Anthropogenic Transformation of Soils in the Barycz Valley – Conclusions for Soil Classification 103 SOIL SCIENCE ANNUAL DOI: 10.1515/Ssa-2015-0001 Vol

DE DE GRUYTER OPEN Anthropogenic transformation of soils in the Barycz valley – conclusions for soil classification 103 SOIL SCIENCE ANNUAL DOI: 10.1515/ssa-2015-0001 Vol. 65 No. 3/2014: 103–110

BEATA £ABAZ*, ADAM BOGACZ, CEZARY KABA£A

Uniwersytet Przyrodniczy we Wroc³awiu, Instytut Nauk o Glebie i Ochrony Œrodowiska ul. Grunwaldzka 53, 50-375 Wroc³aw

Anthropogenic transformation of soils in the Barycz valley – conclusions for soil classification

Abstract: Large-scale river regulation, drainage and intense farming in the Barycz valley initiated in 17th century activated a transformation of the initial alluvial and swamp-alluvial soils. Soils on the Holocene flooded terraces have deep, acid humus horizons (umbric) and gleyic properties at shallow depth, but have no stratification of parent material to a depth of 100 cm. Despite the location in the floodplain, soils cannot be classified as black-earth alluvial soils (mady czarnoziemne) using the criteria of Polish soil classification (2011). The soils on the Pleistocene non-flooded terraces have a deep, base-saturated humus horizon (mollic) and gleyic properties in the lower part of soil profile, which allows to classify them as the black earths (czarne ziemie). Prominent stratification of the parent material well preserved in these soils has no influence on their classification (due to the age sediments). Almost all humus horizons of these soils meet the definition of anthric characteristics, and more than half of the studied soils can be classified as culturozemic soils – rigosols – which emphasises the important role of man in the transformation and gaining of morphological features of these soils. The lack of precise criteria for identifying soil types in the chernozemic order of the Polish soil classification (2011) causes difficulties in the classification of soils on the river terraces, in particular, in distinguishing between black-earth alluvial soils and black earths.

Keywords: „chernozemic alluvial soils”, black earths, culturozemic soils-rigosoils

INTRODUCTION diagnostic horizons, such as mollic, umbric, and murshic, as well as cambic or sideric, which are typical for From the beginning of the 19th century, the soils of other soil types (Chojnicki 2002; D¹bkowska-Naskrêt the river valleys, both in Poland and in other European 1990; Kaba³a et al. 2011). Despite the fact that alluvial countries were largely anthropogenically transformed soils obtain features of black earths, brown earths and as a result of intensive hydro-engineering projects. others (depending on site conditions and degree of The aim of river regulation was not only to protect human interference), the soils may still be classified endangered residential areas against flood, but also as “alluvial soils”, according to the Polish soil to increase the agricultural area, for which was a huge classification (PSC 2011), even if the conditions of demand at that time (Strzemski 1961). Hydrotechnical alluvial environment disappeared. In this regard, the investments were carried out throughout Poland, both PSC (2011) is inconsistent, as has predicted two in the valleys of the biggest rivers (the Vistula and exceptions: (1) heavily gleyed alluvial soils may not the Oder) and in a series of smaller rivers, including be classified as “alluvial soils”, but as gley soils, and Barycz river. Elimination of flooding and river-flow (2) as a rule, the originally alluvial soils on the regulation reduced the natural alluvial sedimentation, Pleistocene non-flooded terraces are not classified as but also led to the degradation, or even the total loss alluvial soils, even if they possess stratified parent of wetland and bog habitats (Klimowicz 1980; Szty- material. In addition, the systematic position of allu- ber and Paw³at 2008; Uziak et al. 2010). In the drained vial soils, which have gained the features of culturo- river valleys, the rapid increase of the biological zemic soils (anthrosols), is unclear. activity and the vertical extent of soil-forming processes The aim of the study is to analyse the alluvial so- are observed as a result of the ground-water table lowe- ils transformation in the Barycz valley, which has been ring (Chojnicki 2002; Laskowski 1986; Rytlewski 1965). taking place under long-lasting and intense human Transformation of the morphological, physical, pressure. In addition, the study aimed to classify the chemical and mineralogical soil properties causes the soils according to the current version of the Polish gradual loss of the original sediment stratification soil classification (2011), as well as to the international (fluvic) and enhances subsequent development of soil classification (IUSS Working Group WRB 2014).

* [email protected] http://www.degruyter.com/view/j/ssa (Read content) 104 BEATA £ABAZ, ADAM BOGACZ, CEZARY KABA£A

MATERIALS AND METHODS capacity (CEC) and base saturation (BS) were calcu- lated. The study was conducted in the Barycz valley, in the Milicz and ¯migród depressions, which were formed RESULTS by huge water flow from the melting continental glacier during Warta (Riss) glaciation. High intensity fluvial The parent material stratification, which is charac- processes have filled the valley bottom with sand teristic of alluvial soils, was not visible in the soils sediments, which later, locally, underwent eolian on the Holocene flooded terraces to a depth of 100 processes that formed the numerous sand dunes. cm (Fig. 1), but was generally easily recognisable in The Barycz valley, initially dissected by many the soils of the Pleistocene flooded terraces (Fig. 2). active and inactive river channels and tributaries, and The stratification of the soil materials, in accordance regularly flooded, was in the past covered by extensive with the criteria for the fluvic materials, was recognised swamps (Bac 1949, Czy¿ewski 1949). An unique as a vertical diversity of soil texture (profiles 5–7) feature of this area is the numerous breeding fishponds, followed by stronger redoximorphic features or irregular established since the Middle Ages. Their construction accumulation of the organic matter throughout the was favoured by the flat terrain, the occurrence of soil profile (profile 6). Redoximorphic features (gleyic excavations after bog iron exploitation, small declines mottles and Fe-Mn segregations) were visible in all in the Barycz river, and a relatively mild climate that soil profiles, but generally occurred with greater was favourable for fish farms (Ranoszek and Rano- intensity and at shallower depths in the soils located szek 2004). The necessity of flood protection, due to on the Holocene flooded terraces. This is due to lower expanding human settlements and the increased position occupied by these soils in the valley that demand for farmland (especially meadows and resulted in shallow groundwater level. pastures), caused expansion of the river artificial Groundwater was not sometimes observed in soil embankments along the river channel and large-scale profiles located on the Pleistocene non-flooded drainage, which resulted in soil overdrying on large areas terraces (profile 6). A characteristic feature of all of of the Barycz valley in the beginning of 19th century the studied soils was deep (30–62 cm) and dark coloured (Drabiñski and Sasik 1995). Numerous fish ponds were humus horizons (arable) having a granular or suban- closed, and, together with the adjacent areas, were taken gular blocky structure. Humus horizons were double under agricultural cultivation. or triple layered in all profiles, reflecting the different The present study included three soil profiles frequency and vertical extent of ploughing. The deepest located on the Holocene flooded terraces (1.5–3 m sub-layers of arable horizon (for example, in profiles above the river level) and three on the Pleistocene 1 and 5) were probably formed by a single ploughing, non-flooded terraces (5–10 m above the river level). and they have features of horizons A and B, or A and The soils studied were used as meadows (profiles 1, C. Furthermore, in all profiles, arable horizons were 2 and 7), arable fields (profiles 5 and 6), or as a forest sharply cut off from the other layers. (profile 11). The field works included description of the Below this abrupt boundary, the soil structure research area and soil morphology, including stratifi- changed rapidly, suppressing activity of macro- and cation of the parent material. A particular emphasis mesofauna (except for profile 6). The TOC content was put on the morphology of the humus horizons was relatively high (up to 5.61%) in humus horizons, and redoximorphic features. but it can be very diverse, both on Holocene flooded The following properties were determined in the and Pleistocene non-flooded terraces (Table 2). In fine earth particles (<2 mm): particle-size distribution profiles 2, 6 and 7, the high TOC content (1.9–3.8%) using the hydrometer and sieves; soil pH in distilled was maintained throughout the arable horizon, even water and 1 M KCl, potentiometrically; organic carbon to a depth of 40–50 cm, although there were always (TOC) using Tiurin method; the calcium carbonate slightly lower levels in bottom subhorizon. The high (CaCO3) content by the volumetric method (according TOC content in other profiles occurred only in the to Scheibler method); total nitrogen content (Nt) using uppermost subhorizons, and rapidly decreased in the the Kjeldahl method, and the hydrolytic acidity (Hh) lower-lying subhorizons (for example, from 1.7 to using the Kappen method. Exchangeable base cations 0.6% in profile 1). TOC content was much smaller in (Ca2+, K+, Mg2+, Na+) were extracted using 1M subsoil (0.01–0.36%), and was related to the soil ammonium acetate at pH=7 and analysed by atomic texture– in sands, the content did not exceed 0.1%, absorption (Mg) and emission (Ca, K, Na) spectro- and higher values were only recorded in loamy sands photometry. Based on the sum of exchangeable cations and loams. All arable horizons had relatively high (S) and the hydrolytic acidity (Hh), the cation exchange nitrogen content, especially in surface subhorizons Anthropogenic transformation of soils in the Barycz valley – conclusions for soil classification 105

FIGURE 1. Soils on the Holocene river terraces (potentially flooded): A – Profile No. 1: Gleyic Umbrisol (Anthric, Arenic), B – Profile No. 2: Gleyic Umbrisol (Anthric, Arenic), C – Profile No. 11: Endoeutric Umbric Gleysol (Anthric, Arenic, Nechic, Pachic)

FIGURE 2. Soils on the Pleistocene river terrace (non-flooded): A – Profile No. 5: Calcaric Cambic Endogleyic Phaeozem (Anthric, Arenic), B – Profile No. 6: Greyzemic Endogleyic Phaeozem (Anthric, Arenic), C – Profile No. 7: Greyzemic Fluvic Endogleyic Phaeozem (Anthric, Arenic) 106 BEATA £ABAZ, ADAM BOGACZ, CEZARY KABA£A

TABLE 1. Selected morphological properties and particle size distribution in soil profiles on the river Holocene and Pleistocene terraces in the Barycz valley

eliforP lioS htpeD roloC erutcurtS civulF citsongaiD ]%[noitubirtsidezis-elcitraP ssalcerutxeT .oN noziroh ]mc[ lairetam snoziroh seitreporpdna 50.0–0.2 200.0–500.0 200.0< )dedoolfyllaitnetop(secarretrevirenecoloHehtnoslioS )cinerA,cirhtnA(losirbmUciyelG 1 1pA 01–0 1/3RY01 ralugnabus – cirbmu 69 3 1 S/lp 2pA 03–01 1/3RY01 ralugnabus – cirbmu 19 8 1 S/lp BA 25–03 1/4RY01 ralugnabus – – 39 6 1 S/lp C 06–25 2/8RY01 esool – – 89 1 1 S/lp gC 77–06 6/7RY01 esool – ciyelg 89 1 1 S/lp g2C 77> 4/7RY01 esool – ciyelg 69 3 1 S/lp )cinerA,cirhtnA(losirbmUciyelG 2 1pA 8–0 1/2RY01 ralugnabus – cirbmu 37 32 4 LS/pg 2pA 33–8 1/2RY01 ralugnabus – cirbmu 57 12 4 SL/gp g1C 05–33 3/6RY01 ralugnabus – ciyelg 59 4 1 S/lp g2C 05> 6/5RY01 ralugnabus – ciyelg 49 5 1 S/lp 11 1pA 51–0 2/2RY01 ralugnabus – cirbmu 18 01 9 LS/pg 2pA 04–51 2/3RY01 ralugnabus – cirbmu 88 5 7 SL/gp gpA 26–04 1/2RY01 ralugnabus – cirbmu 88 4 8 SL/lp gC 26> 3/8RY01 esool – ciyelg 39 4 3 S/lp )dedoolf-non(ecarretrevirenecotsielPehtnoslioS )cinerA,cirhtnA(mezoeahPciyelgodnEcibmaCciraclaC 5 1pA 32–0 2/3RY01 ralugnabus – cillom 48 01 6 SL/gp 2pA 64–32 3/3RY01 ralugnabus – cillom 77 71 6 SL/gp gBA 08–64 3/5RY01 ralugnabus – – 68 7 7 SL/gp gC2 08> 6/6RY01 ralugnabus – ciyelg 86 61 61 LS/pg 1/8RY01dna 6 1pA 32–0 1/3RY01 ralugnabus – cillom 78 9 4 S/sp 2pA 85–32 1/4RY01 ralugnabus – – 78 9 4 S/sp gC 531–85 2/8RY01 ralugnabus + ciyelg 68 11 3 S/sp g2C 531> 3/6RY01 ralugnabus + ciyelg 19 3 6 S/sp )cinerA,cirhtnA(mezoeahPciyelgodnEcivulFcimezyerG 7 1pA 61–0 1/2RY01 ralugnabus – cillom 58 31 2 SL/gp 2pA 24–61 2/2RY01 ralugnabus – cillom 58 11 4 SL/gp C 36–24 2/7RY01 ralugnabus – – 78 4 9 SL/gp gC 86–36 1/6RY01 ralugnabus + ciyelg 86 01 22 LCS/ipg g2C 58–86 2/7RY01 ralugnabus + – 49 1 5 s/sp g2C 09–58 1/7RY01 ralugnabus + ciyelg 88 1 11 sL/gp G 09> 1/6Y5 ralugnabus + ciyelg 29 1 7 S/sp

Explanations: Texture class according to PTG 2008 and USDA: pl, ps/S – sand, gp/SL – sandy loam, pg/LS – loamy sand, gpi/SCL – sandy clay loam.

(up to 0.45%). This ensures a narrow C:N ratio (in all horizons, at levels ranging from 2 to 20% (Table the range of 6 to 14.8) and indicated high biological 2). The cation exchange capacity (CEC) depends on activity and high rate of decomposition process. In the organic matter, the presence of residual carbonates, addition, this ratio also demonstrated a balance the soil reaction and soil texture, but only in deeper between the mineralisation and humification of subsoil horizons. The highest CEC value occurs in organic matter. the humus horizon and decreases with depth. In turn, Soils on the Holocene flooded terraces were either base saturation significantly increases along with the completely decalcified (profile 2) or had very low profile’s depth (except for profile 6). The base satura- calcium carbonate content (1–2%) in the deeper soil tion in the humus horizon of the soils on the Holocene horizons only, hence they had significantly more flooded terraces is much lower (24.6–66.7%) as compa- acidic reaction as compared to soils located on the red to the soils on the Pleistocene non-flooded terra- Pleistocene non-flooded terraces. In the Pleistocene ces (69.3–96.6%). terraces, the calcium carbonate occurred in almost Anthropogenic transformation of soils in the Barycz valley – conclusions for soil classification 107

TABLE 2. Selected physico-chemical properties in soil profiles on the river Holocene and Pleistocene terraces in the Barycz valley

eliforP lioS htpeD Hp OCaC 3 COT NT N:C aH S CEC ]%[sB .oN noziroh ]mc[ 1– H2O lCK ]%[ gk)+(lomc )dedoolfyllaitnetop(secarretrevirenecoloHehtnoslioS )cinerA,cirhtnA(losirbmUciyelG 1 1pA 01–0 3.6 1.5 0 07.1 31.0 7.21 3.3 3.2 6.5 1.14 2pA 03–01 6.6 7.5 0 06.0 60.0 0.01 1.3 0.3 1.6 2.94 BA 25–03 6.6 6.5 0 26.0 26.0 8.41 1.2 1.2 2.3 7.66 C 06–25 3.7 3.6 1 50.0 50.0 .o.n 2.1 2.1 5.1 0.08 gC 77–06 3.7 4.6 1 20.0 20.0 .o.n 3.1 3.1 5.1 8.48 g2C 77> 2.7 2.6 2 10.0 10.0 .o.n 3.1 3.1 6.1 6.08 )cinerA,cirhtnA(losirbmUciyelG 2 1pA 8–0 2.5 0.4 0 03.3 03.0 0.11 3.9 5.3 7.21 3.72 2pA 33–8 8.4 9.3 0 81.3 22.0 4.41 2.8 7.2 8.01 6.42 g1C 05–33 4.4 7.3 0 90.0 .o.n .o.n 8.1 0.1 8.2 0.53 g2C 05> 2.4 7.3 0 20.0 .o.n .o.n 6.1 9.0 5.2 9.43 11 1pA 51–0 9.3 2.3 0 16.5 54.0 5.21 1.7 0.3 1.01 0.03 2pA 04–51 5.4 0.4 0 58.0 60.0 2.41 0.5 1.4 1.9 8.44 gpA 26–04 2.5 6.4 0 99.0 70.0 1.41 3.3 6.6 9.9 7.66 gC 26> 1.7 4.6 1 02.0 .o.n .o.n 5.0 1.5 6.5 1.19 )dedoolf-non(ecarretrevirenecotsielPehtnoslioS E )ihcaP.cihceN.cinerc,cirhtnA(losyelGcirbmUcirtueodn 5 1pA 32–0 2.6 6.5 0 76.1 81.0 3.9 2.3 9.7 1.11 2.17 2pA 64–32 7.6 4.6 2 94.1 61.0 3.9 8.1 5.7 3.9 6.08 gBA 08–64 5.7 2.7 3 42.0 40.0 0.6 7.0 3.5 0.6 7.78 gC2 08> 7.7 3.7 2 10.0 .o.n .o.n 7.0 4.8 1.9 5.29 )cinerA,cirhtnA(mezoeahPciyelgodnEcimezyerG 6 1pA 32–0 6.7 4.7 02 59.2 62.0 3.11 9.0 3.52 2.62 6.69 2pA 85–32 7.7 3.7 4 09.1 12.0 50.9 9.0 0.31 0.31 0.39 gC 531–85 8.7 5.7 1 30.0 .o.n .o.n 5.0 0.4 5.4 9.98 g2C 531> 9.7 6.7 1 10.0 o.n .o.n 5.0 9.2 4.3 1.58 )cinerA,cirhtnA(mezoeahPciyelgodnEcivulFcimezyerG 7 1pA 61–0 4.6 9.5 2 87.3 63.0 5.01 0.4 0.9 0.31 3.96 2pA 24–61 3.6 7.5 1 33.2 71.0 7.31 7.3 0.6 7.9 0.26 C 36–24 8.6 4.6 2 91.0 .o.n .o.n 1.1 8.2 8.3 4.27 gC 86–36 6.6 5.5 0 63.0 .o.n .o.n 2.2 6.6 8.8 1.57 g2C 58–86 1.7 8.6 1 91.0 .o.n .o.n 8.0 4.2 1.3 8.57 g2C 09–58 0.7 3.6 1 61.0 .o.n .o.n 2.1 2.4 4.5 8.77 G 09> 4.7 9.6 0 10.0 .o.n .o.n 8.0 9.2 7.3 6.97

DISCUSSION alluvium) was observed only on the Pleistocene terraces and generally not in soils derived from youn- All of the analysed soils that were formed from ger Holocene sediments. All of the examined soils the Holocene and Pleistocene alluvial sediments in have evolved in the direction of chernozemic-type the Barycz valley have thick humus horizons, which soils (having humus-enriched mollic or umbric horizon) are almost black, structural and rich in organic matter. under excessively moist conditions. Similar soils were They all fulfil the criteria for umbric (on the Holocene identified in the valleys and glacial valleys in south- flooded terraces) or mollic (on the Pleistocene non- central Poland, e.g. in the Kampinoski National Park flooded terraces) diagnostic horizons, despite the sandy (Konecka-Betley et al. 1996), the Sandomierz valley texture. Soil profiles do not have other diagnostic (Klimowicz 1980), the Roztocze region (Uziak et al. horizons and always have redoximorphic features 2010), the Bug valley (Borowiec et al. 2007), and in (gleyic properties). In some cases, these properties the Lower Silesia region (Kaba³a et al. 2011; £abaz are found directly below humus horizons, or rarely, et al. 2006). only in the bottom part of the profile. Soil stratification The basic question concerns the origin of the deep that is typical for the fluvic materials (unchanged humus horizons. On the Polish territory, mineral al- 108 BEATA £ABAZ, ADAM BOGACZ, CEZARY KABA£A luvial sediments with organic matter content high disappearance soil fauna activity directly below the enough to create black-coloured mollic/umbric horizons ploughing horizon. These findings contradict the with a thickness more of 30 cm rarely occur naturally natural formation of the humus horizons that involves (Strzemski et al. 1973). This type of river sediment is gradual development based on zooturbation (Ale- practically unknown from the Pleistocene period. xandrovskiy 2007). This confirms the opinion of Therefore, it is considered that the contemporary Strzemski (1954) that the majority of Polish black alluvial soils, which currently have deep humus earths, in particular on alluvial sediments, were formed horizons, were originally swamp-alluvial or bog- primarily as a result of human intervention in the alluvial soils that were periodically flooded or were river valley environment – river regulation, drainage located in the former river-beds channels and troughs and deep ploughing of drained swamp soils. overgrown by hydrophilic plants, in which the water PSC (2011) classifies soils that are ”developed periodically stagnated (Konecka-Betley et al. 1996; from fluvic material”, undergo flooding (and thus, are Kowaliñski 1952; Prusinkiewicz and Kowalkowski located on the Holocene flooded terraces), and have 1964; Tomaszewski 1956, 1957). In the context of mollic horizon as black-earth alluvial soils (mady current classifications, these soils would be classified czarnoziemne). Unfortunately, none of the studied as Histic Gleysols (IUSS Working Group WRB 2014), soils in the Barycz valley can be classified as this soil which, in PSC (2011), are reflected in different subtypes type. First of all, the term “developed from fluvic of ground-gleyed soils (gleby torfowo-glejowe, tor- material” is unclear. Fluvic materials are identified fiasto-glejowe, murszowo-glejowe, and murszowato- by their stratification, however, it disappears under glejowe). Relics of these soils still exist locally in the pedogenic transformation and cannot be recognized river valleys. Their transformation to mineral soils in any diagnostic horizon, particularly in the humus with thick humus horizons was the result of large-scale horizon. It may be easily recognised only below river regulation and drainage, which were conducted genetic or diagnostic horizons, sometimes in the bottom in the valleys (Klimowicz 1980). part of soil profile. Unfortunately, PSC (2011) does Intensive regulation of the Barycz river and its not define whether and at what depth fluvic material tributaries was mainly associated with the construction should occur in the soil profile. In the soils under of fishponds in the 17th century. The riverbed was investigation, which are developed from young alluvial canalised and embanked at large lengths. Numerous sediments on the Holocene flooded terraces, the channels and floodgates were built to pile up water stratification is not visible, at least to a depth of 100 used to fill the fishponds. An amelioration conducted cm or to groundwater table. It means that the alluvial in the area fundamentally changed the original nature (and classification) of these soils cannot be hydrographic network and led to the elimination of judged based on sediment stratification. flooding and lowering the groundwater table in large Moreover, the definition of black-earth alluvial areas. The former wetlands were drained and almost soils (mady czarnoziemne) requires the mollic horizon, disappeared, transformed into meadows, pastures and while in the Barycz valley soils derived on flooded even arable land (Bac 1949; Tomaszewski 1949). terrace have umbric horizons only. Mollic horizons Organic soils currently occupy only small areas in and the stratification of parent materials in soil profiles the valleys of ¯migród and Milicz region (Ranoszek occur in soils located on the Pleistocene non-flooded and Ranoszek 2004). The majority of the former terraces. Morphologically, these soils meet the swamps were turned into mineral soils after drying requirements of black-earth alluvial soils (mady czar- and ploughing. Organic horizons, which formerly noziemne), however, they are not included in this soil were lying on the soil surface, were mixed with type due to the location on the non-flooded terraces mineral subsoil. Nowadays, due to soil homogenisation (out of range of floodwater) and due to the Pleistocene by repeated ploughing and increasing activity of soil age of their parent material. fauna, the organic materials do not form separate All of the tested soils are morphologically similar horizons or inserted “lenses”, but are totally dispersed to each other and could be classified as one type – in the mineral topsoil, sometimes resulting in the black earths (czarne ziemie) – because all of them peaty or murshic-like characteristic of arable horizon have thick mollic/umbric humus horizon and gleyic (£abaz et al. 2006, 2011). properties in the soil profile. Soils on the Pleistocene Key facts, which indicate human impact on the non-flooded terraces can be classified as black earths formation of thick humus horizons include: (1) the (czarne ziemie). Unfortunately, the classification of sharp lower boundary of humus horizons, (2) abrupt the soils on the Holocene flooded terraces is much change of the soil structure, as well as (3) abrupt more problematic in the PSC (2011). According to Anthropogenic transformation of soils in the Barycz valley – conclusions for soil classification 109 the concept of chernozemic soil order (PSC 2011), ropogenic influences (e.g. deep ploughing) are reflected these soils should be primarily classified as black- in soil classification at second level (by addition of earth alluvial soils (mady czarnoziemne). However, the “Aric” qualifier), as these features are too week as mentioned above, only their occurrence on the to fulfil criteria of diagnostic horizons in the Antro- Holocene flooded terraces supports such classification, sols reference group (e.g. for hortic horizon). because they do not have fluvic materials in the profiles and they have umbric, rather than mollic, CONCLUSIONS diagnostic horizons. On the other hand, the soils studied can be also 1. Large-scale river regulation, drainage and intense classified as leached or gleyed black earths (czarne farming in the Barycz valley conducted since the ziemie wy³ugowane/glejowe) because the definition 17th century caused the transformation of the of these types involves “late Pleistocene and Holocene primary swamp-alluvial soils to mineral soils with parent materials, such as varied sands, loams, clays thick, black-coloured and structural humus horizons and silts on various origins, mostly rich in calcium (mollic and umbric). carbonates” (PSC 2011). Finally, the lack of clear 2. Due to imprecise criteria in the Polish soil classi- criteria, and especially the lack of classification key fication (2011), alluvial soils with umbric horizon, hinders the separation between black earths and can be classified both as black-earth alluvial soils black-earth alluvial soils (Kaba³a 2014; £abaz and and black earths. Kaba³a 2014). 3. Mollic and umbric horizons in all of the studied Moreover, PSC (2011) does not take into account soils were formed by deep ploughing and meet the the anthropogenic nature of some humus horizons, criteria of anthric horizons, which should be both in black earths and black-earth alluvial soils. reflected in soil classification at the lower level. Meanwhile, mollic/umbric horizons meet the criteria 4. Current definition of the rigosols causes contro- of anthric horizon in almost all of the studied profiles, versial classification of many alluvial soils as and it would be the most advisable to classify them culturozemic (anthropogenic) soils based on very as separate subtypes with an anthric horizon. However, deep ploughing only. it is not possible, because there is no mention in the 5. Polish soil classification (2011) should provide PSC (2011) that black-earth alluvial soils (mady clear criteria for precise distinguishing of soil czarnoziemne) can have a humus horizon of anthro- types in chernozemic order that reflect overlapping pogenic origin. In the four soil profiles (1 and 11 on combinations of diagnostic horizons and properties. the Holocene flooded terraces, and 5 and 6 on the Pleistocene non-flooded terraces) the humus (anthric) ACKNOWLEDGMENTS horizons have a thickness exceeding 50 cm, which meet the basic criteria for rigosols (culturozemic an- The study was financially supported by the Polish thropogenic soils). Thus, according to the PSC (2011), Ministry of Science and Higher Education (research the analysed soils belong to leached black earth – project no. N N310 090336). czarne ziemie wy³ugowane (profiles 2 and 7) and rigosols (profiles 1, 5, 6 and 11), regardless of location REFERENCES (flooded or non-flooded terraces) and age of alluvial sediment (Holocene or Pleistocene). Alexandrovskiy A.L., 2007. Rates of soil-forming processes in Due to the lack of stratification of the primarily three main models of pedogenesis. Revista Mexicana de Cien- cias Geológicas, 24(2): 283–292. alluvial materials in the upper part of the soil profile, Bac S., 1949. Zagadnienia hydrologiczne i plan rezerwatu w Do- none of the analysed soils belong to Fluvisols (IUSS linie Baryczy. Czasopismo Geograficzne. Kwartalnik Polskie- Working Group WRB 2014), which are considered go Towarzystwa Geograficznego 19, 1–4: 157–185. to be poorly developed alluvial soils. According to Borowiec J., Urban D., Mikosz A.I., 2007. 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Antropogeniczne przekszta³cenia gleb w Dolinie Baryczy – wnioski dotycz¹ce klasyfikacji gleb

Streszczenie: Wielkoskalowa regulacja, odwodnienia oraz intensywne rolnicze zagospodarowanie doliny Baryczy zainicjowane w XVII wieku uruchomi³y transformacjê pierwotnych gleb aluwialnych i b³otno-aluwialnych. Gleby na holoceñskich terasach zalewowych maj¹ g³êboki, kwaœny poziom próchniczny (umbric) i s¹ p³ytko oglejone, a do g³êbokoœci 100 cm nie zaznacza siê stratyfikacja materia³u macierzystego. Mimo po³o¿enia na terenach zalewowych, gleb tych nie mo¿na zaliczyæ do mad czarnoziemnych pos³uguj¹c siê kryteriami Systematyki gleb Polski (2011). Gleby na plejstoceñskich terasach nadzalewowych maj¹ g³êboki, wysyco- ny zasadami poziom próchniczny (mollic) i oglejenie w dolnej czêœci profilu, co przybli¿a je do czarnych ziem. Dobrze widoczna stratyfikacja materia³u macierzystego nie ma w tych glebach znaczenia klasyfikacyjnego ze wzglêdu na wiek osadów. Niemal wszyst- kie poziomy próchniczne spe³niaj¹ kryteria poziomu anthric, a ponad po³owa badanych gleb mo¿e byæ zaliczona do gleb kulturo- ziemnych – rigosoli, co podkreœla istotn¹ rolê cz³owieka w transformacji i kszta³towaniu cech morfologicznych tych gleb. Brak precyzyjnych kryteriów identyfikacji typów w rzêdzie gleb czarnoziemnych w Systematyce gleb Polski (2011) powoduje trudnoœci w klasyfikacji gleb na terasach rzecznych, a w szczególnoœci rozgraniczanie miêdzy madami czarnoziemnymi oraz czarnymi ziemiami.

S³owa kluczowe: mady czarnoziemne, czarne ziemie, gleby kulturoziemne – rigosole