158 MICHA£ DUDEK, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEASOILTA £ABAZ SCIENCE ANNUAL Vol. 70 No. 2/2019: 158–169 DOI: 10.2478/ssa-2019-0014

MICHA£ DUDEK*, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEATA £ABAZ

Wroc³aw University of Environmental and Life Sciences, Institute of Soil Sciences and Environmental Protection, Grunwaldzka 53 St., 50-375 Wroc³aw, Poland

Vertisols properties and classification in relation to parent material differentiation near Strzelin (SW Poland)

Abstract: Vertisols are characterized by high content of clay fraction that affects their specific morphological and physical features. The shrink-swell phenomena of clayey materials under specific moisture regime cause formation of cracks, wedge-shaped structural aggregates and slickensides on aggregate surfaces. It was formerly believed that these soils can be found only in tropical/ subtropical zones, thus Vertisols have not been expected to form under temperate climate of Central Europe. As a result, Vertisols are insufficiently recognized and documented on soil maps in Poland, including the Lower Silesia region. The aim of this study was to examine soils developed on clayey parent materials near Strzelin, focusing on their morphology, properties and classification issues. There was confirmed that soils developed from Neogene clays have vertic and mollic horizon, accompanied by stagnic or gleyic properties. However, not all soils fulfil the criteria for Vertisols due to the presence of surface or subsurface coarser-textured (sandy- or silty-textured) layers. Native differentiation of parent material and geomorphological processes were found the main factors, which control the spatial mosaic of Vertisols and black earths (Chernozems or Phaeozems). Keywords: Vertisols, Chernozems, Phaeozems, soil classification, mollic, clays

INTRODUCTION at undulating areas (Syers et al. 2001). It was believed that these soils can be found mostly in Bedrock lithology and mineralogy is considered one tropical/subtropical zones; therefore, for a long time, of the most important factors of pedogenesis as it may it was not expected for Vertisols to be formed under determine the soil development and soil basic proper- the temperate climates of Central Europe (Kovda and ties (Waroszewski et al., 2018, 2019). Among various Wilding 2004). soil types, Vertisols are particularly dependent on pa- Vertisols have been rarely recognized in Poland, rent material and lithology (Table 1). The Neogene thus it is difficult to estimate their distribution across and Quaternary clay-rich deposits and the country. Moreover, clay-rich parent materials regoliths provide a unique primary material for occur generally in small patches in Poland, thus Vertisol formation. Vertisols cover approximately 350 drawing the contours of Vertisols in mosaics with million ha of Earth's surface and the largest areas of other soils may be difficult, in particular on small- Vertisols were identified in Australia, United States, scale maps. Vertisols often have dark-coloured and Sudan and India (Ahmad 1996, DeCarlo and Caylor thick topsoil A horizons underlain by subsoil layers 2019). Vertisols featured by high clay content are with strong redoximorphic features, thus they can be difficult to cultivate, although they may have large confused with black earths (£abaz and Kaba³a 2014). reserves of nutrients for plants (Miller et al. 2010, The Polish soil classification has not distinguished Pal et al. 2012). Genesis of these soils is related to Vertisols as separate unit for a long time and only the shrink-swell phenomena of expandable clay suggested their existence as "smolnice" (the term minerals that may occur under specific moisture derived from Balkan tradition). Smolnice have been regime, i.e. alternating strong water saturation and identified in northern Poland, including vicinity of deep soil drying (Kaba³a et al. 2015b, Miller et al. Gniew, Ciechanów, Kêtrzyn and Reszel (Mocek et 2010). The most typical environments for Vertisols al. 2009, Orzechowski et al. 2014, Owczarzak et al. formation are tropics and subtropics because of 1993; Prusinkiewicz 2001; Uggla and Witek 1958). extremely dry and extremely wet seasons (Table 1). Based on current knowledge and existing soil classi- Vertisol formation is supported by preferential fication of Poland (Kaba³a et al. 2019a), the humus- seasonal water accumulation in the local depressions rich "smolnice" may be classified as a "wertisole

* MSc Micha³ Dudek, [email protected] http://ssa.ptg.sggw.pl/issues/2019/702 Morphology and classification of Vertisols in relation to parent material differentiation 159

TABLE 1. Examples of Vertisols across the world

noitazilacoL lairetamtneraP detamitsE enozetamilC naeM launnanaeM lanigirO secnerefeR dnal rialaunna noitatipicrep oitacifissalc egarevoc -arepmet )ah( )C°(erut aidnI stlasaB nlm9.27 dimuh,tsiomdira-imes 93 0051–003 srugeR 1002.latelaP tsiomdimuh-bus,laciport naduS stnemideslaivullA nlm07 dimuh/dira-imes 81 0021toCkcalB not 6991damhA slios ailartsuA ciozoseM nlm07 dira-imes 12 008–003 kcalB 6991damhA enotsyalc shtraE saxeT suoereclaC nlm81 laciportbusdimuh 02 0511–067 slosumurG 4002.latetdroN yratnemides dna kcor slositreV ocixeM dnastlasaB nlm7.0 dimuh-bus 5.32 007–006 slosumurG .lateziuR-oletoS senotsemil slositreVdna 3102 niapS suoreficlaC nlm5.0 naenarretidem 51 007–003 naisuladnA zeugírdoR-zehcnáS senotsdnas shtraekcalb 7102.late aissuR eniramdnalaivullA – latnenitnocdimuh 8 005–004 smezotilS dnavortihK stnemides 4102avenvogoR aissuR stisopedenirtsucaL – latnenitnoc-artlu 2.4- 003lositreV ci 7102.lateadvoK slios eceerG enirtsucaldnareviR nlm3.0 naenarretidem 7.51 084 trerexolpaH 2102sakatsuoM stisopedenecotsielP dnaloP stisopedenecotsielP – etarepmet C°7 006B shtraekcal 9002.latekecoM citrevhtiw 1002zciweiknisurP seitreporp czarnoziemne" (chernozemic vertisols). The other Ver- sediments is highly differentiated. In general, Pleisto- tisols have been evidenced in central-western cene glacial materials, such as glacial till and glacio- Poland (Komisarek 2014, unpublished). Vertisols in fluvial sediments, dominate at land surface. The south western Poland are known from very few sites Neogene and Pleistocene glacial sediments quite often (Kaba³a et al. 2015a), although clays present at very are covered (or admixed) with Vistulian loess shallow depth are relatively common in this region (Badura et al. 2013, Jary et al. 2002). Although the (Kaba³a et al. 2015b). Quaternary sediments may reach a thickness of 40 m Therefore, the aim of this study was to verify and more, locally the Neogene clays may occur very diagnostic criteria for Vertisols in SW Poland accor- near or at land surface (Kural and Jerzmañski 1957). ding to Polish soil classification (Kaba³a et al. 2019a) The Neogene clays and clayey loams with admixture and to analyze the sources of soil variability at the of glacial till (evidenced by Scandinavian rock transitions between Vertisols and black earths. In fragments and coarse sand fraction) and eolian silt particular, the attention was paid to the possibility of (evidenced by higher content of silt fraction in the field recognition of the diagnostic features of mollic surface horizons compared to subsoil layers) occur and vertic horizons in clayey soils that has crucial in the vicinity of Dobrogoszcz village. Locally, also importance for the identification and classification the remnants of a glacio-fluvial (sandy) kames of Vertisols. contribute the landscape morphology and compo sition of surface sediments (Kural and Jerzmañski MATERIAL AND METHODS 1957). Mean annual air temperature in area under study Five soil pits were located on arable land nearby is 8°C, while the mean annual precipitation is 500– Dobrogoszcz village (Strzelin county 50°46'N, 600 mm. The majority of precipitation occurs in 17°01'E) at the foot of the Niemczañsko-Strzeliñskie warmer half of the year (April-September) and is Hills (Kondracki 2002) (Fig.1), where clayey parent between 350 and 400 mm. In colder months (Octo- material was previously evidenced at land surface ber-March) of the year the precipitation is clearly (GóŸdŸ 1957). However, the lithology of surface lower, between 150 and 200 mm. The annual clima- 160 MICHA£ DUDEK, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEATA £ABAZ

FIGURE 1. Location of the study area and soil profiles

tic water balance (precipitation minus evapotranspi- ration was calculated as a percentage of base cations ration) is slightly positive (+40 mm), mainly due to sum in an effective cation exchange capacity (base positive water balance in winter months. Whereas, cations plus exchangeable acidity). the climatic water balance in summer months is ne- Hard nodules of secondary carbonates were gative, that means the water shortage and soil dro- sampled in profile D1 for their age estimation using ughts are seasonally highly probable in this region, 14°C AMS (accelerator mass spectrometry) dating even under temperate climate (Pawlak and Pawlak technique in Poznañ Radiocarbon Laboratory. Calen- 2008). dar age for sample Poz-98379 was obtained using the The sequence of five soil profiles was localized OxCal 4.2 calibration program (Bronk Ramsey 2009) on a gently smooth SW slope. The arable fields (corn, based on the IntCal 13 calibration curve (Reimer et wheat, raps) are drained with an open-ditch network al. 2013). Calibrated ages are given in the 2σ range, (Fig. 1). All soil profiles were described and classified minimum and maximum values. according to Polish soil classification (Kaba³a et al. 2019a) and the FAO-WRB system (IUSS Working RESULTS Group WRB 2015). Soil samples, collected for labo- ratory analyzes from all horizons, were air-dried, All profiles in the catena have similar morphology, manually crushed and sieved using a 2 mm mesh. manifested in the following general sequence of soil Particle-size distribution was conducted using sieves horizons: Ap-ABig-Big. The thickness of A horizons for sand fractions and the hydrometer method for clay varied in a range from 31 cm (profile D4) to 70 cm and silt fractions after sample dispersion with (profile D2). The lower limit of A horizons has hexametaphosphate-bicarbonate, according to the different morphology. In some profiles, the transition legal standard PN-R-04032. Texture classes were to Bi horizon is smooth with narrow dark tongues; named after Polish (Polskie Towarzystwo Gleboznaw- while in other profiles the transition is irregular with cze 2009) (Table 3) and WRB classifications (IUSS thick tongues. In the most specific case of the profile Working Group WRB 2015). Soil organic carbon D2, fragments of underlying material are incorporated content was determined by dry combustion method into black matrix of A horizon (Fig. 2). Plough hori- (using the CS-MAT analyzer). Soil pH was measured zons generally have strong subangular and angular in distilled water and in 1M KCl solution (at a 1:5 blocky structure, in some profiles also the granular ratio). Content of calcium carbonates (equivalent) was one, variable in size (fine to coarse), and hard consi- determined volumetrically (Scheibler apparatus). stence in a dry state. The clods formed by ploughing Content of exchangeable base cations was determi- are coarse in size, but smaller than 30 cm in diameter ned by ICP-ES method after extraction with ammo- and always have internal blocky subangular structure, nium acetate (at pH 7) and exchangeable acidity was even if hard. Topsoil A horizons are black or nearly determined potentiometrically after extraction with black (10YR 2/1-3/1; Table 2), contain 1.6–2.5% of 1M KCl (Kaba³a and Karczewska 2018). Base satu- organic carbon and are featured with slightly Morphology and classification of Vertisols in relation to parent material differentiation 161

FIGURE 2. Toposequence of soil profiles alkaline reaction and very high base saturation probably are closed cracks filled with humus-rich (Table 4). Taking into account both morphological material from A horizon are recognizable in transi- and physico-chemical properties, the topsoil layers tional AB and Bi horizons of all profiles, in particular meet the criteria of diagnostic mollic horizon in all in the profile D5. soil profiles of the catena. The A horizons contain in The subsurface vertic horizons were identified in most cases more than 30% of clay fraction and have all profiles, according to both FAO-WRB system texture of silty clay loam, silty clay and clay loam (IUSS Working Group WRB 2015) and Polish soil classes (Table 3). Only the A horizon in the profile Classification (Kaba³a et al. 2019a). These horizons D2 has 19% of clay and texture class of loam. All A have all required diagnostic features of vertic horizons have higher content of silt fraction than the horizon, i.e. contain ≥30% of clay fraction (Table 3), subsoil layers, and the profiles located in the lower have a thickness of ≥25 cm (Table 2), the vertical slope positions (D3, D4 and D5) contain clearly more cracks (filled and seasonally closed; Fig. 3c), the silt that the profiles D1 and D2. Open cracks were wedge-shaped or lenticular structural aggregates and absent in A horizons during the pit digging and the slickensides on the surfaces of structural aggre- description; however, the narrow black tongues that gates (Fig. 3a, 3d). The presence of wedge-shaped 162 MICHA£ DUDEK, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEATA £ABAZ

TABLE 2. Field soil characteristics eliforP noziroH htpeD )tsiom(ruoloC erutcurtS ecnetsisnoC setanobraC DI )mc( xirtaM cihpromixO cihpromotcudeR tsiom yrd 1D pA 83–0 2/3RY01 – – RG/AS RF AH – giBA 07–83 1/3RY01 – – BA IF/RF AH – 6/5RY01 gckiB 501–07 6/5RY01 – 3/6Y5 EW+BA IFV/IF AH n gkiB 521–501 – 2/6Y5 4/5Y5.2 EW+BA IFE AHV + giB 061–521 – 6/6RY01 2/6Y5 EW+BA IFE AHV – liB 081–061 – 6/5Y5.2 1/7Y5.2 EW IFE AHV – 2D pA 53–0 1/2RY01 – – RG/BS RF AH – hA 86–53 1/2RY01 – – AS IF/RF AH – giB/A 59–86 1/2RY01 – 3/6Y5.2 EW+BS IFV AH – gC2 221–59 – 8/5RY5.7 3/6Y5.2 BA IF AH – gC3 031–221 – 8/5RY5.7 3/6Y5.2 BA IFV/IF AH – 1gC4 041–031 – 8/5RY5.7 3/5Y5.2 BA IF OS – 2gC4 051–041 – 8/5RY01 – BS IF OS – 3gC4 871–051 – 6/3RY5.2 – BS IF OS – 3D 1pA 81–0 1/2RY01 – – RG/AS RF AH – 2pA 04–81 1/2RY01 – – BA IF/RF AH – lkiB 86–04 – 6/5RY01 RY5.2 BA+EW IFV AHV + 6/3RY5.2 3/5 gckiB2 88–86 – 8/5RY01 4/5Y5.2 BA+EW IFE/IFV AHV n 8/5RY5.7 1gkiB2 011–88 – 6/5RY01 4/6Y5 BA+EW IFE AHV + 2gkiB2 531–011 – 6/5RY01 4/6Y5 BA+EW IFE AHV + 4D 1pA 41–0 1/2RY01 – – BS RF AH – 2pA 13–41 1/2RY01 – – BA IF/RF AH – giB 45–13 – 8/5RY01 2/5Y5 BA+EW IFV AHV – gkiB 501–45 – 8/5RY01 2/5Y5 BA+EW IFE/IFV AHV + gckiB 031–501 – 6/5RY01 2/5Y5 EW IFE AHV n liB 031> – 6/5RY01 2/6Y5 EW IFE AHV – 5D 1pA 51–0 1/2RY01 – – AS RF AH – 2pA 04–51 1/2RY01 – – BA IF/RF AH – gkiB/A 07–04 – 8/5RY01 1/5RY5.2 BA+EW IFE/IFV AHV + gckiB 001–07 – 6/5RY01 1/5Y5 BA+EW IFE AHV n lckiB 531–001 – 6/5RY01 1/5Y5 BA+EW IFE AHV n

Explanations: structure: GR – granular, AB – blocky angular, SA – blocky subangular and angular, SB – blocky subangular, WE – wedge-shaped; carbonates: + – few, n – hard nodules; consistence (moist): FR – friable, FI – firm, VFI – very firm, EFI – extremely firm; consistence (dry): SO – soft, HA – hard, VHA – very hard. aggregates with slickensides is visible not only in Bi, nodules, fine to moderate in size. Profile D2 is an but also in overlying transitional horizons and even exception, as it is poor in carbonates (up to 0.1%) or in lower parts of clayey A horizons. completely free of them in some layers; moreover, The content of carbonates in the profiles D1, D3, the highest content of carbonates (probably of anth- D4 and D5 ranges from 0.1 to 9.8% and increases in ropogenic origin) is noted in the topsoil (Table 4). the profiles from the surface down to the depth of A predominance of stagnic properties is clearly 88–130 cm, where it reaches the maximum and then manifested in all subsurface horizons, though it decreases (Table 4). Surface horizons have signs of varies in intensity and contribution of reductomorphic decalcification, whereas the underlying transitional and oximorphic colours. Reductomorphic colours are horizons have visible accumulation of secondary represented with grey (2.5Y 5/2-4) or more olive (5Y (pedogenic) carbonates, mostly in the form of hard 5-6/1-4) colours. Reducing conditions are particularly Morphology and classification of Vertisols in relation to parent material differentiation 163

FIGURE 3. Effects of shrinking-swelling phenomena in soils under study: (a) shining surfaces on soil peds, (b) closed narrow cracks in the lowermost horizon in profile D5 with reductomorphic colours developing along the cracks, (c) fragments of subsoil material "incorporated" into A horizon in the profile D2; closed narrow cracks filled with dark (humus-rich) material, (d) slickensides on the surfaces of lenticular aggregates (cross section in the wall of the profile D1) visible along cracks, which most likely are seasonally DISCUSSION filled with stagnating (surface) water in a deep sub- soil horizons in the profile D5 (Fig. 3b), as well as on Diagnostic features and classification of soils the surfaces of wedge-shaped/lenticular aggregates in a catena (Fig. 3d). Among the oximorphic colours prevail such as 10YR 5/6-8 or more reddish 7.5YR 5/8. Deep sub- All soils in a catena have a subsurface vertic soil horizons (below the depth of 130 cm) of the horizons featured by: clayey texture (30% of clay profiles D1, D4 and D5 are featured with the gleyic fraction or more), presence of wedge-shaped (or lenticular) structural aggregates inclined at various properties (Table 2), resulting from permanent soil angle, slickensides on the surfaces of these aggre- saturation with infiltrating water. In profiles D2 and D3, the gleyic properties were noticed also at a depth gates, and cracks filled with humus-rich material of 68–95 cm and 40–68 cm, respectively. In both ca- falling from A horizon during dry seasons (when cracks ses the gleyic properties have developed within or presumably are open). All this confirms the shrink- directly above horizons having clearly higher clay swell phenomena to be active. With an exception of the profile D2, these vertic horizons have a thickness content that neighboring horizons. The reductomor- much larger than required 25 cm. Vertic horizons do phic colours of strongly saturated horizons are mo- stly grey (5Y5-6/1-2 or 2.5Y 7/1) and cover up to not have specific colour and may be both similar to 75–85% of the cross-section, including the internal underlying parent material, may be covered with a parts of soil aggregates. redoximorphic colour pattern, as well as may belong to A horizon (its lower part). The recognition of Vertisol requires both the presence of vertic horizon and, additionally, a clayey texture (i.e. ?30% of clay fraction) in all layers between soil surface and vertic horizon (IUSS Working Group WRB 2015, Kaba³a 164 MICHA£ DUDEK, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEATA £ABAZ et al. 2019a). Only the profiles D1, D4 and D5 fulfill All soils under study (including the Vertisol these two requirements; whereas the Ap horizon in profiles D1, D4 and D5) are seasonally excessively profile D2 and Bikl horizon in profile D3 have loamy saturated with surface water (from snow melting and texture classes with less than 30% of clay fraction precipitation) and are drained (using the open ditches). (Table 3). Due to seasonal saturation with water and reducing The other important issue under consideration was conditions, all soils have well developed stagnic the recognition of mollic horizons in clay-textured properties starting directly below the A horizon and soils. All topsoil A horizons contain >1.6% of organic covering vertic horizons/subhorizons. The loamy Bikl carbon, have black or nearly black colour, slightly horizon in the profile D3 (at a depth of 40–68 cm), alkaline reaction and base saturation much higher than underlain by much finer clay loam, is probably much 50% (Table 4), thus meet basic morphological and longer saturated with water (compared to other soil physico-chemical criteria for diagnostic mollic horizon. layers), thus the reductomorphic colours dominate in However, the possibility of mollic horizon presence this horizon and gleyic properties may be recognized in clay-textured soils in Poland was questioned (Po- instead of stagnic properties. Although the calcic lish Soil Classification 2011) due to its hard consi- horizons are absent, the accumulation of secondary stence and massive structure in a dry state. In fact, carbonates in subsurface horizons allows to recognize the soil consistence in the plough horizons is hard in the protocalcic properties in profiles D1, D4 and D5 a dry state; however, the structure is in all horizons (and also D3, as stated above). blocky subangular and angular, in some parts even Finally, the Vertisols in profiles D1, D4 and D5 granular. The clods produced by ploughing (angular have in their full names, derived after the WRB rules blocks) are smaller than 30 cm in diameter and (IUSS Working Group WRB 2015), only one prima- always have internal blocky structure. Thus, even if ry qualifier – Pellic. The Pellic qualifier refers to the the consistence of aggregates is hard in dry state, the presence of thick and dark topsoil A horizon (that may aggregate structure of topsoil horizons cannot be or may not meet the criteria for mollic horizon). An recognized as massive following the diagnostic expected Grumic qualifier (that refers to the presence requirements for mollic horizon (IUSS Working of a self-mulching fine-structural topsoil layer) is Group WRB 2015, Kaba³a et al. 2019a). Taking into disputable, as this layer may be easily destroyed by account both morphological and physico-chemical ploughing, thus may occur in these soils only seaso- properties, including the non-massive structure, the nally. During the profile description, the self-mulching topsoil horizons meet the criteria of diagnostic layers have not been recognized. Moreover, the mollic horizon in all soil profiles under study. following supplementary qualifiers may be added: Soils in the profiles D2 and D3 have a thick Aric (soils are ploughed to the depth of 20 cm and mollic horizon and slightly alkaline or alkaline more), Protocalcic, Drainic, Humic, Mollic and reaction, connected with high base saturation Katostagnic, as explained above (Table 3). throughout the profile that allows their classification, According to Polish Soil Classification (Kaba³a respectively, as Phaeozem (no calcic/protocalcic et al. 2019a), profiles D1, D4 and D5 are "chernoze- properties) or Chernozem, if the calcic/protocalcic mic vertisols", where vertic and mollic horizons properties are present in subsurface layers (IUSS (thicker than 30 cm) are required and stagnic proper- Working Group WRB 2015). It must be stated that ties typically are presumed (Table 3). the present definition of chernic horizon (IUSS Wor- king Group WRB 2015) requires a granular or fine Origin of soil variability in the landscape subangular blocky structure that would not be the case of Ap horizon in the profile D3 (as in many other A recognition of Vertisols as a separate soil unit is ploughed layers of chernozemic soils), shifting this highly dependent on the clayey soil texture and any soil to Kastanozems. However, this error has already coarse-textured admixture or layering may result in a been identified by WRB Working Group and the change of soil classification, as these additions may change of the size criteria for structural aggregates in weaken or prevent the shrinking-swelling phenomena chernic horizon has been agreed (+, personal communi- (DeCarlo and Caylor 2019; Miller et al. 2010). cation). Also according to Classification of Polish Soils Meanwhile, the spatial and vertical variability of (Kaba³a et al. 2019a), the profiles D2 and D3 cannot sediments, and therefore also soil texture, is common be named vertisols, but "vertisolic black earths" di- in the post-glacial landscapes of Poland, including stinguished as soils that have mollic horizon, strong the Lower Silesia region (Kaba³a et al. 2015b). This redoximorphic features and vertic horizon, but do not is a result of repeated Pleistocene glaciations, have clayey texture in all horizons from the surface erosion of glacial materials, Late Pleistocene (peri- down to the vertic horizon (final soil names are given in Table 3). Morphology and classification of Vertisols in relation to parent material differentiation 165 LCiS LCiS LCiS LCiS CiS CiS CH CH CH CH CH CH CH CH LC LC LC LS LS LS LS L L C C C C C C C C ssalcerutxeT iypg iypg iypg – clay loam, HC heavy ypi ypi ypi ypi ypi zg ig zg ig pg ig pg lg pg zi ci zi zi ci zi ci ci zi zi ci ci ci ci , CL 54 44 54 24 84 57 54 54 65 46 83 35 55 23 53 62 15 46 26 43 18 48 38 13 86 13 91 81 41 71 31 )ciugnoT,citparodnE,cihcaP,cimaolodnE,ciyalconA,cir , iz – i³ zwyk³y; C clay )cingatsodnEcitparodnE,cihcaP,ciyalC,ciclacotorP,ci 20.0 200.0< GTP ADSU 03 82 82 23 42 03 82 43 03 42 03 82 62 52 62 82 12 81 41 51 81 31 81 61 9 4 8 8 6 4 6 )cingatsotaK,cilloM,cimuH,ciniarD,ciclacotorP,cirA( )cingatsotaK,cilloM,cimuH,ciniarD,ciclacotorP,cirA( )cingatsotaK,cilloM,cimuH,ciniarD,ciclacotorP,cirA( 22 02 02 02 21 61 41 81 21 01 81 81 61 81 61 9 4 6 2 4 3 2 6 2 8 8 8 8 2 2 2 03 02 42 22 62 01 21 01 41 01 21 8 6 4 8 8 6 8 8 8 4 4 4 8 6 6 8 6 9 2 2 64 64 04 54 41 41 61 31 7 2 1 0 0 5 4 4 2 2 0 3 2 2 5 0 6 8 2 1 1 1 1 A(mezoeahPcingatsodnEcitreV/awokitrewaimeizanrazC–2 )mm(snoitcarfezis-elcitrapfoegatnecreP 7 7 2 2 0 2 2 3 0 3 3 6 9 6 3 0 0 0 0 0 2 9 0 1 1 1 1 1 1 1 1 rA(mezonrehCcitreV/awokitrewaimeizanrazC–3DeliforP 4 4 0 0 2 0 2 6 0 3 2 0 0 0 0 0 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 lositreVcilleP/ynmeizonrazclositreW–5DeliforP lositreVcilleP/ynmeizonrazclositreW–4DeliforP – sandy loam. lositreVcilleP/ynmeizonrazclositreW–1DeliforP 0 0 0 0 0 0 0 0 0 0 0 0 0 2 0 0 0 0 0 0 0 0 0 0 0 0 0 1 1 1 1 – silty clay loam, SL 0 5 0 0 0 0 5 0 0 0 0 0 0 0 0 0 0 0 5 0 0 0 0 0 0 0 0 0 0 0 0 , SiCL 531–001 031–501 521–501 061–521 081–061 031–221 041–031 051–041 871–051 531–011 001–07 501–45 501–07 221–59 011–88 07–04 86–04 88–86 07–83 86–53 59–86 04–51 13–41 45–13 04–81 83–0 53–0 51–0 41–0 81–0 031> mc 2> 1–2 5.0–1 52.0–5.0 1.0–52.0 50.0–1.0 20.0–50.0 200.0– oiolo htpeD nozirohlioS 3. Particle-size distribution of the soils under study DeliforP – loam, SiC silty clay gkiB/A gckiB2 1gkiB2 2gkiB2 gckiB lckiB gckiB gckiB giB/A 1gC4 2gC4 3gC4 giBA , L gkiB lkiB gkiB 1pA 2pA 1pA 2pA 1pA 2pA gC2 gC3 liB giB giB liB pA hA pA TABLE Explanation: gi – glina ilasta, gl lekka, gp piaszczysta, gpyi pylasto-ilasta, gz zwyk³a, ic i³ ciê¿ki, ipy pylasty clay 166 MICHA£ DUDEK, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEATA £ABAZ

TABLE 4. The physicochemical properties of soils under study

DIeliforP noziroH htpeD Hp Hp OCaC 3 C N --egnahcxE fomuS esaB )mc( H2O lCK ytidicaelba esab noitarutas snoitac % gk·)+(lomc( 1– ) 1D pA 83–0 05.7 76.6 12.0 46.1 21.0 66.2 5.22 98 giBA 07–83 67.7 74.6 41.0 06.0 50.0 09.1 2.42 39 gckiB 501–07 64.8 63.7 08.6 81.0 .d.n 59.0 7.84 89 gkiB 521–501 21.8 50.7 72.2 21.0 .d.n 02.1 3.55 89 giB 061–521 30.8 21.7 44.1 70.0 .d.n 03.1 0.64 79 liB 081–061 01.8 00.7 43.0 80.0 .d.n 03.1 9.24 79 2D pA 53–0 02.7 15.6 11.0 63.2 71.0 42.3 4.12 78 hA 86–53 32.7 53.6 40.0 54.1 11.0 41.3 0.12 78 giB/A 59–86 37.7 13.6 60.0 35.0 40.0 05.2 0.33 39 gC2 221–59 00.8 85.6 40.0 41.0 .d.n 20.1 02.1 45 gC3 031–221 02.8 57.6 20.0 22.0 .d.n 34.1 21.2 06 1gC4 041–031 92.8 00.7 20.0 90.0 .d.n 58.0 71.1 85 2gC4 051–041 53.8 01.7 00.0 21.0 .d.n 86.0 14.1 76 3gC4 871–051 82.8 60.7 00.0 30.0 .d.n 86.0 3.11 49 3D 1pA 81–0 24.7 17.6 60.0 30.2 61.0 70.2 2.52 29 2pA 04–81 96.7 30.7 71.0 00.2 41.0 08.1 2.32 39 lkiB 86–04 43.8 75.7 73.4 32.0 20.0 97.0 6.62 79 gckiB2 88–86 12.8 04.7 57.9 32.0 .d.n 59.0 1.93 89 1gkiB2 011–88 41.8 13.7 54.4 81.0 .d.n 02.1 3.93 79 2gkiB2 531–011 90.8 91.7 78.1 11.0 .d.n 01.1 1.83 79 4D 1pA 41–0 62.7 51.6 60.0 50.2 61.0 43.2 2.52 29 2pA 13–41 64.7 33.6 40.0 99.1 41.0 74.2 7.72 29 giB 45–13 42.8 98.6 53.0 82.0 20.0 41.1 9.82 69 gkiB 501–45 33.8 90.7 98.3 61.0 .d.n 59.0 7.24 89 gckiB 031–501 42.8 62.7 28.9 12.0 .d.n 41.1 3.44 79 liB 031> 92.8 40.7 97.0 60.0 .d.n 00.1 0.14 89 5D 1pA 51–0 99.7 61.7 80.1 74.2 81.0 26.1 6.04 69 2pA 04–51 61.8 61.7 14.1 71.2 61.0 33.1 4.04 79 gkiB/A 07–04 73.8 61.7 07.1 65.0 50.0 41.1 3.55 89 gckiB 001-–07 44.8 23.7 86.8 01.0 .d.n 59.0 8.73 89 lckiB 531–001 62.8 82.7 02.6 11.0 .d.n 01.1 1.24 79

Explanation: n. d. – not determined.

TABLE 5. Radiocarbon date of carbonates nodule from profile D1

yrotarobaL gnilpmaS 41 )derusaem(egaC 41 egadetarbilacC edoc )mc(htped 97389–zoP 08–07 PB53–/+5193 PBlac7344–1424=CB1922)%4.59(CB7842

Explanation; BC – before Christ, BP – before present (1950). Morphology and classification of Vertisols in relation to parent material differentiation 167 glacial) eolian accumulation, and slope processes that was possible in the Holocene period, where the may both mix and translocate the sediments (Waro- summer and winter seasons became alternately szewski et al. 2019). All these transformations are enough dry and moist to allow the development of believed to occur subsequently in the catena under stu- wedge-shaped aggregates and slickensides in the dy. The main parent material for the local soils is Neo- clayey subsoil (Pal et al. 2012, Pierre et al. 2018). gene clay that contains here 45–84% of clay Kabala et al. (2015b) argue that the artificial drainage fraction and does not contain coarse gravel/stone after clearing the forest could promote the shrink- fractions (Table 3). Typical glacial tills are absent in swell phenomena by enhancing the topsoil drying in the catena under study, despite of at least two Scan- summer, even under generally moist temperate dinavian glaciations, which covered this area. The climate. Therefore, the post-Neolithic Subboreal-Sub- subrounded rock fragments (medium and coarse atlantic periods are considered favorable periods for gravels) are only relics of these tills admixed to the formation of vertic horizons and Vertisol deve- underlying clays (recognizable in particular in the lopment in arable lands of Central Europe (on a clayey profiles D4 and D5). High content of silt fraction in substrates). This hypothesis is convergent with an age the topsoil horizons, up to 48–50% in the profiles D4 of carbonate nodules from the profile D1 (Table 5). and D5, indicates eolian addition, which was very Radiocarbon date approximates the first part of Sub- common in the Lower Silesia during the Pleniglacial boreal period as a time of intense decalcification of period of the Last Glacial Maximum (Waroszewski initially carbonate-rich soil substrate due to strong et al. 2018). It is unknown, whether (1) the pure loess leaching driven by moist climate. The same environ- layer initially covered the soils in the catena and then mental factor (long term moistening of the climate) it was eroded, or (2) eolian silt was mixed by slope that led to carbonate leaching and supported the processes under periglacial conditions directly after shrink-swell phenomena (and formation of vertic its sedimentation and did not form separate silt layer. horizons), also resulted in a development of redoxi- Nevertheless, both these scenarios may result in a morphic features (mostly the stagnic properties), formation of similar silt-enriched mixed topsoil layer which strong expression is important diagnostic (Waroszewski et al. 2018). feature. Possibility of "gilgai" microrelief formation Moreover, eroded remnants of the kame-type land- in SW Poland was confirmed by Kabala et al. (2015b), form (consisting of glacio-fluvial sediments) have also on gentle slopes. However, the presence of been recognized east of the catena (Kural and Jerz- "gilgai" in the catena under study has not been iden- mañski 1957). Sands from the eroded kame could tified as it is typically destroyed by regular and deep reach the upper part of the catena that is recognizable ploughing (modern agriculture activities) that led to as clearly higher content of sand fraction in topsoil surface flattening. horizons of profile D2 and, to a lesser extent, of profile D3 (Table 3). The presence of medium and CONCLUSIONS coarse sand in the profile D3 confirms the importance of slope processes that transported the soil material The analyses of morphological features of soils downward along the slope. The most disputable is located near Strzelin allow confirming the presence the origin of "clayey sand" (sandy loam in terms of of Vertisols in this area. Clay-rich parent material, in pedological texture classifications) present in the sub- combination with seasonally alternating water satu- soil layers of the profile D2. The most probable is ration promotes the formation of vertic properties that sand-rich material is a lens of fluvial/lacustrine (slickensides and deep cracks) also under temperate sediments interbedding the Neogene clays. However, climate of SW Poland. Moreover, seasonal soil satu- it is only a hypothesis as no deep excavation or ration with water allows stabilization and accumula- drilling was made to check it. tion of the organic matter in topsoil layer. Under Undoubtedly, the current morphology of the these conditions, humus-rich Vertisols featured by profiles and soil properties are a result of different thick mollic horizon form a spatial mosaic with other phases of pedogenesis. It is believed that thick humus-rich soils – Phaeozems and Chernozems. High chernozemic horizons started to form in south- spatial variability of Vertisols and accompanying western Poland as early as in Late Pleistocene soils is an effect of textural soil variability, resulting (Kabala et al. 2019a). It is also probable that the A both from native variability of parent materials and horizons have been "rejuvenated" and deepened geomorphological processes. Similar to black earths since the Neolithic period, i.e. after large-scale forest Pellic Vertisols (having thick mollic horizon) in SW clearing and spreading of the forest-steppe vegetation Poland are believed to be relatively young Holocene (£abaz et al. 2019). The formation of vertic horizon soils, which development was possible due to the 168 MICHA£ DUDEK, JAROS£AW WAROSZEWSKI, CEZARY KABA£A, BEATA £ABAZ human-driven large scale forest clearing and soil Kaba³a C., Przyby³ A., Krupski M., £abaz B., Waroszewski J., drainage. Consequently that created conditions for 2019b. 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Received: May 8, 2019 Accepted: August 5, 2019 Associated editor: W. Szymañski

W³aœciwoœci i klasyfikacja wertisoli w warunkach zró¿nicowania utworów macierzystych w rejonie Strzelina (SW Polska)

Streszczenie: Wertisole to gleby charakteryzuj¹ce siê wysok¹ zawartoœci¹ frakcji i³owej, która przek³ada siê bezpoœrednio na ich morfologiê i w³aœciwoœci fizyczne. Zdolnoœci do cyklicznego kurczenia siê i pêcznienia minera³ów ilastych, w naprzemiennie wystêpuj¹cych porach suchych i wilgotnych, powoduj¹ powstawanie w tych glebach g³êbokich szczelin, wrzecionowatych agregatów i g³adkich powierzchni œlizgu na powierzchniach agregatów. W przesz³oœci uwa¿ano, ¿e wertisole wystêpuj¹ g³ównie w strefie tropikalnej lub subtropikalnej i do tej pory nie wykazywano ich obecnoœci w umiarkowanym klimacie œrodkowej Europy. W efekcie wertisole nie zosta³y wystarczaj¹co przebadane i opisane w Polsce, w tym na Dolnym Œl¹sku. Celem niniejszej pracy by³a analiza gleb ilastych wystêpuj¹cych w rejonie Strzelina ze szczególnym uwzglêdnieniem ich morfologii, w³aœciwoœci i klasyfikacji. Wykazano, ¿e gleby wytworzone z neogeñskich i³ów maj¹ poziomu diagnostyczne vertic i mollic, którym towarzysz¹ w³aœciwoœci gleyic lub stagnic. Jednak¿e nie wszystkie gleby spe³niaj¹ kryteria wertisoli ze wzglêdu na obecnoœæ powierzchnio- wych lub podpowierzchniowych poziomów o grubszym uziarnieniu. Stwierdzono, ¿e g³ównymi czynnikami decyduj¹cymi o przestrzennej mozaice wertisoli i czarnych ziem s¹ ró¿nicowanie materia³u macierzystego oraz procesy geomorfologiczne. S³owa kluczowe: wertisole, czarnoziemy, czarne ziemie, klasyfikacja gleb, mollic, i³y