization processes of plant residues and depends on existing ecological conditions and soil mineral-chemical potential (Bolin et al. 2000; Targulian & Krasilnikov 2007). Identification of the humus cover type enables researchers to characterize soil humus status, evaluate its adequacy for the existing pedo-climatic conditions and arrange sustainable soil management.

Land use change leads to a considerable change in soil cover properties and functions. When natural forest areas are converted into arable land, the forest floor on the soil surface is mixed with mineral horizons forming a substantially changed humus horizon. New types of humus covers are formed in place of natural humus covers (Table 3, Fig. 2C, D). The depths of humus cover in arable lands are significantly higher than in forest lands in all soil groups (Table 9). The mean depth of humus cover in arable areas is equal at least to plough depth. The stocks of organic carbon in the whole forest and the arable soil cover of rendzinas and brown soils are approximately similar (Table 4). Significant differences in organic carbon stocks between forest and arable soils are revealed in gley-podzols, where the soil organic carbon stocks are greater in forest soil than in arable soils. Great changes in the parameters of soil acidity and percentage base saturation in arable pseudopodzolic soils and podzolic gley-soils are due to liming, which is necessary for transforming the growth conditions favourable for cultivated plants.

The loss of topsoil organic carbon (mostly through reduced input of organic matter) by the conversion from natural into cultivated soil is well known (Post & Mann 1990; Davidson & Ackerman 1993; Murty et al. 2002). Rapid decline in soil organic matter is partly due to a lower fraction of non-soluble material in the more readily decomposed crop residues. Tillage, in addition to the mixing and stirring of soil, breaks up aggregates and exposes organo-mineral surfaces otherwise inaccessible to decomposers. The accumulation of organic carbon is reduced by [greater than or equal to] 50% when pasture is converted to arable land, but can be increased by only 18-20% when the conversion is from arable land to pasture or forest (Guo & Gifford 2002).

Although the humus cover is profoundly transformed with land use change, the accordance of forest soil humus cover types with arable soils is generally observable in all soil groups (Table 3, Fig. 2C, D). This pedo-ecologically caused accordance is most evident in the conditions of low input agriculture. In the conditions of high input agriculture (fertilizing, liming, drainage) the relative roles of inherited soil properties are decreased and not clearly evident. The annual input of new organic matter and retained organic residues in arable soil varies largely due to crop rotation, soil management and climatic characteristics (Rychcik et al. 2006). The subsoil properties alter insignificantly in connection with land use change or rest in an almost unchanged status (Kolli et al. 2010).

The transformation of arable soil into forest soil starts from humus cover; it takes over one decade to complete the conversion. When agricultural land is no longer used and natural plant cover is allowed to grow, then, according to Post & Kwon (2000), the accumulation of organic carbon in soil increases. The management methods used on cultivated soils have exhibited after-effects on grassland for several decades. The application of mineral fertilizers on wooded meadow 20 years ago is still causing decreased species richness (Sammul et al. 2003).

Problems with weeds arise with conversion of natural areas (forests, natural grasslands) into cultivated ones (arable lands, cultivated grasslands). The presence of some weeds depends on the cultivated plant species, but others result from pedo-ecologic and agro-technologic situations; their survival strategies and injuring capabilities are diverse (Laasimer 1965; Hyvonen & Salonen 2002; Bender 2006; Cimalova & Lososova 2009). Weeds can also have a positive influence, increasing biological diversity, and filling ecosystem niches in both spatial and temporal aspects. However, the main negative influence is lower cultivated crop productivity, which can be observed from the moment the critical abundance of weeds is exceeded. At this point, cultivated crop productivity is suppressed and, more broadly, total agro-ecosystem productivity is decreased, because weeds are less capable of producing phytomass than crops.

An ecosystem approach to sustainable land use

Ecologically sound land management is based on an ecosystem approach which, along with general pedo-climatic (soils, microclimate) and external environmental conditions, takes into account the pedo-diversity and environmental protection ability of soils as internal (intrinsic) properties of the ecosystem. For attaining ecologically sound land use or to increase the efficiency of the utilization of soil resources, the disharmonies in matching plant cover with soil cover or biodiversity with pedo(geo)diversity should be overcome (Kask 1975; Chertov 1981; Fisher et al. 2002).

Although the ecosystem pattern in natural and cultivated areas is mainly induced from the pedo-ecological conditions of the region, it may be controlled by diverse activities of landowners. As a result of continuous human interactions with natural ecosystems, coupled human and natural systems are formed (Liu et al. 2007). These couplings have evolved from direct to more indirect interactions, from adjacent to more distant linkages, and from simple to complex patterns and processes.

The regularities of the causally bound development sequence, parent material (geodiversity) [right arrow] soil cover (or pedodiversity) [right arrow] ecosystems (with floristic composition adequate to soil and productivity), are more clearly revealed when interference and edge effects of contiguous areas are absent. In cultivated areas, aside from the natural background, different kinds of outside impacts with various influence intensity play the leading role (Liniger & Critchley 2007). To increase the efficiency of soil resource development, the principles of plant cover suitability for soils must be taken into account.

The total productivity of ecosystems formed on well-drained soil depends mainly on clay and organic matter content and stock in the soil profile (Kask 1975; Kolli 1987; Kasparinskis & Nikodemus 2012). These parameters, indicating capabilities of soils, are also used as a basis for indirect evaluation of soil quality (ELB 1992; Kolli 1994; Lohmus 2006). The amount of annual flux in organic carbon depends largely on the dominant species of plant cover. As a rule, a few plant species or edificators are responsible for the prevailing part of phytomass areal density as well as annual substance fluxes. Accordingly, the maximum functioning of an ecosystem is observed in the presence of plant cover diversity optimal to soil (specific to the soil variety). If the floristic composition is unsuitable for soil plant cover, the activity of the ecosystem may be suppressed. An excessive biodiversity is unfavourable as well. Productivity may also be lower in the conditions of lower vs. optimal plant species richness, as the capability of some ecological niches is not used.

The most species-rich but relatively low-productive plant associations are formed on extensively used seminatural grasslands on calcareous soils. Alvar site type forests and dry alvar natural grasslands on rendzinas have unique plant associations, and are the target of protection efforts. Partel et al. (2004) pointed out that the proportion of protected plant associations on these soils is unusually high in Northern Europe. For conservation of such unique associations, the soil cover should be maintained in its natural status or under extensive but low-productivity management conditions, such as mowing or pasture.

Society at large and landowners in particular should find a compromise in the ratio of protected areas for scientific purposes (conservation of high plant cover biodiversity) and conventionally (sustainable) managed territory, as the highest plant species richness is observed only in low input management conditions. For attaining stable and high ecosystem productivity, it is important to maintain soil biodiversity at an optimal level, or it should be soil type-specific.

Humus cover, which is formed from returned litter fall into soil fresh organic matter, is a good integrated indicator (aside from soil productivity) in the estimation of ecosystem functioning intensity, as the humus cover type characterizes the decomposition-humification process in the forestlgrassland floor. The PES soils analysed reflect different humus cover formation conditions where the dry carbonate-rich medium is changing into wet acid conditions, resulting in differences in the fabric, structure, humus stocks and other properties of humus cover.

Soil functioning capability (quality) may be determined by different methods: (1) by the total phytomass and APP (Rodin et al. 1968; Kolli 1987; Bazilevich & Titljanova 2008), (2) by yield of field crops and grasslands (Bender 2006; Older 2007), (3) by indirect (model-based) estimation according to different soil parameters (ELB 1992) and (4) by interpolation of generalized data (Panagos & van Liedekerke 2008). The most appreciated method, however, involves the evaluation of both ecosystem productivity and its functioning activity.

The activities for arrangement of ecologically sound soil management of an area are site-specific, that is, they depend on soil properties. Soil properties can change in very small areas, so there may be plant associations containing species not characteristic of soil properties. A mosaic soil cover leads to the formation of plant cover, which in some places is rich in species and variable in plant associations (Karpachevskij 1977). Without knowing the causality of interrelationships of soil and plant cover, the sustainable use of rural areas is problematic. For amelioration of soil management quality, the adequacy of land use (forests, arable or grasslands) and the suitability of their plant cover to soil cover should be critically analysed and corrected, where necessary. Without such determination, various disharmonies may occur between our endeavours and local site conditions. Using the principles of an ecosystem approach, it is possible by the choice of suitable land use, and well matched soils and plant cover to assure the functioning stability in forest and grassland ecosystems and step-by-step form conditions for increasing productivity of agro-ecosystems.

It is important to use new technologies and methods to improve conventional management of soil cover, thereby increasing soil productivity and quality. For the development of efficient conservation agriculture on arable soils, suitable crops should be chosen for soils; the opposite approach always requires corrections in soil properties. Reforestation of low-quality grasslands and fields is acceptable.

For safeguarding the healthy environmental status of areas, the functioning of soil cover should be arranged in accordance with local soil capability. For environmentally sound and continuous use of arable soils the annual losses of soil organic carbon and pool of nutritional elements should be compensated. Step-by-step improvement of soil fertility and soil productivity increase sustainable functioning and the environmental protection ability of soils.


Soil cover of a natural area has a decisive role in the formation of plant cover composition, productivity and diversity. Therefore the awareness of the composition and properties of soil cover and its relationship with plant cover in different land use conditions is the basis of ecologically proper and sustainable management of land (soil) resources.

The existing pedodiversity of an ecosystem should be taken as an abiotic base in the formation of optimal plant cover biodiversity for a specific location. It is important to maintain an 'optimal to soil-type' biodiversity; in most cases, the highest species richness is not a guarantee of the highest possible functioning intensity and autotrophic productivity. The ecologically sound matching of soil and plant cover is of pivotal importance from the aspect of ecosystem functioning sustainability and for good environmental status of an area.

Comparative analysis of soil-plant interrelationships along the pedo-ecological sequence rendzinas [right arrow] brown soils [right arrow] pseudopodzolic soils [right arrow] gley-podzols shows that (1) the biodiversity of an ecosystem depends on soil properties and therefore biodiversity should be treated as a soil type-specific feature and (2) the character or type of humus cover is a good ecological indicator, because it adequately characterizes the outlines of the biological turnover between soil and plant, and clearly distinguishes all studied ecosystems from one another.

With land use change (from natural to arable and vice versa), more drastic changes occur in the fabric and properties of humus cover (as topsoil), but the subsoil rests in an almost unchanged state. In circumstances of low input as opposed to intensive agriculture, the inherited soil properties persist to a greater extent in the functioning of agro-ecosystems formed by cultivation.

Indirect characterization of forest soil (edaphic) conditions according to the floristic composition of ground vegetation should be turned into direct (i.e. according to soil properties) identification of an area's growth conditions. Prerequisites for this are large-scale soil maps, in which soil distribution and properties are identified on the level of soil variety for entire Estonia.

Acknowledgements. The study was supported by the target-financed project SF0172613s03 and by the Estonian Science Foundation (grants 3539 and 4991). We are grateful to Prof. M. A. Fullen from The University of Wolverhampton for improving the English of our manuscript, as well for valuable remarks related to terminology used in the work.

doi: 10.3176/earth.2013.08


Arnold, G. 1992. Soil acidification as caused by the nitrogen uptake pattern of Scots pine (Pinus sylvestris). Plant and Soil, 142, 41-51.

Arold, I. 2005. Eesti maastikud [Estonian Landscapes]. Tartu Ulikooli Kirjastus, Tartu, 453 pp. [in Estonian, with English summary].

Asi, E., Kolli, R. & Laas, E. 2004. Pollumaade metsastamine [Afforestation of Arable Lands]. Methodical guide for afforestation of arable lands. Metsakaitse-ja Metsauuenduskeskus, Tartu, 83 pp. [in Estonian].

Astover, A., Roostalu, H., Lauringson, E., Lemetti, I., Selge, A., Talgre, L., Vasiliev, N., Motte, M., Torra, T. & Penu, P. 2006. Changes in agricultural land use and in plant nutrient balances of arable soils in Estonia. Archives of Agronomy and Soil Science, 52, 223-231.

Bazilevich, N. I. & Titljanova, A. A. 2008. Bioticheskij krugovorot na pjati kontinentakh: azot i zol'nye elementy v pripodnykh nazemnykh ekosistemakh [Biotic Turnover on Five Continents: Element Exchange Process in Terrestrial Natural Ecosystems]. Publishing House SB RAS, Novosibirsk, 380 pp. [in Russian].

Bender, A. 2006. Erituubiliste rohumaade rajamine ja kasutamine [Establishment and Management of Different Grassland Types], part I. Tartu Ulikooli Kirjastus, Tartu, 338 pp. [in Estonian].

Bolin, B., Sukumar, R., Ciais, P., Cramer, W., Jarvis, P., Kheshgi, H., Nobre, C., Semenov, S. & Steffen, W. 2000. Global perspective. In Land Use, Land-Use Change, and Forestry (Watson, R., Noble, I. R., Bolin, B., Ravindranath, N. H., Verado, D. J. & Dokken, D. J., eds), pp. 23-51. Cambridge University Press.

Chertov, O. G. 1981. Ekologiya lesnykh zemel': pochvenno-ekologicheskoe issledovanie lesnykh mestoobitanij [Ecology of Forest Lands: Pedo-Ecological Research of Forest Sites]. Nauka, Leningrad, 192 pp. [in Russian].

Cimalova, S. & Lososova, Z. 2009. Arable weed vegetation of the northeastern part of the Czech Republic: effects of environmental factors on species composition. Plant Ecology, 203, 45-57.

Davidson, E. A. & Ackerman, I. L. 1993. Changes in soil carbon inventories following cultivation of previously untilled soils. Biochemistry, 20, 161-193.

Deckers, J. A., Nachtergaele, F. O. & Spaargaren, O. (eds). 1998. World Reference Base for Soil Resources: Introduction. ISSS-ISRIC-FAO, Acco, Leuven, 165 pp.

[EAP] Estonian Agro-project. 1989. ENSV mullastik arvudes [Soils of the Estonian SSR in Numbers], VIII. Tallinn, 88 pp. [in Estonian].

[EC] European Commission. 2005. Soil Atlas of Europe. European Soil Bureau Network of European Commission. OOP EC, Luxembourg, 128 pp.

[ELB] Estonian Land Board. 1992. Maade tootlikkuse hindamise tabelid [The Tables for Evaluation of Lands' Productivity]. Tallinn, 22 pp. [in Estonian].

[ELB] Estonian Land Board. 2012. Explanatory letter for the large scale digital soil map of Estonia. docs/muld/mullakaardi_seletuskiri.pdf [in Estonian, accessed 11.04.2012].

Fisher, G., van Velthuizen, H., Shah, M. & Nachtergaele, F. 2002. Global Agro-Ecological Assessment for Agriculture in the 21st Century: Methodology and Results. Research Report 2, IIASA & FAO. Remaprint, Vienna, 119 pp.

Giesler, R., Hoegberg, M. & Hoegberg, P. 1998. Soil chemistry and plants in Fennoscandian boreal forest as exemplified by a local gradient. Ecology, 79, 119-137.

Guo, Y., Gong, P. & Amundson, R. 2003. Pedodiversity in the United States of America. Geoderma, 117, 99-115.

Guo, L. B. & Gifford, R. M. 2002. Soil carbon stocks and land use change: a meta analysis. Global Change Biology, 8, 345-360.

Hyvonen, T. & Salonen, J. 2002. Weed species diversity and community composition in cropping practices at two intensity levels--a six-year experiment. Plant Ecology, 159, 73-81.

Ibanez, J. J., De-Alba, S., Lobo, A., Zucarello, V. & Yaalon, D. H. 1998. Pedodiversity and global soil patterns at coarse scales (with Discussion). Geoderma, 83, 171-192.

[IUSS] IUSS Working Group WRB. 2006. World Reference Base for Soil Resources. 2nd ed. World Soil Resources Reports, 103. FAO, Rome, 128 pp.

Jaagus, J. 1999. New data about the climate of Estonia. In Studies on Climate of Estonia (Jaagus, J., ed.), Publicationes Instituti Geographici Universitatis Tartuensis, 85, 28-38 [in Estonian].

Kachinsky, N. A. 1965. Fizika pochv [Soil Physics]. Vol. 1. University Press, Moscow, 323 pp. [in Russian].

Karpachevskij, L. O. 1977. Pestrota pochvennogo pokrova v lesnom biogeotsenoze [Variation of Soil Cover in Forest Biogeocoenosis]. Publisher of Moscow University, 312 pp. [in Russian].

Kask, R. 1975. Eesti NSV maafond ja selle pollumajanduslik kvaliteet [Land Resources of Estonian SSR and Its Agricultural Quality]. Valgus, Tallinn, 358 pp. [in Estonian].

Kasparinskis, R. & Nikodemus, O. 2012. Influence of environmental factors on the spatial distribution and diversity of forest soil in Latvia. Estonian Journal of Earth Sciences, 61, 48-64.

Kokk, R. 1995. Muldade jaotumus ja omadused [Distribution and properties of soils]. In Estonia. Nature (Raukas, A., ed.), pp. 430-439. Valgus, Tallinn [in Estonian, with English summary].

Kolli, R. 1987. Pedoekologicheskij analiz fitoproduktivnosti, biogeokhimicheskikh potokov veshchestv i gumusogo sostoyaniya v estestvennykh i kul turnykh ekosistemakh [Pedoecological Analysis of Phytoproductivity, Biogeochemical Fluxes of Substances and Humus Status in Natural and Cultivated Ecosystems]. Doctoral dissertation, Estonian Agricultural Academy, Tartu, 553 pp. [in Russian].

Kolli, R. 1994. Muldade kasutussobivus ja agroruhmad [Suitability of Soils for Crops and Soil Agro-Groups]. Estonian Agricultural University, Tartu, 85 pp. [in Estonian].

Kolli, R., Ellermae, O. & Teras, T. 2008. Eesti muldade digitaalne kogu [Digital Collection of Estonian Soils]. Maaulikool, [accessed 11.04.2012].

Kolli, R., Ellermae, O., Koster, T., Lemetti, I., Asi, E. & Kauer, K. 2009. Stocks of organic carbon in Estonian soils. Estonian Journal of Earth Sciences, 58, 95-108.

Kolli, R., Koster, T., Kauer, K. & Lemetti, I. 2010. Pedo-ecological regularities of organic carbon retention in Estonian mineral soils. International Journal of Geosciences, 1, 139-148.

Kont, A., Rooma, I. & Aruvali, J. 2004. Erineva saaste-koormusega mohnastike muldade omaduste soltuvus lahtekivimi koostisest [Dependence of soil properties on the character of parent material in the kame fields of different loads of dry deposition]. In Soil in Ecosystem, Monitoring and Protection (Reintam, L., ed.), pp. 75-103. Teaduste Akadeemia Kirjastus, Tallinn [in Estonian, with English summary].

Krall, H., Pork, K., Aug, H., Puss, O., Rooma, I. & Teras, T. 1980. Eesti NSV looduslike rohumaade tuubid ja tahtsamad taimekooslused [The Types and Most Important Plant Associations of Natural Grasslands in the Estonian SSR]. ENSV PMM IJV, Tallinn, 88 pp. [in Estonian].

Kull, K. & Zobel, M. 1991. High species richness in an Estonian wooded meadow. Journal of Vegetation Science, 2, 715-718.

Laasimer, L. 1965. Eesti NSV taimkate [Vegetation of the Estonian SSR]. Valgus, Tallinn, 397 pp. [in Estonian, with English and Russian summaries].

Laasimer, L. & Masing, V. 1995. Taimestik ja taimkate [Flora and plant cover]. In Estonia. Nature (Raukas, A., ed.), pp. 364-396. Valgus, Tallinn [in Estonian, with English summary].

Lillema, A. 1962. Die humus-karbonatboden in der Estnischen SSR. In Transactions on Soil Science and Agrochemistry (Tarandi, K., ed.), Transactions EAA, 24, 173-185 [in Russian, with German summary].

Lindborg, R., Zobel, M., Bommarco, R., Heikkinen, R. K., Kuhn, I., Pyhala, J. & Partel, M. 2012. Effect of habitat area and isolation on plant trait distribution in European forests and grasslands. Ecography, 35, 356-363.

Liniger, H. & Critchley, W. (eds). 2007. WOCAT 2007: Where the Land is Greener--Case Studies and Analysis of Soil and Water Conservation Initiatives Worldwide. CTA, FAO, UNEP & CDE, Bern, 364 pp.

Liu, J., Dietz, T., Carpenter, S. R., Folke, C., Alberti, M., Redman, C. L., Schneider, S. H., Ostrom, E., Pell, A. N., Lubchenco, J., Taylor, W. W., Ouyang, Z., Deadman, P., Kratz, T. & Provencher, W. 2007. Coupled human and natural systems. Ambio, 36, 639-649.

Lohmus, E. 1973. Tipologicheskij analiz lesov Estonskoj SSR [Typological Analysis of Forests in the Estonian SSR]. Abstract of dissertation, Tartu, 35 pp. [in Russian].

Lohmus, E. 1974. Metsad rabadest nommede ja loopealseteni [Forests from high bogs to heaths and alvars]. In Estonian Forests (Valk, U. & Eilart, J., eds), pp. 80-98. Valgus, Tallinn [in Estonian].

Lohmus, E. 2006. Eesti metsakasvukohatuubid [Estonian Forest Site Types]. Eesti Loodusfoto, Tartu, 80 pp. [in Estonian].

Lososova, Z., Chytry, M., Cimalova, S., Kropac, Z., Otypkova, Z., Pysek, P. & Tichy, L. 2004. Weed vegetation of arable land in Central Europe: gradients of diversity and species composition. Journal of Vegetation Science, 15, 415-422.

Masing, V. 1969. Metsatupoloogia probleeme [Problems of forest typology]. In Loodusuurijate Seltsi aastaraamat 59 (Trass, H., ed.), pp. 150-169. Valgus, Tallinn [in Estonian, with Russian and German summaries].

Menyailo, O. V., Hungate, B. A. & Zech, W. 2002. Tree species mediated soil chemical changes in a Siberian artificial afforestation experiment. Plant and Soil, 242, 171-182.

Morecroft, M. D., Masters, G. J., Brown, V. K., Clarke, I. P., Taylor, M. E. & Whitehouse, A. T. 2004. Changing precipitation patterns alter plant community dynamics and succession in an ex-arable grassland. Functional Ecology, 18, 648-655.

Murty, D., Kirchbaum, M. U. F., McMurtrie, R. E. & McGilvray, H. 2002. Does conversion of forest to agricultural land change soil carbon and nitrogen? A review of the literature. Global Change Biology, 8, 105-123.

Older, H. 2007. Rohumaaviljeluse, karjakasvatuse ja haljastuse integratsioon [Integration of Grassland Husbandry, Cattle Breeding and Creating of Green Areas]. Estonian Grassland Society, Saku, 258 pp. [in Estonian].

Paal, J. 1997. Eesti taimkatte kasvukohatuupide klassifikatsioon [Classification of Estonian Vegetation Site Types]. Ministry of the Environment of Estonia & UNEP, Tallinn, 297 pp. [in Estonian].

Paal, J., Rooma, I. & Turb, M. 2004. Surjametsadest Otepaa korgustikul [About meso-eutrophic boreo-nemoral hillock forests on Otepaa Upland]. Metsanduslikud Uurimused, 40, 124-149 [in Estonian].

Paal, J., Rajandu, E. & Koster, T. 2010. Vegetation-environment relationship in Estonian Hepatica site type forests in the light of A. K. Cajander's forest site type approach. Baltic Forestry, 16, 194-208.

Paal, J., Turb, M., Koster, T., Rajandu, E. & Liira, J. 2011. Forest land-use history affects the species composition and soil properties of old-aged hillock forests in Estonia. Journal of Forest Research, 16, 244-252.

Panagos, P. & van Liedekerke, M. 2008. Multi-Scale European Soil Information System (MEUSIS): novel ways to derive soil indicators through upscaling. In Threats to Soil Quality in Europe (Toth, G., Montanarella, L. & Rusco, E., eds), pp. 139-148. JRC, European Communities.

Partel, M., Helm, A., Ingerpuu, N., Reier, U. & Tuvi, E.-L. 2004. Conservation of Northern European plant diversity: the correspondence with soil pH. Biological Conservation, 120, 525-531.

Post, W. M. & Kwon, K. C. 2000. Soil carbon sequestration and land-use change: processes and potential. Global Change Biology, 6, 317-327.

Post, W. M. & Mann, L. K. 1990. Changes in soil organic carbon and nitrogen as a result of cultivation. In Soils and the Greenhouse Effect (Bouwman, A. F., ed.), pp. 401-406. John Wiley, New York.

Pritchett, W. L. & Fisher, R. F. 1987. Properties and Management of Forest Soils. John Wiley & Sons, New York, 494 pp.

Raukas, A. 1995. Pinnakate [The Quaternary cover]. In Estonia. Nature (Raukas, A., ed.), pp. 93-118. Valgus, Tallinn [in Estonian, with English summary].

Reintam, L. Yu. 1973. Avtomorfnoe pochvoobrazovanie na morenakh i dvuchlennykh porodakh Estonii [Automorphic Soil Formation on Estonian Tills and on Two-Layered Parent Materials]. Doctoral Thesis, Novosibirsk, 54 pp. [in Russian].

Reintam, L. 1997a. Pedogenetic changes in the quantity and distribution of textural and chemical soil constituents during thirty years. Proceedings of the Estonian Academy of Sciences, Biology, Ecology, 46, 174-190.

Reintam, L. 1997b. Soil formation. In Geology and Mineral Resources of Estonia (Raukas, A. & Teedumae, A., eds), pp. 298-306. Estonian Academy Publishers, Tallinn.

Reintam, L. 1998. Soil genesis, diagnostics and classification. In Problems of Estonian Soil Classification (Kolli, R., ed.), Transactions EAU, 198, 24-36 [in Estonian, with English summary].

Reintam, L. 2007. Soil formation on reddish-brown calcareous till under herbaceous vegetation during forty years. Estonian Journal of Earth Sciences, 56, 65-84.

Rodin, L. E., Remezov, N. P. & Bazilevich, N. I. 1968. Metodicheskie ukazaniya k izucheniyu dinamiki i biologicheskogo krugovorota v fitotsenozakh [Methodical Instructions for the Study of Dynamics and Biological Turnover in Phytocoenosis]. Nauka, Moscow, 143 pp. [in Russian].

Rychcik, B., Adamiak, J. & Wojciak, H. 2006. Dynamics of the soil organic matter in crop rotation and long-term monoculture. Plant, Soil and Environment, 52, 15-20.

Sammul, M., Kull, K. & Tamm, A. 2003. Clonal growth in a species-rich grassland: results of a 20-year fertilization experiment. Folia Geobotanica, 38, 1-20.

Sepp, R. 1960. Metsa alustaimestiku osatahtsus loometsade tupiseerimisel ja loomuldade arenguprotsessis [The role of the forest ground vegetation at a classification of alvar forests into types and at the development of alvar soils]. Proceedings of the Academy of Sciences of the ESSR, Biology, 9, 144-166 [in Estonian, with Russian and English summaries].

Sepp, R. 1962. The study of the relations between the forest vegetation and the soil in alvar forests. In Transactions on Soil Science and Agrochemistry (Tarandi, K., ed.), Transactions EAA, 24, 186-205 [in Russian, with English summary].

[SPAC] Soil and Plant Analysis Council. 1992. Handbook on Reference Methods for Soil Analysis, 202 pp.

[SSDS] Soil Survey Division Staff. 1993. Soil Survey Manual. USDA, Washington DC, 437 pp.

Tamme, R., Hiiesalu, I., Laanisto, L., Szava-Kovats, R. & Partel, M. 2010. Environmental heterogeneity, species diversity and co-existence at different spatial scales. Journal of Vegetation Science, 21, 796-801.

Targulian, V. O. & Krasilnikov, P. V. 2007. Soil system and pedogenic processes: self-organization, time scales, and environmental significance. Catena, 71, 373-381.

Toth, G., Montanarella, L., Stolbovoy, V., Mate, F., Bodis, K., Jones, A., Panagos, P. & van Liedekerke, M. 2008. Soils of the European Union. OOP EC, Luxembourg, 85 pp.

Valk, U. & Eilart, J. 1974. Eesti metsad [Estonian Forests]. Valgus, Tallinn, 307 pp. [in Estonian, with Russian, English and German summaries].

Vorobyova, L. A. 1998. Khimicheskij analiz pochv [Chemical Analysis of Soils]. Moscow University Press, Moscow, 272 pp. [in Russian].

Zinko, U., Dynesius, M., Nilsson, C. & Seibert, J. 2006. The role of soil pH in linking groundwater flow and plant species density in boreal forest landscapes. Ecography, 29, 515-524.

Zobel, M. 1992. Plant-species coexistence: the role of historical, evolutionary and ecological factors. Oikos, 65, 314-320.

Tiina Koster (a,b) and Raimo Kolli (b)

(a) Agricultural Research Centre, Saku, Teaduse 4/6, 75501 Harju County, Estonia

(b) Estonian University of Life Sciences, Kreutzwaldi 1A, 51014 Tartu, Estonia;,

Received 14 May 2012, accepted 6 September 2012

Table 1. Nomination of sampling soil groups by the Estonian
Soil Classification (ESC) and distribution of analysed soil
groups among Estonian normally developed mineral soils

Nomination of soil               Percentage of soil
groups by ESC                     group from normal
                                 mineral soils area
                                       (1) on

No.   Name             Code      total   forest
                                 land    land

1     Rendzinas        Kh,        2.9      1.1
      (limestone,      Kr
      pebble,          (Kk)

2     Brown soils      Ko,        9.1      4.2
      (typical,        KI
      lessive,         (Kor)

3     Pseudopodzolic   LP,       13.1      5.9
      soils            LPg

4     Gley-podzols     LG,        5.2     13.4
      (gley-, peaty)   LG1

1-4   Totally PES      8(10)     30.3     24.6
      soils            soil

Nomination of soil       Percentage of soil
groups by ESC             group from normal
                         mineral soils area
                               (1) on

No.   Name             arable      grassland

1     Rendzinas           3.7         3.1

2     Brown soils        18.7        12.6

3     Pseudopodzolic     24.9         5.7

4     Gley-podzols       0.9 (2)      4.0 (2)
      (gley-, peaty)

1-4   Totally PES        48.2        25.4

(1) The distribution % of total, forest and arable land is
calculated after Kokk (1995), on grassland--our approximate
estimation; (2) to the area of gley-podzols (LG) and peaty
podzols (LG1) the area of podzolic gley-soils (LkG) was

Table 2. Identification and characterization
of soil groups by the World Reference Base
for Soils (WRB)

Soil group

No.   Reference        Qualifiers (1)
      soil by WRB

1     Leptosols       leptic/lithic,

2     Cambisols,      cambic, mollic,
      Luvisols        luvic/cutanic/

3     Albeluvisols    albic, luvic,
                      glossic, umbric/

4     Podzols         spodic/
                      arenic, dystric

1) Three groups of qualifiers separated
by '/ ' are, respectively: main
characteristics of reference soil/prefix
qualifiers/suffix qualifiers.

Table 3. Moisture conditions, texture and humus cover types
of soil groups

Group    Moisture    Dominating         Humus cover type
No.     conditions   soil group
           (1)       texture (2)
                                    on forest      on arable
                                      soils          soils

1       Dry,         Gravelly      Dry calci-     Skeleti-
        fresh        loam on       mull, fresh    calcaric
                     pebble,       calci-mull     mild
                     loam on

2       Fresh        Loam on       Fresh mull,    Neutral
                     gravelly      fresh          mild,
                     loam          moder-mull     eluvic

3       Fresh,       Loamy sand    Fresh moder,   Acid low
        moist        on loam,      moist moder    humuous,
                     loam                         eluvic

4       Wet,         Sand          Wet mor,       Oligotrophic
        peaty                      peaty mor      raw humuous

(1) Adequate estimations for soil cover: dry--drought-prone;
fresh--normally moist; moist--gleyed, endogleyic, temporally
over-moist; wet--gley-, epigleyic, permanently over-moist;
peaty--peaty-gley-, epigleyic, permanently strongly over-moist.
2) Content of physical clay (particles with [empty set] < 0.01
mm) in fine earth (particles with [empty set] < 1 mm): loam
20-10%, loamy sand 10-20% and sand < 10%.

Table 4. Generalized characteristics of soil covers
by studied soil groups

Characteristic (1)          No. of soil group (2)

                              1            2

Thickness of soil cover    23a (3)   52/74 (4) b/c
or solum, cm

SOC stock in forest soil   80-100       85-105
solum, Mg [ha.sup.-1]

SOC stock in arable soil    70-90       80-100
solum, Mg [ha.sup.-1]

Mean solum SOC stock of      75b          91c
soil group, Mg

CEC of solum, 10 kmol       65-75       140-155

Stock of physical clay      75-90       200-300
in solum, 10 Mg

N stock in solum (For/      4/5-7      3-5/8-10
Arb) (5), Mg [ha.sup.-1]

SOM stock of forest         8-10a        7-9a
floor, Mg [ha.sup.-1]

Ratio Chh/Cff (6)            14c          14c

Characteristic (1)          No. of soil group (2)

                              3           4

Thickness of soil cover      92d         76c
or solum, cm

SOC stock in forest soil    60-75      100-120
solum, Mg [ha.sup.-1]

SOC stock in arable soil    65-75       60-80
solum, Mg [ha.sup.-1]

Mean solum SOC stock of      67a        114d
soil group, Mg

CEC of solum, 10 kmol      165-190     130-160

Stock of physical clay     300-350     60-150
in solum, 10 Mg

N stock in solum (For/     2-3/7-8   0.8-1.2/4-5
Arb) (5), Mg [ha.sup.-1]

SOM stock of forest        10-15b      50-75c
floor, Mg [ha.sup.-1]

Ratio Chh/Cff (6)           5.7b       < 0.5a

(1) SOC--soil organic carbon, CEC--cation exchange capacity,
N--nitrogen, SOM--soil organic matter;

(2) for soil group names see Tables 1 (by ESC) and 2 (by
WRB), whereas the exception is soil group 4, where in
arable areas the data are presented for podzolic gley-soils
(LkG), which are modified by cultivation of gley- and peaty
podzols (LG, LG1); (3) letters next to the data indicate
significant difference at p < 0.05; (4) respectively Ko and
KI; (5) For--forest soils, Arb--arable soils; 6) ratio of
organic carbon in humus horizon (Chh) to organic carbon in
the forest floor (Cff) or ratio of endo- and exogenous
organic carbon.

Table 5. Accordance of soil groups with forest site type, soil
agro-groups and grassland types

Soil      Model forest       Soil agro-groups       Natural
group      site type         (code and short       grassland
No.          (code)         characterization)     type (code)

1       Acrostaphylos-     C1--unsuitable for     Dry alvar
        alvar (ll)         field crops,           (Lok)
                           suitable for
                           grassland husbandry

2       Hepatica (sl)      A22--medium-textured   Dry typical
                           automorphic soils      (Aak)
                           well suitable for
                           field crops

3       Oxalis (jk),       A--medium-textured     Dry heathy
        Oxalis-Myrtillus   automorphic (A21)      (Pak), moist
        (jk-ms)            and well-drained       heathy (Pan)
                           gleyed (A42 (1))
                           soils well suitable
                           for field crops

4       Vaccinium          B33(1)--light-         Poor
        ulginosum (sn)     textured well-         paludified
                           drained gley soils,    (Sov)
                           reasonably suited
                           to field crops,
                           well suited for
                           grassland husbandry

(1) Group codes A42 and B33 are valid if soils are sufficiently

Table 6. Generalized characteristics of plant covers by
studied soil groups

Characteristics                     No. of soil group1)

                                      1            2

Dominant species                  Pc, Pn       Pc, Pn,
of tree layer (2)                              Qu, Be

Number of      Underwood           7-9 (11)     8-10 (17)
species (3)    Herb layer         25-30 (32)   30-35 (52)
               Moss layer         4 (6)         5-8 (10)
               Shrub layer        2 (3)         0-2

Above-ground   Tree layer,        108.5a (4)   159.4b
phytomass      Mg [ha.sup.-1]
in dry
weight         Underwood,         14.8a        42.8b
               [10.sup.2] kg

               Herb layer,        6.1c         6.2c
               [10.sup.2] kg

               Moss layer,        12.5a        11.6a
               [10.sup.2] kg

               Shrub layer,       0.3a         0.3a
               [10.sup.2] kg

Number of      Geobotanical       2/3          3/2
plant          approach For/Grl
associations   (5) (Laasimer

               Grasslands         5            5
               (Krall et al.

               Grasslands         4            6
               (Paal 1997)

Suitability    B-R-P (6)          6-5-4        10-9-9

for crops      A-C-Fg (8)         8-4-4         9-9-9

Characteristics  No. of soil group1)

                   3            4

Dominant speciePc, Pn,      Pn
of tree layer (Be

Number of      6-8 (10)     3-4
species (3)    20-25 (34)   5-10 (13)
               7-10         5-7
               2-3          4-6 (7)

Above-ground   197.3c       105.8a
in dry
weight         13.2a        11.4a

               3.4b         0.5a

               11.4a        45.0b

               1.9b         13.9c

Number of      1/2          1/2

               6            2-3

               4            2

Suitability    9-10-10      7(5) (7)-8

for crops      4-9-9        3(1)-5

(1) For soil group names see Tables 1 (by ESC) and 2
(by WRB), the exception is soil group 4, where arable
areas data are presented for podzolic gley-soils (LkG),
which are modified by cultivation from gley- or peaty
podzols (LG, LG1); (2) tree species: Pc--spruce,
Pn--pine, Qu--oak, Be--birch; (3) species, which have
certain importance from the functional aspect; the
maximum number of species is given in brackets;
(4) letters next to the data indicate significant
difference at the p < 0.05 level; (5) respectively in
forest and in grassland; (6) suitability of arable
soils for crops B-R-P: respectively barley, rye and
potato; (7) in brackets suitability of undrained LkG
soil for crops; (8) A-C-Fg: alfalfa, clover and field

Table 7. Generalized characteristics of plant cover productivity
by soil groups

Characteristic                     Type of      No. of sampling soil
                                ecosystem (2)         group (1)

                                                    1          2

APP (3) of tree layer                FES        53.0b (4)    90.2c
  and underwood, [10.sup.2]
  kg [ha.sup.-1]
APP of ground vegetation,            FES          9.2b       11.0b
  [10.sup.2] kg [ha.sup.-1]
Generalized limits of APP,           FES          5-9a      12-14b
  Mg [ha.sup.-1]
Standard yield of cereal             AES          1.64       2.65
  grains (by E. Kitse,
  unpublished data),
  Mg [ha.sup.-1]
Above-ground phytomass of            AES           6-8        8-9
  barley, Mg [ha.sup.-1]
Natural grasslands hay               GES           4-5        13
  yield, 100 kg [ha.sup.-1]
Annual falling litter,               FES           4-7       7-8.5
  Mg [ha.sup.-1] [yr.sup.-1]
Annual falling litter of             AES          2-3.5      4-4.5
  barley, Mg [ha.sup.-1]
Mean SOC annual balance,             FES         2.2-2.3    3.6-3.7
  Mg [ha.sup.-1]

Characteristic                        No. of sampling soil
                                            group (1)

                                      3                4

APP (3) of tree layer               88.9c            35.1a
  and underwood, [10.sup.2]
  kg [ha.sup.-1]
APP of ground vegetation,            6.7a            13.2c
  [10.sup.2] kg [ha.sup.-1]
Generalized limits of APP,          13-15b            5-8a
  Mg [ha.sup.-1]
Standard yield of cereal        2.40(2.31) (5)   1.91(1.37) (5)
  grains (by E. Kitse,
  unpublished data),
  Mg [ha.sup.-1]
Above-ground phytomass of          7.5-8.5            ND6)
  barley, Mg [ha.sup.-1]
Natural grasslands hay              13-14              5
  yield, 100 kg [ha.sup.-1]
Annual falling litter,               6-8              3-5
  Mg [ha.sup.-1] [yr.sup.-1]
Annual falling litter of           3.5-4.2             ND
  barley, Mg [ha.sup.-1]
Mean SOC annual balance,           3.4-3.5          1.7-1.8
  Mg [ha.sup.-1]

(1) For soil group names see Tables 1 (by ESC) and 2 (by WRB);
the exception is soil group 4, where on the arable area data are
presented for podzolic gley-soils (LkG), which are modified by
cultivation of gley- and peaty podzols (LG, LG1);
(2) FES--forest, AES--agro- and GES--grassland ecosystems;
(3) APP--annual phytoproductivity, in dry matter; (4) letters
next to the data indicate significant difference atp < 0.05;
(5) in brackets the yield on undrained soil;
(6) ND--not determined.

Table 8. Characteristics of forest (FES), agro-(AES) and natural
grassland (GES) ecosystem productivity by means of soil quality
classes and soil group environmental protection ability

Soil group             Soil quality    Soil quality classes in
                          points             the case of
                       (act/drn) (1)

No.   Name             AES             FES      AES       GES

1     Rendzina         29-33a2)        IV-V   VI-VIII     IX
2     Brown soils      57-58d          I-II      V       VIII
3     Pseudopodzolic   50-51/53c/c      I        V      VIII-IX
4     Gley-podzols     18-20/29a/b      V      IX-X        X

Soil group                 Environment
                       protection ability

No.   Name             Mean point   Class

1     Rendzina            3.6         V
2     Brown soils         10.6      I-II
3     Pseudopodzolic      12.1      I-II
4     Gley-podzols        4.4        IV

(1) Act--quality points according to soil actual status and
drn--the same after the soil drainage; (2) letters next to
the data indicate significant difference at p < 0.05.

Table 9. Comparison of epipedon characteristics in forest and
cultivated areas by soil groups

Characteristics (1)        No. of soil group (2)

                              1               2

Thickness of epipedon   17/22a/a (4)      20/27a/b
  For/Arb (3), cm
BS of epipedon              91/96           86/92
  For/Arb, %
Ratio C: N For/Arb      17-20/9-11b/a   15-16/9-11a/a
[pH.sub.KCl] For          5.0/>7c/b      5.0/6-7c/b
  (O-hor)/Arb (A-hor)
[H.sub.8.2] For/Arb,     30-50/20-25    70-140/65-80
  kmol [ha.sup.-1]

Characteristics (1)          No. of soil group (2)

                               3                4

Thickness of epipedon      19/26a/b          14/23a/a
  For/Arb (3), cm
BS of epipedon               29/81            18/68
  For/Arb, %
Ratio C: N For/Arb      17-18/10-11a/a    37-39/12-13c/b
[pH.sub.KCl] For         4.3/5-5.6b/a      2.9/>5.0a/a
  (O-hor)/Arb (A-hor)
[H.sub.8.2] For/Arb,    240-260/100-110   75-100/140-200
  kmol [ha.sup.-1]

(1) BS--base saturation stage, [H.sub.8.2]--hydrolytical acidity;
(2) for soil group names see Tables 1 (by ESC) and 2 (by WRB),
whereas the exception is soil group 4, where on arable areas the
data are presented for podzolic gley-soils (LkG), which are
modified by cultivation of gley- and peaty podzols (LG, LG1); (3)
For--forest and Arb--arable soils; (4) letters next to the data
indicate significant difference at p < 0.05 between soil groups.
COPYRIGHT 2013 Estonian Academy Publishers
No portion of this article can be reproduced without the express written permission from the copyright holder.
Copyright 2013 Gale, Cengage Learning. All rights reserved.

Article Details
Printer friendly Cite/link Email Feedback
Author:Koster, Tiina; Kolli, Raimo
Publication:Estonian Journal of Earth Sciences
Article Type:Report
Geographic Code:4EXES
Date:Jun 1, 2013
Previous Article:Long-term storminess and sea level variations on the Estonian coast of the Baltic Sea in relation to large-scale atmospheric circulation/Tormisuse ja...
Next Article:Phosphatized organic nanostructures in the Cambrian Linguloid brachiopod Ungula inornata (Mickwitz)/Fosfatiseerunud orgaanilised nanostruktuurid...

Terms of use | Privacy policy | Copyright © 2022 Farlex, Inc. | Feedback | For webmasters |