DE DE GRUYTER 180 OPEN EL¯BIETA MUSZTYFAGA, CEZARY KABA£A SOIL SCIENCE ANNUAL DOI: 10.1515/ssa-2015-0035 Vol. 66 No. 4/2015: 180–190

EL¯BIETA MUSZTYFAGA*, CEZARY KABA£A

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

Lithological discontinuity in Glossic Planosols (Albeluvisols) of Lower Silesia (SW Poland)

Abstract: The paper focuses on Glossic Planosols (formerly Albeluvisols) with sandy topsoil widely represented in the north- eastern part of Lower Silesia (SW Poland), in the range of tills from the Odra and Warta glaciations (Riss glaciation). The aim of the study was to characterize the texture of these soils in the context of the origin of parent materials and present-day pedogenic processes. Both the sedimentological and granulometric indexes, unbalances clay (and silt) fraction, and ventifact pavement at the contact of underlying loam and topsoil sandy layer confirm, that the textural differentiation of the topsoil and subsoil horizons has not resulted from the pedogenic processes, but primarily from the lithological discontinuity of glacial and post-glacial parent materials. Particle-size distribution and granulometric indexes of albeluvic tongues in the glossic horizon also confirm that the tongues has not been formed by eluviation of the fine fractions from the loamy material, but primarily by filling the initial thin crack with the sandy material. The coarser-textured tongues foster a deep infiltration and stagnation of water, and the development of reductic conditions allows further widening and deepening of the albeluvic tongues.

Keywords: Glossic Planosols, Albeluvisols, textural differentiation, lithological discontinuity

INTRODUCTION “loam sandification (spiaszczenie gliny)” that preceded the concept of clay illuviation (“lessivage”), Soil texture is a fundamental parameter determining but involved differentiation not only in clay but also soil properties and land use. An analysis of the particle- in silt fractions (Konecka-Betley 1961, Sza³ata and size distribution can provide a lot of information about Komisarek 2014). genesis, litho- and pedogenetic processes, as well as Despite expected abundance, derived from geolo- taxonomic position of soil (Dobrzañski et al. 1977, gical and soil-agricultural maps (Kaba³a (ed.) 2015), Kowalkowski and Borzyszkowski 1977, Konecka- lithological discontinuity in soils was rarely described Betley 1979, Mycielska-Dowgia³³o 1980). Texture in the lowland part of Lower Silesia, excluding analysis is crucial in case of heterogeneous profiles stratification of alluvial soils (£abaz et al. 2014). of soils developed from stratified glacial deposits Meanwhile, it seems that in many soils classified (Zagórski 2001). Frequently, the textural differentiation previously as Albeluvisols (in Polish: gleby p³owe is often associated with lithological and facial changes zaciekowe spiaszczone), the large and abrupt vertical of glacial deposits, as well as may develop under textural differentiation results from primary lithological periglacial conditions (GoŸdzik 1973, Manikowska stratification rather than from eluviation of fine fractions 1997, Zagórski 1995, 1996). Recently, the lithological (Kaba³a (ed.) 2015). discontinuity within soil profile has been increasingly The aim of the work was (1) to characterize the recognized in various typological units, particularly nature and origin of textural differentiation in profiles in the lowland clay-illuvial soils (Kühn 2003, Œwito- of clay-illuvial soils of north-eastern Lower Silesia niak 2008, van Ranst et al. 2011), as well as in the and (2) to indicate the consequences of lithological mountain Podzols (Waroszewski et al. 2013a, b) and discontinuity for soil naming and classification. Cambisols (Kacprzak and Derkowski 2007). Some researchers avoid to recognize the lithological discon- MATERIAL AND METHODS tinuity between eluvial and illuvial horizons of Luvi- sols and related soils, as they have insufficient argu- The study focused on clay-illuvial soils (gleby ments to distinguish primary lithological features from p³owe) displayed in the Polish soil-agricultural map illuvial features. Pure pedological explanation of te- as having significant textural diversity, e.g. sand xtural differentiation was the base for the concept of texture in topsoil and loam in shallow subsoil, in the

* MSc. E. Musztyfaga, [email protected] http://www.degruyter.com/view/j/ssa (Read content) Lithological discontinuity in Glossic Planosols (Albeluvisols) of Lower Silesia (SW Poland) 181 north-eastern part of Lower Silesia. More than 20 were collected separately from the albeluvic tongues profiles were described and finally four representative (abbrev. „tongues”) and from angular aggregates ones are selected for this paper, as located in: the between tongues („aggregates”, abbrev. „aggreg.”), Oleœnicka Plain – profile 1 – Mi³oszyce and profile 2 as well as bulk, mixed samples were collected from – Bielawa, the Twardogórskie Hills – profile 3 – Gra- the whole horizon volume. bowno, and the ¯migrodzka Basin – profile 4 – Pru- Particle-size distribution of the fine earths (<2 mm) sice (Fig. 1). The profiles Mi³oszyce and Bielawa are was conducted using sand separation on sieves and located in a range of the Odra glaciation (the older the hydrometer method for silt and clay fractions, after Middle-Polish (Riss) glaciation, 300–230 ka), while sample dispersion with hexametaphosphate-bicarbonate, the profiles Prusice and Grabowno are in the range according to the standard PN-R-04032. The names of the Warta glaciation (the younger Middle-Polish of texture classes were given according to classification (Riss) glaciation, 210–130 ka). During the Vistulian of Polish Society of Soil Science (Polskie Towarzy- (the North-Polish (Würm) glaciation, 115–7.3 ka) se- stwo Gleboznawcze 2009) and the USDA classification vere periglacial conditions occurred in the area of (Schoeneberger et al. 2012), with an indication of do- Lower Silesia, which fostered the transport of sandy minant sand sub-fraction (Table 1 and 2). and silty materials, and enabled the accumulation of Based on the distribution of sand and silt fractions cover sands (Kondracki 2001, Manikowska 1997) and and subfractions, a set of granulometric indices proposed loess (Chlebowski and Linder 1991) of varying by Kowalkowski and Prusinkiewicz (1963) was thickness. Soils were described and classified according calculated, as well as other indices suggested by the to Polish Soil Classification (PSC 2011) and FAO-WRB WRB to be diagnostic for lithological discontinuity classification (IUSS Working Group WRB 2015). (IUSS Working Group WRB 2015). These include In each of the distinguished soil horizons and sub- the following ratios (Table 4): fine sand to medium horizons, soil samples were collected for laboratory sand (A), fine sand + very fine sand to medium sand analysis. In all soil profiles under investigation, the (B), fine sand to coarse sand (C), fine sand + coarse E/B horizons with albeluvic tongues were present, silt to coarse + medium sand (D), medium + fine + typically for Albeluvisols (IUSS Working Group very fine sand to coarse sand (E), very fine sand to WRB 2006), in PSC (2011) called “gleby p³owe medium sand (F), and very fine sand to fine sand (G). zaciekowe”. Thus, in the E/B and B/E horizons, samples For the comprehensive characteristics, the sedimen-

FIGURE 1. Location of soil profiles within study area. Profile designations: 1 – Mi³oszyce, 2 – Bielawa, 3 – Grabowno, and 4 – Prusice 182 EL¯BIETA MUSZTYFAGA, CEZARY KABA£A LCS LCS LCS LCS LCS LCS LCS LCS LCS LCS LSF LSF LSF LSF SFL SFL SFL SFL SFL SFL SFL LC SF L ssalcerutxeT ipg ipg ipg ipg ipg ipg ipg ipg ipg ipg gp gp gp gp gp gp lp gp ig zg pg lg pg pg 82 32 12 72 82 62 52 52 42 13 52 22 01 51 01 61 91 11 8 4 3 2 4 2 4 4 2 3 5 0 6 3 2 2 2 2 2 3 3 3 2 3 0 1 1 1 1 1 600.0–20.0 200.0< GTP 200.0–600.0 ADSU 61 51 41 01 01 5 8 2 9 2 8 9 3 3 8 8 9 7 8 4 1 6 8 5 12 71 31 01 11 11 11 2 8 6 9 6 5 3 9 7 5 6 7 4 3 8 7 2 01 41 31 41 31 31 81 71 41 01 01 41 31 71 71 51 11 11 9 7 9 9 9 6 34 04 74 22 02 42 63 23 83 93 43 63 42 22 62 72 82 23 33 65 13 83 72 41 32 32 32 12 52 92 02 41 01 81 31 51 31 01 21 71 01 11 11 11 7 5 5 9 )%(noitubirtsid)mm(ezis-elcitraP 01 2 1 4 5 4 7 5 5 9 9 8 5 8 5 5 4 1 6 2 2 2 3 3 4 4 4 0 0 0 2 2 5 0 0 1 1 1 1 1 1 1 1 1 1 1 1 1 0.2> 0.1–0.2 5.0–0.1 52.0–5.0 1.0–52.0 50.0–1.0 20.0–50.0 4 0 0 0 2 6 8 5 6 2 2 2 0 1 1 1 1 1 1 1 1 1 1 1 501–001 521–021 541–041 031–001 001–08 511–57 seugnot seugnot seugnot seugnot .gergga 58–26 04–42 21–6 htpeD )mc( xgtB/E2 36–85 1 1 7 22 52 9 01 8 3 51 lg LS noziroh gtB/E2 57–36 gtB/E2 26–04 gtB/E2 08–05 gtB/E2 08–25 E/gtB2 .gergga E/gtB2 seugnot gtB2 .gergga gtB2 1 011–58 0 4 01 12 31 9 11 5 72 ipg LCS gtB2 09–08 2pA 53–62 5 3 01 22 23 11 6 21 1 3 gp SFL pAEA 62–0 2 53–62 2 3 2 41 01 14 14 23 63 3 3 1 1 2 4 2 2 2 1 lp lp SM SM pA 83–0 1 1 7 72 44 7 3 6 2 3 sp SF pA 62–0 2 3 11 32 23 21 6 9 1 3 gp SFL E 85–53 3 2 01 14 43 7 2 2 0 2 lp SM E 42–21 A 6–0 E 05–83 3 1 8 03 24 9 1 4 2 3 sp SF E 25–53 2 3 01 12 23 51 5 6 4 4 gp SFL elbaratsop–tserof( ecisurP–4eliforP )lioselbara( )lioselbara( )liostserof( –3eliforP –2eliforP –1eliforP ecyzso³iM onwobarG 1. Particle-size distribution of the soils under study awaleiB eliforP lioS )lios TABLE Explanation: gi – clay loam, gl sandy loam (finer), gp gpi sandy-clay gz pg loamy sand, pl sand (coarser), ps (finer); CL FS fine FSL fine-sandy loam, LFS – loamy fine sand, SCL sandy clay L loam; aggreg. structural aggregates, tongues albeluvic tongues. Lithological discontinuity in Glossic Planosols (Albeluvisols) of Lower Silesia (SW Poland) 183

TABLE 2. Percentage of sand sub-fractions in the soils under study

eliforP lioS )mmniretemaid(noitcarf-busdnasfoegatnecreP ssalC noziroH htpeD mc 0.1–0.2 5.0–0.1 52.0–5.0 1.0–52.0 50.0–1.0 –1eliforP pA 62–0 4 41 82 04 41 f ecyzso³iM 2pA 53–62 4 31 82 14 41 f E 25–53 4 21 62 04 81 f gtB/E2 08–25 2 5 81 84 72 f seugnot 1 4 42 75 41 f E/gtB2 seugnot 0 2 13 06 7 f 001–08 2 4 02 55 91 f 031–001 2 3 31 75 52 f –2eliforP pA 83–0 1 8 13 15 9 f awaleiB E 05–83 1 9 33 74 01 f gtB/E2 08–05 2 7 02 74 42 f .gergga 0 2 01 36 52 f seugnot 1 8 32 54 32 f gtB2 09–08 2 9 02 44 52 f 501–001 2 51 52 24 61 f 521–021 2 9 12 94 91 f 541–041 2 9 91 15 91 f –3eliforP A 6–0 5 01 52 04 02 f onwobarG 21–6 5 21 03 34 01 f E 42–21 6 11 82 64 9 f 04–42 5 11 72 64 11 f gtB/E2 26–04 2 8 02 05 02 f seugnot 3 6 91 05 22 f E/gtB2 .gergga 2 8 91 54 62 f 58–26 3 9 42 74 71 f gtB2 011–58 0 8 12 44 72 f –4eliforP pA 62–0 3 51 44 43 4 m ecisurP EA 53–62 2 11 54 93 3 m E 85–53 2 11 44 63 7 m xgtB/E2 36–85 2 11 43 93 41 f gtB/E2 57–36 0 9 03 34 81 f seugnot 1 6 72 15 51 f gtB2 .gergga 0 6 12 24 13 f 511–57 0 3 21 25 33 f Explanation: f – fine, m – medium; aggreg. – structural aggregates, tongues – albeluvic tongues. tological indexes according to Folk and Ward (1957) Directly below the humus horizon, the layer is preserved were calculated, both in original linear scale (in µm), that meets the requirements for an eluvial horizon, and after conversion to the phi scale, using the extending down to the depth of 40–58 cm (Table 1), formula ϕ = – log2d, where d is the particle diameter with oximorphic mottles or iron-manganese concen- in mm (Krumbein 1964). trations in its bottom part. Horizons A and E have a sandy texture, with similar distribution of particular RESULTS sand fractions in A and E horizons. The contact of eluvial and illuvial horizons is clearly marked in all Basic morphological properties profiles; “clear” or “abrupt” in terms of morphological terminology, even if its continuity is broken by inter- The soils under investigation are clearly vertically fingering of eluvial material into an illuvial one. Also, differentiated in terms of their morphology and the abrupt contact between eluvial and illuvial texture (Table 1). The humus horizons have a thickness (genetic) horizons is an abrupt transition between sandy- from 12 cm (forest soils) up to 38 cm (arable soils). and loamy-textured layers. Moreover, the disconti- 184 EL¯BIETA MUSZTYFAGA, CEZARY KABA£A nuous line of cobbles and coarse gravels, a residuum is higher than in the surrounding 2E/Btg horizon, and, of former “moraine pavement” occur at the contact in particular, than in 2Btg (Table 3). Horizons A+E of underlying loam and overlying sand. At least some and 2Btg differ in degree of sorting ratio (index W of the stones are ventifacts, i.e. have a double-sided and Wϕ). According to the sedimentological termi- polished upper part, clear effect of eolian process nology, the grains in the A+E horizons are poorly sor- under harsh periglacial conditions. Loamy 2E/Btg, ted (Wϕ = 2.0), and in the underlying loam are very 2Btg/E, and 2Btg horizons meet criteria for argic dia- poorly and extremely poorly sorted (2Btg horizons: gnostic horizon, because of abundant clay cutans pre- Wϕ about 3.7). The other confirmation of different sent on the aggregate surfaces and in the larger pores sorting degree is the kurtosis (indexes Sp and Spϕ), in the loamy part of horizons (clay cutans or bridges which is leptokurtic (1.6–2.0) in topsoil and platy- are absent in albic material of the tongues). Also, at kurtic (range 0.6–0.8) in 2Bt horizons. The diversity least some subhorizons of the loamy subsoil fulfil of kurtosis values is a result of unimodal particle-size criteria of the fragic horizon, due to high density and distribution in A+E horizons (due to absolute dominance massive structure (PSC 2011). Moreover, glossic ho- of sand fraction) and bimodal distribution in 2Bt rizon (2E/Btg) was recognized in the upper part of horizons (a relatively high content of sand and clay loamy layer in all profiles under investigation. Glossic fractions, at low content of silt, Table 1). The skewness horizon is featured by numerous tongues similar in is positively skewed (Skϕ = 0.3) in A+E horizons, colour to the eluvial horizon (E) and coarser in texture and strongly positively skewed (Skϕ = 0.4–0.5) in as compared to surrounding loamy Bt horizon. The 2E/Btg, albeluvic tongues, and 2Btg horizons (Table 3). boundaries between 2E/Btg, 2Btg/E, and 2Btg are Positive skewness indicates importance of the grains unclear and contractual, as the density of tongues finer than average diameter. penetrating into the Bt horizon changes gradually and Significant differences in the average diameter of irregularly down to the depth of more than 100–120 cm. grains, and in sorting ratios are interpreted by sedi- Both the glossic and argic/fragic horizons have strong mentologists as sufficient indicators of different stagnic properties, with redox mottles covering up to sedimentation environments and different kind of 100% of the exposed soil matrix (as the sum of sediments (Racinowski et al. 2001). However, in reductimorphic and oximorphic colours). soils impacted by lessivage, that interpretation cannot be applied directly, due to the pedogenic differentiation Sedimentological features of soil material driven by clay translocation. Nevertheless, huge differences between the indicators’ values (Table 3) The upper horizons (A + E) are featured by a much in the topsoil and subsoil cannot arise only from the larger average diameters of grains (mean M range lessivage process, but at least in part are resulting 142–171 µm, geometric mean dg range 99–121 µm), from the primary lithological discontinuity between compared to the subsoil horizons (especially 2Bt), soil layers under comparison (Schülli-Maurer et al. where the values of M and dg greatly decrease to about 2007, Jaworska et al. 2014). 22 µm. Average grain diameter in albeluvic tongues

TABLE 3. Sedimentological indices according to Folk and Ward (1957) for the unified horizons of the soils under study

lioS M W kS pS ϕΜ Wϕ kS ϕ pS ϕ gd noziroh )mµ( (µ )m A *241 2.4 3.0- 6.1 0.3 0.2 3.0 6.1 99 **162-05 5.6–9.2 )2.0-(–3.0- 8.1–3.1 3.4–9.1 7.2–5.1 3.0–2.0 8.1–3.1 571–14 E 171 8.3 3.0- 7.1 7.2 9.1 3.0 7.1 121 142–5.45 6.6–4.2 )3.0-(–4.0- 8.1–2.1 2.4–1.2 7.2–2.1 4.0–3.0 8.1–2.1 971–54 gtB/E2 6.14 6.01 5.0- 1.1 7.4 4.3 5.0 1.1 24 3.46–5.32 5.21–6.8 )3.0-(–5.0- 8.1–7.0 4.5–0.4 6.3–1.3 5.0–3.0 8.1–7.0 56–52 seugnoT 2.48 6.5 4.0- 0.2 7.3 3.2 4.0 0.2 66 641–6.83 0.11–2.2 1.0-6.0- 3.2–7.1 7.4–8.2 5.3–1.1 6.0–1.0 3.2–7.1 59–14 gtB2 4.22 8.21 4.0- 7.0 5.5 7.3 4.0 7.0 22 2.62–5.71 6.41–0.01 )4.0-(–5.0- 8.0–6.0 8.5–3.5 9.3–3.3 5.0–4.0 8.0–6.0 62–91

Explanation: *mean; **range (minimum–maximum); M – mean grain size; W – standard deviation; Sk – skewness; Sp – graphic kurtosis; dg – geometric mean grain size. Lithological discontinuity in Glossic Planosols (Albeluvisols) of Lower Silesia (SW Poland) 185

Particle-size distribution and texture classes gradient of clay content in the illuvial horizon. The expected decrease of clay content with depth is clearly The A+E horizons have a texture of sand and visible in the profile Bielawa (featured by low intensity loamy sand, at variable content of silt fraction of albeluvic tonguing) and invisible in the Prusice (5–20%), and low content of clay fraction, below 4% profile (at high intensity of tonguing in 2E/Btg, 2Btg, (Fig. 2). Sub-fraction of fine sand (32–45%) followed and 2Btg horizons), where it even looks like a clay by medium sand (21–30%) dominate among sand increase downward the soil profile (Table 1). fractions in these horizons (Table 2). The order of sand sub-fractions is different in the profile Prusice Relative granulometric indexes only, where medium sand prevails above the fine sand (Table 2). The illuvial horizons (2Btg) most frequently The relative granulometric indexes used for evaluation have a texture of sandy clay loam (Fig. 2) in bulk of the lithological discontinuity are based on the (mixed) samples, whereas the texture of aggregates proportion of sand and silt (sub-)fractions, which are collected separately from the tongues is always finer considered not vulnerable to eluvial/illuvial processes and qualifies to clay loam class (Table 1, Prusice pro- (Kowalkowski and Prusinkiewicz 1963). The granu- file). In the illuvial horizons (2Btg) in all of the soils lometric indexes calculated in this study have very under investigation (including the profile Prusice), different values in particular soil horizons (Table 4). the fine sand predominates (up to 38%), followed by Quantitative proportions of fine sand to medium sand medium sand (22%). The albeluvic tongues have (index A), fine sand plus very fine sand to medium a texture of sand to sandy loam (Fig. 2), but generally, sand (B), and fine sand plus coarse silt to coarse sand the texture class is more similar to this in topsoil rather plus medium sand (D) were at least two times lower than that in 2Btg horizon (Fig. 3). Surprisingly, the in topsoil A+E horizons (A: 1.3–1.4; B: 1.7–1.8; D: texture of tongues is sometimes coarser than in the 1.3–1.5) than in 2Btg horizons (A: 2.6; B: 3.9; D: eluvial horizon (profile Mi³oszyce, tongues in 2Btg/E 3.8). The ratio of fine sand to coarse sand (index C) horizon). It must be clearly stated, that the particle- showed similar values throughout soil profiles (C: size distribution reported for 2Btg and in particular 2.6–3.2), and only in albeluvic tongues the index value for 2E/Btg horizons is an average for loamy soil matrix was 6.3 that is two times higher than in surrounding (aggregates) and albeluvic tongues. If the density 2E/Btg and 2Btg horizons. Also the values of granu- (abundance) of tongues is higher, the averaged particle- lometric indexes recommended by the WRB classifi- size distribution of glossic horizon is more closely cation (IUSS Working Group WRB 2015) differ related to eluvial than to illuvial horizon (Fig. 3 ACD). significantly between A+E and 2Btg horizons (Table Another consequence of albeluvic tonguing in 4), in particular with F index (the proportion of very 2Btg horizon is the difficulty in describing the fine sand to fine sand).

FIGURE 2. Graphical display of the texture of soil horizons under study 186 EL¯BIETA MUSZTYFAGA, CEZARY KABA£A 3. Cumulative texture curves for E and 2Btg horizons albeluvic tongues in glossic horizon FIGURE Lithological discontinuity in Glossic Planosols (Albeluvisols) of Lower Silesia (SW Poland) 187

DISCUSSION highlighting i.a. domination of the same fine sand sub-fraction throughout the soil profile. However, the The data presented in this paper confirm that the other facts argue for lithological discontinuity as the textural differentiations in the profiles of soils deve- primary cause of textural differentiation. loped from glacial materials in the north-eastern part The first argument for the lithological discontinuity of Lower Silesia meet the criteria for lithological is an unbalanced content of silt and clay fractions in discontinuity. The horizons A+E (in other profiles, the “eluvial” and “illuvial” horizons. The balance was not included in this paper, also ABv and AE horizons) calculated based on the content of clay in the “parent have a texture of sand with minimum clay content, material”, i.e. in the loam of the bottom profile whereas 2Bt horizons (2E/Bt and 2Bt/E) have a texture (occurring below the depth of 100 cm). If we assume of loam, most frequently sandy clay loam. The albeluvic that the entire profile had initially a texture of the tongues in glossic 2E/Bt horizons contain much coarser loam in the parent material, we can calculate the material than the surrounding loamy aggregates. stocks of illuvial clay in Bt horizons and stocks of Textural differentiations influence the physical and clay “removed” from (or lacking in) topsoil horizons water properties, as well as the agricultural value of (taking into account the current clay content, thickness the soils. The thicker cover sand layer, the larger are of horizons, and soil bulk density in these horizons). negative consequences for water storage potential and In most cases, the hypothetically eluviated amount soil fertility (Marcinek and Komisarek 2004, Glina of clay is up to two times higher than the stocks of et al. 2013). According to the Polish Soil Classification illuvial clay in Bt horizons. Selective erosion of clay (2011) most of profiles meet the criteria for lessive fraction (removal out of the soil profile) is theoretically soils with glossic horizon and thick sand layer in topsoil possible (Kühn et al. 2006), but it may occur in cultivated (gleby p³owe zaciekowe spiaszczone). FAO-WRB has topsoil only, and the selective clay erosion from the formerly classified these soils as Albeluvisols (IUSS layer of 50 cm thick seems impossible, especially in Working Group WRB 2006), but presently the soils the plain area. Even more difficult to explain is the belong to Glossic Planosols (IUSS Working Group low content of silt fraction in A+E horizons. Illuvial WRB 2015). horizons of soil under study are not enriched in silt, The origin of the textural differentiation in “po- as compared to parent material. Thus, the loss of silt dzolic” soils (until 60s of 20th century the clay illuvial fraction in A+E horizons is not reflected by its translo- soils and podzols have not been distinguished in cation to Bt horizons in course of pedogenic process. Poland) has long been disputed in Poland. Some of Such a large decrease of silt content may only result the researchers explain this as related to pedogenic from selective water or wind erosion, but, as stated processes (lessivage) only and exclude a lithological above, such a selective erosion from the layer of 50 discontinuity (Komisarek and Sza³ata 2008), cm thick is questionable. Moreover, loss of silt or clay

TABLE 4. Granulometric indices according to Kowalkowski and Prusinkiewicz (1963) and WRB (IUSS Working Group WRB, 2015) for the unified horizons of the soils under study

lioS lobmysxednI noziroH ABCDEFG snoitcarffooitaR /1.0–52.0 /50.0–52.0 /1.0–52.0 /20.0–52.0 /50.0–5.0 50.0–1.0 50.0–1.0 52.0–5.0 52.0–5.0 5.0–0.1 52.0–1 5.0–1 52.0–5.0 1.0–52.0 A *4.1 8.1 7.2 5.1 5.7 4.0 3.0 **6.1–8.0 4.2–9.0 9.3–1.2 1.2–7.0 1.11–4.5 8.0–1.0 5.0–1.0 E 3.1 7.1 2.3 3.1 1.8 3.0 2.0 7.1–8.0 2.2–0.1 1.4–1.2 7.1–8.0 1.01–8.6 7.0–1.0 50–1.0 gtB/E2 9.1 7.2 0.3 4.2 7.01 8.0 4.0 5.2–1.1 5.3–5.1 5.3–6.2 0.3–5.1 5.31–0.8 2.1–4.0 5.0–4.0 seugnot 2.2 9.2 3.6 5.2 6.22 7.0 3.0 7.2–9.1 9.3–1.2 5.41–8.2 2.3–1.2 5.54–2.11 2.1–2.0 5.0–1.0 gtB2 6.2 9.3 6.2 8.3 4.41 3.1 5.0 4-4–7.1 2.7–4.2 0.5–6.1 8.8–0.2 0.14–5.5 8.2–7.0 60–4.0

Explanation: *mean; **range (minimum–maximum). 188 EL¯BIETA MUSZTYFAGA, CEZARY KABA£A fraction resulting from the surface water or wind erosion Granulometric indexes are also useful in an is not a pedogenic, but a lithogenic process (Myciel- explaining of the origin of albeluvic tongues in Glossic ska-Dowgia³³o 1980, Manikowska 1997, Jaworska et Planosols under study. Most of the indexes in tongues al. 2014). significantly differ from their values for Bt horizons The second argument for the lithological discon- (especially B, C, E, F indexes; Table 4). This means tinuity are significant differences and changes in that the clay eluviation has not been the main process relative values of the granulometric indexes. Although in the formation of tongues, because it would not change the fine sand fraction dominates throughout the profiles the proportions between the stable sand factions. At in the most of soils under investigation, the propor- least in part, the tongues were formed by filling the tions of this fraction to other “stable” sand fractions thin cracks with sandy material from the overlying (as medium and coarse sand fractions) are different layer. The complete explanation of the tongues in “eluvial” and “illuvial“ horizons (Table 4; indexes formation is still impossible based on the present data, A, B, D, E, F), whereas the ratios of particular but the specific texture of the tongue in 2Btg/E horizon sub-fractions of quartzitic sand cannot differentiate of Mi³oszyce profile (Table 2) might indicate that in course of lessivage (Schülli-Maurer et al. 2007, some cracks were open on the soil surface under Van Ranst et al. 2011). FAO-WRB classification periglacial conditions that allowed their filling with (IUSS Working Group WRB 2015) requires at least eolian sand, much better segregated than the latter 5% of absolute and 25% of relative difference in com- cover sand (different contents and ratios of almost all pared fractions as the criterion for lithological discon- particle-size fractions). A similar phenomenon, but tinuity. The differences found in soils under investi- on a much larger scale, has been described by Dzier- gation are much larger: the absolute differences are ¿ek and Stañczuk (2006). two-three times higher than the required minimum, It was noticed during the fieldwork that the texture and the relative differences often exceed 100%. The of albeluvic tongues is differentiated in the cross-section, lower values of the granulometric indexes in the sandy which impeded soil sampling for laboratory analysis. topsoil indicate the relatively coarser sand fraction in The innermost part of the tongues is filled with sandy topsoil as compared to loamy subsoil. This difference material, whereas the outer part at the contact with can only be explained by different sedimentological the soil aggregates is in fact a bleached hypocoating. conditions or different source material for the topsoil It seems that the “true” sand tongues have much lesser and subsoil layers (Mycielska-Dowgia³³o 1980). thickness than it is considered based on colour diffe- The third argument for the lithological discontinuity rentiation of the soil mass. The seasonal inflow and in the analyzed profiles, crucial for researchers who stagnation of (surface) water in tongue creates reducing study the Pleistocene sediments and landforms, is the conditions and allows migration of reduced iron, and presence of eolized pavement at the contact of sand the development of bleached (reduced) hypocoatings and till layers. On the one hand, the pavement testifies on the surface of soil aggregates adjacent to the tongue for the strong erosion of the former topsoil layer (Lindbo et al. 2000). Thus, the present-day redox (former loamy eluvial horizon?) that led to accumu- phenomena may cause continuous morphological thic- lation of the most coarse fragment on the soil surface. kening and vertical extending of the albeluvic tongues On the other hand, the polished surfaces of the pavement (Szymañski et al. 2011). Also, the clay eluviation or cobbles testify for a long-term existence of the stone decay cannot be excluded in these reduced soil zones layer at land surface, because only the fully exposed (Kühn et al. 2006). stones and gravels could be specifically (two-sided) polished by wind. Therefore, the cover sand was CONCLUSIONS deposited after a certain period of time after the pavement formation and wind polishing. The other 1. Both the sedimentological and granulometric stones and gavels spread throughout the till (below indexes testify for the textural difference between the pavement) do not have remarks of wind erosion. the sandy “eluvial” horizons (sand and loamy sand It must be stated that the single polished stones (ven- classes) and loamy “illuvial” horizons (sandy clay tifacts) are spread above the pavement line, in the loam class) of the Glossic Planosols in Lower overlying sand layer or even on the soil surface, trans- Silesia does not originate from pedogenic processes, ported there by upfreezing (GoŸdzik and French but is a kind of primary lithological discontinuity. 2004). This observation explains why a pavement 2. The layer of eolized pavement (consisting of polished layer at the contact of a till and cover sand is not gravels and cobbles – ventifacts) on the contact of continuous, or even poorly visible in some profiles. till and overlying sand indicates, that the cover sand Lithological discontinuity in Glossic Planosols (Albeluvisols) of Lower Silesia (SW Poland) 189

was settled on previously eroded loamy soil, for Kaba³a C. (ed.)., 2015. Soils of Lower Silesia: origins, diversity, a certain period of time exposed at land surface and protection. PTG, PTSH. Wroc³aw: 256 pp. for a wind erosion under periglacial conditions of Kacprzak A., Derkowski A., 2007. Cambisols developed from the arctic desert. cover-beds in the Pieniny Mts (southern Poland) and their mineral composition. Catena 71(2): 292–297. 3. The albeluvic tongues in Bt horizons were not formed Komisarek J., Sza³ata S., 2008 Textural differentiation in pedons exclusively by clay eluviation from the loamy soil, of Albeluvisols in the Wielkopolska Region. Nauka Przyroda but at least in part by filling the thin cracks with Technologie, Melioracje i In¿ynieria Œrodowiska 2: 2–10 (In sandy material. Presently, the thickness and depth Polish). of albeluvic tongues may grow due to water Kondracki J., 2001. Geografia regionalna Polski. Wydawnictwo stagnation and redox phenomena. Naukowe PWN, Warszawa (In Polish). 4. Both the lithological discontinuity and unbalanced Konecka-Betley K., 1961. Studies of the sorption complex of soils from boulder loams in relation to their genesis. Soil Scien- clay (and silt) content (in “eluvial” and “illuvial” ce Annual 10(2): 469–524 (In Polish). horizons) indicate a multi-step polygenetic origin Konecka-Betley K., 1979. Reliktowe procesy glebotwórcze w of the Glossic Planosols in SW Poland which glebach wspó³czesnych wytworzonych z gliny zwa³owej. requires a further explanation. Zeszyty Naukowe SGGW-AR w Warszawie, Rolnictwo 18: 77–95 (In Polish). ACKNOWLEDGMENT Kowalkowski A., Borzyszkowski J., 1977. The role of periglacial and extraperiglacial perstruction in the formation of the soil The study was financed by the National Science profile in Central Europe. Folia Quaternaria 49: 25–37. Kowalkowski A., Prusinkiewicz Z., 1963. Granulometric numeral Centre of Poland (research grant 2012/05/B/NZ9/ indieces as indicators of uniformity in Pleistocene sedimental 03389). strata. Soil Science Annual 13: 159–162 (In Polish). Krumbein W.C., 1964. Some remarks on the phi notation. Journal REFERENCES of Sendimentary Petrology 34: 195–196. , Kühn P., 2003. Micromorphology and Late Glacial/Holocene Chlebowski R., Lindner L., 1991. Zród³a materia³u i warunki genesis of Luvisols in Mecklenburg-Vorpommern (NE-Ger- akumulacji lessów m³odszych Wy¿yny Ma³opolskiej. Biule- many). Catena 54: 537–555. tyn Geologiczny. WG UW, 32: 15–50 (In Polish). Kühn P., Billwitz K., Bauriegel A., Kühn D., Eckelmann W., 2006. Dobrzañski B., Konecka-Betley K., Czêpiñska-Kamiñska D., Distribution and genesis of Fahlerden (Albeluvisols) in 1977. Procesy kszta³towania siê gleb wytworzonych z glin Germany. Journal of Plant Nutrition and Soil Science 169(3): zwa³owych Wysoczyzny Siedleckiej. Zeszyty Naukowe 420–433. SGGW-AR w Warszawie, Rolnictwo 16: 9–24 (In Polish). Lindbo D.L., Rhoton F.E., Hudnall W.H., Smeck N.E., Bigham Dzier¿ek J., Stañczuk D., 2006. Record and palaeogeographical J.M., Tyler D.D., 2000. Fragipan degradation and nodule implications of Pleistocene periglacial processes in the Dro- formation in Glossic Fragiudalfs of the Lower Mississippi hiczyn Plateau, Podlasie Lowland (Eastern Poland). Geolo- River Valley. Soil Science Society of America Journal 64(5): gical Quarterly 50(2): 219–228. 1713–1722. Folk R.L., Ward W., 1957. Brazos River Bar: A study in the £abaz B., Bogacz A., Kaba³a C., 2014. Anthropogenic transfor- significance of grain size parameters. Journal of Sedimentary mation of soils in the Barycz valley-conclusions for soil Petrology 27: 3–26. classification. Soil Science Annual 65(3): 103–112. Glina B., Jezierski P., Kaba³a C., 2013. Physical and water Manikowska B., 1997. Periglacial cover sediments and soil properties of Albeluvisols in the Silesian Lowland (SW Po- profile evolution on the fluvioglacial interfluve area of Cen- land). Soil Science Annual 64(4): 123–129. tral Poland. Soil Science Annual, 48(3/4): 151–167 (In Polish). GoŸdzik J., 1973. Geneza i pozycja stratygraficzna struktur pery- Marcinek J., Komisarek J., 2004. Antropogeniczne przekszta³ce- glacjalnych w œrodkowej Polsce. Acta Geographica Lodzie- nia gleb Pojezierza Poznañskiego na skutek intensywnego nisia 30: 119 pp. (In Polish). u¿ytkowania rolniczego. Wydawnictwo AR, Poznañ, 118 pp. GoŸdzik J.S., French H.M., 2004. Apparent upfreezing of stones (In Polish). in late-Pleistocene coversand, Be³chatów vicinity, Central Mycielska-Dowgia³³o E., 1980. Wstêp do sedymentologii. WSP, Poland. Permafrost and Periglacial Processes 15(4): 359–366. Kielce, 178 pp. (In Polish). IUSS Working Group WRB, 2006. World Reference Base for Polish Soil Classification, 2011. Soil Science Annual 62(3): Soil Resources. World Soil Resources Reports 103. FAO, 1–193 (In Polish). Rome: 128 pp. PTG, 2009. Particle size distribution and textural classes of soils IUSS Working Group WRB, 2015. World Reference Base for and mineral materials – classification of Polish Society of Soil Soil Resources 2014 – an international system for soil classi- Sciences 2008. Soil Science Annual 60(2): 6–15 (In Polish). fication, first update 2015. World Soil Resources Reports 106. Racinowski R., Szczypek T., Wach J., 2001. Prezentacja i inter- FAO, Rome: 181 pp. pretacja wyników badañ uziarnienia osadów czwartorzêdo- Jaworska H., D¹bkowska-Naskrêt H., Kobierski M., 2014. The wych. Wydawnictwo UŒ, Katowice, 146 pp. (In Polish). influence of litho- and pedogenic processes on Luvisols Schoeneberger P.J., Wysocki D.A., Benham E.C., 2012. Field formation of selected area of Vistula Glaciation. Geological book for describing and sampling soils, Version 3.0. Soil Quarterly 58(4): 685–694. Survey Staff. National Soil Survey Center, Lincoln, NE: 266 pp. 190 EL¯BIETA MUSZTYFAGA, CEZARY KABA£A

Schülli-Maurer I., Sauer D., Stahr K., Sperstad R., Sorensen R., Waroszewski J., Kaliñski K., Malkiewicz M., Mazurek R., 2007. Soil formation in marine sediments and beach deposits Koz³owski G., Kaba³a C., 2013a. Pleistocene-Holocene cover-beds of southern Norway: investigations of soil chronosequences on granite regolith as parent material for Podzols – An example in the Oslofjord region. Revista mexicana de ciencias geoló- from the Sudeten Mountains. Catena 104: 161–173. gicas 24(2): 237–246. Waroszewski J., Kaba³a C., Koszelnik K., 2013b. Litological Sza³ata S., Komisarek J., 2014. Morphological diversity of Arenic discontinuities in Podzols developed from upper Cretaceous Albeluvisols of the Central Wielkopolska Region. Nauka, sandstones in the Sto³owe Mountains. Prace Geograficzne 135: Przyroda, Technologie 8(4), 55 (In Polish). 87–100 (In Polish). Szymañski W., Skiba M., Skiba S., 2011. Fragipan horizon Zagórski Z., 1995. Micromorphological features of litho- and degradation and bleached tongues formation in Albeluvisols pedogenic processes in nonuniform soils developed from glacial of the Carpathian Foothills, Poland. Geoderma 167: 340–350. deposits. Soil Science Annual 46(3/4): 71–93 (In Polish). Œwitoniak M., 2008. Classification of young glacial soils with Zagórski Z., 1996. Granulometric indices of litho- and pedogenic vertical texture-contrast using WRB system. Agrochimija processes in non-uniform soils developed from glacial deposits. i Gruntoznawstwo 69: 96–01. Soil Science Annual 47(supl.): 125–235 (In Polish). Van Ranst E., Dumon M.,. Tolossa A.R, Cornelis J.-T., Stoops Zagórski Z., 2001 Iron forms as indicators of pedo-and lithogenetic G., Vandenberghe R.E., Deckers J., 2011. Revisiting ferrolysis processes in non-uniform soils. Soil Science Annual 52 (supl.): processes in the formation of Planosols for rationalizing the 87–96 (In Polish). soils with stagnic properties in WRB. Geoderma 163: 265– 274. Received: February 9, 2016 Accepted: March 4, 2016

Uziarnienie gleb p³owych zaciekowych spiaszczonych (Albeluvisols, Glossic Planosols) na Dolnym Œl¹sku

Streszczenie: Badaniami objêto gleby p³owe zaciekowe spiaszczone (opadowo-glejowe) pokrywaj¹ce znaczne obszary pó³noc- no-wschodniej czêœci Dolnego Œl¹ska, w zasiêgu wystêpowania glin zlodowacenia Odry i Warty. Celem pracy by³a charakterystyka uziarnienia gleb w kontekœcie genezy materia³ów macierzystych tych gleb oraz wspó³czesnych procesów glebotwórczych. WskaŸni- ki sedymentologiczne i granulometryczne, niezbilansowana zawartoœæ frakcji ilastej (i py³owej), a tak¿e obecnoœæ bruku morenowe- go na kontakcie piaszczystych poziomów powierzchniowych oraz gliniastych poziomów podpowierzchniowych wskazuj¹, ¿e zró¿- nicowanie uziarnienia tych poziomów nie jest efektem procesów pedogenicznych (w szczególnoœci „spiaszczenia” gliny moreno- wej), ale przede wszystkim wynika z pierwotnej nieci¹g³oœci litologicznej materia³u macierzystego tych gleb. Uziarnienie i wskaŸni- ki granulometryczne w zaciekach eluwialnych w poziomie glossic wskazuj¹, ¿e zacieki nie powsta³y wy³¹cznie przez wymycie drobnych frakcji z materia³u gliniastego, ale w pierwszej kolejnoœci przez wype³nienie pierwotnych szczelin materia³em piaszczy- stym. Zacieki eluwialne o grubszym uziarnieniu ni¿ matrix poziomu iluwialnego umo¿liwiaj¹ g³êbokie wnikanie i stagnowanie wody, a wytwarzaj¹ce siê warunki redukcyjne sprzyjaj¹ poszerzaniu i wyd³u¿aniu siê zacieków eluwialnych.

S³owa kluczowe: gleby p³owe zaciekowe, zró¿nicowanie uziarnienia, nieci¹g³oœæ litologiczna