Physical and water properties of Albeluvisols in the Silesian Lowland 123 SCIENCE ANNUAL DOI: 10.2478/ssa-2013-0019 Vol. 64 No. 4/2013: 123–129

BART£OMIEJ GLINA*, PAWE£ JEZIERSKI, CEZARY KABA£A

Wroc³aw University of Environmental and Life Sciences, Institute of Soil Science and Environmental Protection ul. Grunwaldzka 53, 50-357 Wroc³aw

Physical and water properties of Albeluvisols in the Silesian Lowland (SW Poland)

Abstract: Soil texture, bulk and specific density, total porosity, and the water capacity at pF 0–2.7 were measured in Albeluvisols with more or less pronounced lithological discontinuity. The soil pits were located in the north-eastern part of the Silesian Lowland, on the glacial built of till blanketed with cover materials of various origin, mainly . Distinct albeluvic tongues with sandy texture and strong stagnic color mosaic at the contact of eluvial and illuvial horizons were identified in all profiles under study. The lowest bulk density was measured in the plough layers, while the highest in EBw horizons or glossic E/Bt horizons. Total porosity was the largest in plough layers, rapidly decreased in subsoil E horizons and then back increased with depth. Water capacity (at each measured pF value) was strongly correlated mainly with content and rapidly raised in E/Bt horizons. The highest field water capacity was measured in E/B horizons at low albeluvic tonguing intensity, or in deeper parts of Bt horizon at larger intensity of albeluvic tonguing into the illuvial horizon. The easily available water stock in the upper 100 cm-thick column of Albeluvisols with lithological discontinuity depends mainly on the depth of transition of eluvial (coarser) and illuvial (finer-textured) zones, similarly to typical Luvisols with the same type of textural (lithological) variability in the soil profile.

Key words: Albeluvisols, water properties, soil texture, lithological discontinuity

INTRODUCTION

Albeluvisols cover over 3.2 mln km2 of the Earth and glacial sands (Buczko et al., 2002; Jaworska and surface, mainly in the north-eastern , northern D¹bkowska-Naskrêt, 1999; Komisarek and Sza³ata, and central Asia, and South America (Bockheim and 2008; Sauer et al., 2009).Specific case of Luvisols Gennadiev, 2000). The origin of these is mainly and Albeluvisols are soils with a lithological discon- related to lessivage process that means a substantial tinuity, where the surface humus and eluvial horizons vertical transfer of clay particles from the near-surfa- are developed from the younger “cover materials” ce to the deeper layers (De Jonge et al., 2004), that (mainly the glacio-fluvial or eolian sands), and the differentiates the soil profile into a clay-depleted elu- deeper horizons, including illuvial Bt horizon – from vial horizon and clay-enriched argic horizon, where the till of the older glaciation. The textural change in the clay illuviation is identified by the presence of these soils is accompanied by the clear differentia- clay skins and coatings visible both in the macrosco- tion of bulk density and other physical soil properties pic and microscopic scales (Konecka-Betley and Za- (Porêbska et al., 2010; Zaleski, 2012), which affects górski, 1994). The distinguishing between Albeluvi- the soil water properties (Bogacz et al., 2008). Water sols and Luvisols based on the occurrence of albelu- retention and amounts of plant-available water are vic tonguing in the upper part of argic horizon (Ko- among the most important parameters describing the misja V Genezy, Klasyfikacji i Kartografii Gleb PTG, functional and ecological soil properties (Dexter, 2011; IUSS Working Group WRB, 2007). Tongues 1997). Physical and water properties of the Luvisols, formation is related to the periglacial climate and ice including the water retention, is well recognized and wedges (Konecka-Betley and Zagórski, 1994; Szy- described in the professional literature (Kaczmarek, mañski et al., 2011; Szymañski and Skiba, 2012) or 2001; Kaczmarek et al., 2006; Kobierski and D¹b- to the ferrolysis process (Van Ranst and De Coninck, kowska-Naskrêt, 2002; Marcinek and Komisarek, 2002). Luvisols and Albeluvisols are developed from 2004; Paluszek, 2011; Walczak et al., 2002a). Howe- a various parent materials, including and other ver, much less available (Komisarek and Sza³ata, (Turski and Witkowska-Walczak, 2004; Szymañ- 2008) is information about the possible differences ski et al., 2011; Szymañski et al., 2012), glacial tills, in physical and water properties between “typical”

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Luvisols and Albeluvisols, recently introduced to the termined for pF range between 0 and 2.7, using a Polish (Komisja V Genezy, Kla- block (pF 0–2.0) and the kaolin-sand block syfikacji i Kartografii Gleb PTG, 2011) at the “type” (pF 2.2–2.7). Based on the these results, the stock of plant- level. available water at pF 2.2 in the upper 100 cm-thick soil

The aim of work was to determine selected, basic layer was calculated using the formula: z = (g1×w1)/ physical and water properties of Albeluvisols deve- 100 + ... + (gn×wn)/100, where: z – water stock, g – thick- loped from sandy and loamy materials with more or ness of (mm), w – soil moisture (% v/v) at less pronounced lithological discontinuity, that are pF 2.2. widespread in the north-eastern part of the Silesian In tables, only the mean values are displayed. Due Lowland. To the preliminary comparison, two pairs to low number of cases (only four profiles) no specific of the most typical Albeluvisols (four profiles) were statistical analysis was done, only the Pearson correla- selected. tion coefficients (at p<0.05) were calculated for the entire set of samples (using Statistica 10 package). MATERIAL AND METHODS

The Oleœnicka Plain, situated in the north-eastern RESULTS AND DISCUSSION part of Silesian Lowland, is a gently undulated gla- cial plain, built of the ground moraine tills of Riss The Albeluvisols under investigation had a typi- Glacial Stage (Odra Glaciation in Polish terminolo- cal arrangement of genetic soil horizons A-Et-E/B- gy) blanketed with a thin layer of cover sands of va- Bt-BC. In the soils Paw³owice 1 and 2, eluvial E ho- rious origin (fluvial, colluvial, eolian, etc.) and age. rizons were poorly preserved due to erosion, deep Therefore, the various types of lithological disconti- plowing and the development of secondary cambic nuity are common within the profiles of prevailing horizon. According to the Polish Soil Classification Luvisols and Albeluvisols. Mean annual air tempera- (Komisja V Genezy, Klasyfikacji i Kartografii Gleb ture of the area is 9.5oC, and the mean annual preci- PTG, 2011) all described soils were classified as so- pitation is between 500 and 620 mm. The plain is ils lessives with glossic horizon and stagnic proper- located in the transitional zone between areas of po- ties (gleby p³owe zaciekowe opadowo-glejowe), due sitive and negative climatic water balance (Dubicki to irregular albeluvic tongues penetrating into the Bt et al., 2002). Soil pits were situated on the arable fields horizon and strong redoximorphic features in the up- in the north-eastern peripheries of Wroc³aw, in the per part of the profile. The profiles differ in the de- Paw³owice district (profiles 1 and 2) and Psie Pole gree of penetration of the eluvial (albic) material into district (profiles 3 and 4). the illuvial horizon that, both on the vertical and ho- Soil morphology was described according to Gu- rizontal soil sections, may be correlated with abun- idelines (2006), and soil classification was establi- dance, width and depth of albeluvic tongues. The ton- shed according to Polish Soil Classification (Komi- guing intensity was much higher in the soils 2 and 3 sja V Genezy, Klasyfikacji i Kartografii Gleb PTG, than in the 1 and 4. The thickness of surface sandy 2011) and the FAO-WRB classification (IUSS Wor- layer in the profile Psie Pole 3 was large enough to king Group WRB, 2007). In each of the distinguished indicate it in the soil name (Komisja V Genezy, Kla- soil horizon, a set of disturbed and undisturbed soil syfikacji i Kartografii Gleb PTG, 2011) at the sub- samples was collected. type level (gleba p³owa zaciekowa spiaszczona, opa- Particle-size distribution of the £2 mm fraction dowo-glejowa). According to FAO-WRB (IUSS Wor- was conducted using sand separation on sieves and king Group WRB, 2007), all described soils were the hydrometer method for and clay fractions, after basically classified as Stagnic Cutanic Albeluvisols. sample dispersion with heksametaphosphate-bicarbo- The soils Paw³owice 1 and 2 had the texture of nate, according to standard PN-R-04032. The names sandy in and sandy-clay loam in subso- of texture classes were given according to Polish Soil il. The fine sand (0.25–0.1 mm) dominated among Science Society classification (Polskie Towarzystwo sand fractions (2–0.05 mm) throughout the profiles, Gleboznawcze, 2009). Organic carbon was determi- with the percentage share up to 30% in the upper ned by dry combustion method with absorption of horizons (Table 1). Silt (0.05–0.002 mm) content ran-

CO2 using Stroelein CS MAT 5500, and the particle ged between 16 and 26%, and was rather poorly diffe- density was determined by picnometric method. Bulk rentiated throughout the profile (Paw³owice 1), or was density and water properties were assessed in undi- significantly higher in the subsoil (Paw³owice 2). Clay sturbed soil samples collected in the stainless steel fraction (<0.002 mm) was the most clearly differen- rings (100 cm3). Water desorption curves were de- tiated in the profiles with 7–11% in the topsoil (Ap Physical and water properties of Albeluvisols in the Silesian Lowland 125

TABLE 1. Particle-size distribution in the studiem soils Soil Hhorizon DeptPercentageofparticle-sizefraction Textureclass profile [cm]>1225–15–0.01.5–0.205.25–0.02.1–0.005.05–0.002.02–0.00<0.00[PTG2008] Paw³owice1 StagnicCutanicFragicAlbeluvisol(glebap³owazaciekowaopadowo-glejowa) 1pA 0–261310203089137gp EBw26–3736101925108139gp E/Btg37–501251221961332gpi 2Btg/Eg150–7512511191451430gpi 2Btg/Eg275–9512512221081328gpi 2Btg95–12002512221171427gpi Paw³owice2 StagnicCutanicFragicAlbeluvisol(glebap³owazaciekowaopadowo-glejowa) 2pA 0–401392027127158gp EBw40–4524918258101611gl Eg/Btg45–5512613211251328gpi 2Btg/Eg55–8002715221261027gpi 2Btg80–12002415201341230gpi PsiePole3 StagnicCutanicFragicAlbeluvisol(glebap³owazaciekowaspiaszczonaopadowo-glejowa) 3pA 0–353411213314593ps Eg 35–554413243110693pg Eg/Btg55–65251829299361ps 2Btg/Eg65–1151252223158196gp 2Btg115–1504252027156817gp PsiePole4 StagnicCutanicFragicAlbeluvisol(glebap³owazaciekowaopadowo-glejowa) 4pA 0–3023819351767 5pg Eg30–4513819341658 7pg 2Btg/Eg45–701261631165618gp 2Btg70–1201262034175313gp

Explanation: ps – sand (piasek s³abogliniasty), pg – loamy sand (piasek gliniasty), gp – sandy loam (glina piaszczysta), gl – sandy loam (glina lekka), gpi – sandy clay loam (glina piaszczysto-ilasta). and E or EBw horizons) and 27–32% in the subsoil. layer and further colluvial, fluvial or eolian accumu- The abrupt change in clay content was accompanied lation of the covering materials (mainly sands). This by the occurrence of gravelly periglacial pavement kind of stratification or welding se- that argued for the lithological discontinuity between ems to be very common in Albeluvisols in the post- soil materials in the surface and subsurface horizons. glacial areas of the central and northern Europe The profiles Psie Pole 3 and 4 differ in texture that (Kühn, 2003). was sandy in topsoil (sand or loamy sand) and loamy Bulk density of the undisturbed soil samples were in (sandy loam) in the subsoil. Moreover, fine sand a wide range between 1.51 and 1.91 g cm–3 (Table 2). (0.25–0.1 mm) predominated among sand fractions Clear differences between soil horizons were obse- (up to 35%) in these soils. However, the share of me- rved in each of examined soil profiles. The lowest dium sand was similarly high (up to 29% in the pro- values (1.51–1.69 g cm–3) occurred in the surface ho- file 3). The content of silt was generally low (even rizons due to the regular tillage and correlation (Ta- less than 10%) and uniform in the profile 4, whereas ble 3) to organic matter content (Bogacz et al., 2008; clearly differentiated between E and Bt horizons in Kaczmarek et al., 2006). The highest bulk density the profile 3. The share of clay in the upper horizons values were recorded in EBw horizons (Paw³owice 1 ranged between 1 and 7%, and rapidly increased in and 2) or in E/Bt horizons (Psie Pole 3 and 4). In the the illuvial horizons, up to 18%. The lithological di- first case it may be a result of the “plow sole” formed scontinuity (Komisja V Genezy, Klasyfikacji i Kar- directly under the plough layer (Marcinek et al., 1995; tografii Gleb PTG, 2011, IUSS Working Group WRB, Zaleski, 2012). High mean bulk density of E/Bt hori- 2007) was recognized in all four profiles on the con- zons (profile 3 and 4) that was despite the presence tact between eluvial and illuvial horizons. It may re- of sandy tongues with generally lower density, indi- sult from a selective denudation of the surface till cates the high compaction and density of the loamy 126 BART£OMIEJ GLINA, PAWE£ JEZIERSKI, CEZARY KABA£A r e e y g a l a r o m t c s r 0 ) e 0 t 3 2 1 m 1 1 a 0 8 2 8 m n W i ( 3 2 2 1 2 6 8 7 8 1 7 6 1 7 7 9 9 0 4 5 9 3 4 8 ...... 1 1 1 0 4 8 2 3 0 8 9 9 8 5 6 3 3 9 1 8 2 2 3 3 2 2 2 2 2 2 1 1 1 1 1 1 1 1 1 1 9 0 0 3 5 6 1 6 8 7 3 7 7 0 1 1 5 4 9 8 ...... 2 0 3 2 1 2 0 0 5 9 3 6 1 0 2 6 7 4 4 9 27 2 2 3 3 2 2 2 2 2 2 2 2 2 2 1 1 1 1 1 4 2 4 8 8 0 0 8 4 6 0 2 1 0 6 6 4 8 2 0 ...... 6 3 6 4 9 9 4 2 9 2 2 2 9 5 4 6 3 8 9 8 25 2 2 3 3 2 2 2 2 2 3 3 2 2 2 2 1 1 1 1 1 7 6 7 9 2 0 0 3 9 8 2 7 7 7 6 0 2 5 1 1 ...... 7 4 7 5 3 2 5 4 0 3 3 3 0 0 6 6 7 4 9 9 22 2 2 3 3 3 3 2 2 3 3 3 2 3 2 2 2 1 1 1 1 8 3 0 8 7 7 1 1 3 7 2 8 9 9 0 2 7 9 5 1 ...... 0 4 9 8 8 6 9 7 7 6 7 4 6 5 3 5 2 6 2 3 . 4 3 2 3 3 3 2 2 3 3 3 3 2 2 3 3 3 2 3 3 10 ) v / v % ( 2 3 7 4 9 5 2 0 3 9 7 2 3 9 4 5 4 6 2 6 ...... F 2 0 0 0 5 0 8 0 8 7 8 7 9 7 5 7 5 9 4 5 p 4 4 4 4 00 3 3 3 3 2 3 3 3 2 2 3 3 3 2 3 3 ) c i 1 n – ) n o 0 0 0 0 0 g a a 0 0 0 0 0 0 0 0 0 0 0 b 8 0 0 0 3 8 1 1 2 g k . r . . . . . w 2 1 6 1 5 1 8 4 4 5 3 r 2 1 0 ...... a 3 . . . 4 1 1 1 1 o g j 7 7 O c ( 3 3 8 2 0 0 0 0 0 1 1 1 1 e l g - o w ) ) ) y 3 o ) t a a – i a d s l w w a m w o a 6 8 8 3 5 7 1 9 0 5 5 2 7 7 1 1 0 3 1 4 o o p r t 3 j j o 3 2 2 3 3 3 3 2 3 3 3 4 3 3 3 3 4 3 3 3 j o o o e e ...... l l m e T p l ( 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 0 g g a g - - n - o o o o z w w c w o o z o s d d ) d a a a 3 i e a l y – p p p t c p i i o o s m s t o 5 5 5 0 2 3 0 2 2 1 9 1 5 4 3 3 1 6 4 4 r c n a a a 5 6 5 6 6 6 6 6 6 6 5 6 6 6 6 6 6 6 6 6 a a e ...... g w w w P d ( 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 2 w o o o o k k k k e e e i i i e i c c c c a a a a z z z ) z 3 a a a y – t a i w w w m s k w 6 1 3 4 9 6 9 5 4 0 9 1 7 6 2 1 8 9 3 5 l c o o o n o ³ ³ ³ u 6 9 8 7 6 6 6 8 8 7 6 5 6 6 8 8 5 7 8 7 e ...... ³ g p p p B d ( 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 1 p a a a a b b b b e e e l l l e l g g g g ( ( ( ( l l l l o o o o 0 s s s s 5 i i i i 0 0 0 5 5 5 1 v v v v 5 5 5 5 0 2 7 0 5 0 5 2 2 1 6 0 5 6 1 0 u u u u t 3 l l l l 9 4 5 7 1 3 5 7 1 8 1 4 ) – – – – 2 4 3 p – e e e e – – – – – – – – – – – – 5 – – 5 5 5 – m e 0 b b b b 5 0 5 5 0 6 7 0 5 5 0 0 l l l l 1 0 0 3 5 6 0 c D 7 4 4 4 7 ( 2 3 5 9 5 8 3 1 A A A A c c c c i i i i g g g g a a a a 1 2 r r r r n g g g g g F F F F g g o E E E E E t t / / / / / z g i c c c c t g g g g g g g g g i i i i B B r w w t t t t t t t t t / / 1 n n n n B o 2 / B g B g g g B B B B B B B B B a a a a t t t t Hh E E A E A E E A E A E 2 2 2 2 2 2 2 2 2 3 4 e e u u u u c c i i e e C C C C l l w w o o c c c c i i i i o o e P P l ³ ³ n n n n i f l g g g g e e i w w i i o a a a a a a s s r o t t t t P P P P p 4p S S S 2p S 3p S 1p TABLE 2. Selected physical and water properties pf soils TABLE Physical and water properties of Albeluvisols in the Silesian Lowland 127 peds in the upper part of an illuvial horizon. The peds wice 1 and 2 (Table 2). The most important for agri- meet requirements for fragic material; however, a fra- cultural use, a field water capacity (at pF=2.2), ran- gic horizon was distinguished not in the upper but in ged in humus A horizons between 16.6 and 26.4% the lower part of Bt horizon – due to an excessive and was higher in Paw³owice 1 and 2 soils by at least volume of cracks/tongues. It should be noted that the one fourth. The highest values were observed in the bulk density in E/Bt horizons in soils 3 and 4 was in E/Bt horizons – up to 36.4% (Paw³owice 1 and Psie general lower than this in the profiles 1 and 2, due to Pole 4) or in the illuvial horizons Bt/E with various differences in texture, especially lower content of share of albeluvic tongues – up to 32.6% (Paw³owice clay fraction, but also larger volume of eluvial (san- 2 and Psie Pole 3). The best ability of water storage dy) tongues. Particle density of investigated soils in soil was strongly correlated with content of collo- ranged from 2.55 to 2.66 g cm–3 and was the highest idal clay fraction, even when these horizons are dis- in the eluvial horizons, between 2.62 and 2.66 g cm–3 sected by tongues of albic material. However, in the (Table 2), e.g. due to negative relationship to organic profiles where penetration of albeluvic tongues into carbon and clay contents (Table 3). the illuvial horizons are very intensive, the highest Values of total porosity, calculated on the basis on average content of clay fraction and moisture at particle density and bulk density ranged between 0.28 pF=2.2 were in the deeper parts of B-horizon (like in to 0.43 m3 m3 and were significantly diversified wi- the soil Paw³owice 2), sometimes at the depth 100 cm thin the soil profiles (Table 2) with no simple depen- or deeper (Psie Pole 3). dence on organic matter or clay content (Table 3). Both the maximum and field water capacity in A, The highest values of total porosity were recorded in E, and Bt horizons of Luvisols developed of glacial the humus Ap horizons of all profiles, and in the illu- materials vary in a very broad ranges, and our results vial Bt horizons of soils Paw³owice 1 and 2. Obta- are similar to these given by other authors for Luvi- ined results of total porosity, contrary to the commonly sols with similar lithological discontinuities (Kacz- accepted assumption (Walczak, 1984), differed par- marek, 2001; Kobierski and D¹bkowska-Naskrêt, tly from the maximum retentive capacity. However, 2002; Komisarek and Sza³ata, 2008; Marcinek et al., reported difference may result from the inconsisten- 1995; Paluszek, 2011; Walczak et al., 2002b). This cy of measurement methods. Maximum retentive ca- can be interpreted either as (1) a prevailing impor- pacity (at pF=0) was directly determined after capilla- tance of textural differentiation, not a tonguing, for ry rise to the state of full saturation, while the total the water capacity of Luvisols and Albeluvisols, or porosity was calculated on the basis of the specific (2) the result of common analyzing of all clay-illu- gravity and bulk density. This difference may be espe- viated soils without distinguishing the Albeluvisols cially visible in the soils with high content of the from the Luvisols. Walczak et al. (2002b) have pro- swelling clay minerals (Paluszek, 2011). High values posed dividing of arable soils in three classes based of the total porosity in some E/Bt horizons of soils on the field water capacity. According to this classi- under study are also contrary to the results obtained fication, the investigated soils belong to the second in other Luvisols (Marcinek and Komisarek, 2004). class – soils with medium values of field water capa- This may result from the larger share of sandy infil- city (0.2–0.3 m3 m3). ling of tongues that influences the mean result of the Based on the field water capacity, the stock of easi- measurements. ly available water (at pF=2.2) in a 100 cm thick soil Soil moisture (expressed in volume percent) in column was calculated (Table 2). The water stock in most genetic horizons, in particular in the illuvial soils Paw³owice 1 and 2 was clearly higher indica- horizons, was at consecutive pF values higher in the ting larger ability for water retention at field capaci- profiles Paw³owice 1 and 2 as compared to Psie Pole 3 ty. Potentially, these soils can store 282–303 mm of and 4 (Table 2), probably due to strong positive corre- water, whereas the soils Psie Pole 3 and 4 between lation with clay content (Table 3). However, in the lo- 181 and 221 mm (Table 2). Among the analyzed Al- amy-textured humus A horizons (Paw³owice 1 and 2), beluvisols, the highest potential stock of easily ava- the moisture corresponding to the maximum water ilable water was determined in the profile 1, where capacity (pF=0) was 30–36% v/v, that was similar to the thickness of covering, coarser-textured material the values recorded in the sandy-textured is shallow and the intensity of dissecting with albelu- A horizons of the soils Psie Pole 3 and 4 (35–37% v/v). vic tongues is relatively lowest. Contrary, the lowest Also, there were no significant differences in moisture stock of water retention was found in the profile 3, at pF=0 in the sandy- and loamy-textured E and EBw due to the highest thickness and coarse texture of elu- horizons. But in E/Bt horizons, the moisture at pF=0 vial and humus horizons, as well as high share of was clearly higher in the finer-textured soils Paw³o- albeluvic tongues in the illuvial horizon. This situ- 128 BART£OMIEJ GLINA, PAWE£ JEZIERSKI, CEZARY KABA£A

TABLE 3. Coefficients of Pearson correlation for the entire data CONCLUSIONS set (coefficients significant at p<0.05 are marked with *) 1. Water storage at field water capacity in Albeluvi- dw pgor C0orp2Fp7F2.ptF2.syilcla dv0*.21-0.95-0.45*-0.080.270.390.080.25sols with lithological discontinuity is mainly de- dw 0.00-0.52*-0.53*-0.55*-0.56*0.26-0.36termined by texture variability and the thickness por 0.310.04-0.40-0.50*-0.01-0.30of eluvial (A+Et) and iluvial (E/B+Bt+BC) zones, Corg -0.09-0.24-0.20-0.04-0.41and may not differ from those in Luvisols with si- pF0 0.77*0.64*0.070.78* pF2.2 0.88*-0.14*0.91*milar textural differentiation pF2.7 -0.150.82*2. Water capacity in glossic E/Bt horizons of Albelu- silt -0.15visols depends on the intensity of eluvial material penetration into the illuvial horizon, which is rela- Explanation: dv – bulk density, dw – specific gravity, por – total porosity, Corg – organic carbon, pF0, pF2.2, pF2.7 – water capacity at given pF ted to abundance, width and depth of albeluvic ton- value. gues on the horizontal and vertical cross-sections. 3. Field water capacity of illuvial horizons largely ation is aggravated by intensive penetration of albe- dissected by albeluvic tongues (Bt/E) is the highest luvic tongues into the loamy B-horizon. Identified in the deeper part of horizon, below the zone of water stocks in examined profiles of Albeluvisols very intensive albeluvic tonguing. varied significantly, but were within wide range of values reported for Albeluvisols with texture diffe- ACKNOWLEDGMENT rentiation in soil profile (Kaczmarek et al., 2006). Easily available water stock is the result of both va- The study was financed by the National Science riable texture and thickness of the soil horizons, in Centre (research grant No. 2012/05/B/NZ9/03389). particular in soils with preserved distinct differentia- tion on the eluvial and illuvial zones within the profi- REFERENCES le (Zaleski, 2012). The most important feature influ- encing water retention in the Luvisols/Albeluvisols Bockheim J.G., Gennadiyev A.N., 2000. The role of soil-forming with lithological discontinuity seems to be the depth processes in the definition of taxa in soil taxonomy and the of occurrence of the loamy iluviall horizon and the world soil reference base. Geoderma, 95: 53–72. mean clay content in the illuvial horizon (including Bogacz A., £abaz B., D¹browski P., 2008. Wybrane w³aœciwoœci fizyczne i fizykochemiczne czarnych ziem w parku krajobra- mixed E/B or B/E horizons). Profiles with finer-te- zowym „Dolina Baryczy”. Roczniki Gleboznawcze – Soil xtured Bt horizons (clay content 27–32%) under thin- Science Annual, 59(1): 43–51. (In Polish). ner layer of covering materials had much higher wa- Buczko U., Bens O., Fischer H., Hüttl H.R.F., 2002. Water repel- ter retention properties than these with coarser- te- lency in sandy luvisols under different forest transformation xtured Bt horizons (clay content 6–18%) overlaid by stages in northeast . Geoderma, 109(1–2): 1–18. thicker cover sands. De Jonge, L.W., Kjaergaard, C., Moldrup, P., 2004. Colloids and Moreover, this study showed, which wasn’t ear- colloid-facilitated transport of contaminants in soils: an in- troduction. Vadose Zone Journal, 3: 321–325. lier commented more widely in the Polish soils, that Dexter A.R., 1997. Physical properties of tilled soils. Soil Tillage for the proper estimation of the water storage in the Research, 43: 41-63. Albeluvisols (soils with an argic horizon and albe- Dubicki A., Dubicka M., Szymanowski M., 2002. Klimat Wro- luvic tonguing) important are the characteristics of c³awia. [In:] Œrodowisko Wroc³awia – Informator 2002. Dol- E/Bt and B/E horizons, e.g. their thickness and share noœl¹ska Fundacja Ekorozwoju, Wroc³aw 9–25. (In Polish). (volume percentage) of albeluvic tongues in the trans- Guidelines for soil description, 2006. 4rd Edition, FAO, Rome. ition/illuvial horizons. Due to the small thickness and IUSS 2006. World Reference Base for Soil Resources 2006. 2nd edition, World Soil Resources Reports 103, FAO, Rome. complex (polygonal) character of albeluvic tongues, IUSS Working Group WRB, 2007. World Reference Base for it is impossible to collect separate samples of undi- Soil Resources 2006. First update 2007. World Soil Resour- sturbed eluvial and illuvial soil material from E/Bt ces Reports, 103. FAO, Rome. and Bt/E horizons. Larger number of replications (col- Jaworska H., D¹bkowska-Naskrêt H., 1999. Gleby p³owe wy- lected in various sites of mixed horizon) has, there- tworzone z utworów py³owych Pojezierza Che³miñsko-Do- fore, extreme importance for proper estimation of bulk brzyñskiego i Wysoczyzny Kaliskiej. Cz. III. Sk³ad chemicz- density and water properties of E/Bt and Bt/E hori- ny i mineralogiczny. Roczniki Gleboznawcze – Soil Science zons of the Albeluvisols. Annual, 50(1/2): 97–114. (In Polish). Kaczmarek Z., 2001. Pojemnoœæ wodna oraz zdolnoœci retencyj- ne gleb p³owych i czarnych ziem wytworzonych z glin more- nowych w rejonach oddzia³ywania Koniñskiego Zag³êbia Wêglowego. Roczniki AR Poznañ, 61, 49–61. (In Polish). Physical and water properties of Albeluvisols in the Silesian Lowland 129

Kaczmarek Z., Owczarzak W., Mocek A., 2006. W³aœciwoœci fi- Porêbska G., Ostrowska A., Borzyszkowski J., 2010. Forest soil zyczne i wodne uprawnych gleb p³owych oraz usytuowanych characteristic with respect to potential and actual water stora- pod zadrzewieniem œródpolnym w obrêbie agroekologiczne- ge. Polish Journal of Soil Science, 42(2): 115–128. go Parku Krajobrazowego im. Dezyderego Ch³apowskiego. Sauer D., Schülli-Maurer I., Sperstad R., Sorensen R., Stahr K., Journal of Research and Applications in Agricultural Engine- 2009. Albeluvisol development with time in loamy marine ering, 51(3): 35–39. (In Polish). sediments of southern Norway. Quaternary International, Kobierski M., D¹bkowska-Naskrêt H., 2002. Sk³ad mineralogicz- 209(1–2): 31–43. ny i wybrane w³aœciwoœci fizykochemiczne zró¿nicowanych Szymañski W., Skiba M., Skiba S., 2011. Fragipan horizon degra- typologicznie gleb Równiny Inowroc³awskiej. Cz. I. Morfo- dation and bleached tongues formation in Albeluvisols on the logia oraz w³aœciwoœci fizyczne i chemiczne wybranych gleb. Carpathian Foothils, Poland, Geoderma: 167–168, 340–350. Roczniki Gleboznawcze – Soil Science Annual, 54(4): 17– Szymañski W., Skiba M., Skiba S., 2012. Origin of reversible 27. (In Polish). cementation and brittneless of the fragipan in Albeluvisols of Komisarek J., Sza³ata S., 2008. Zró¿nicowanie uziarnienia w pro- the Carpathian Foothills, Poland. Catena, 99: 66–74. filach gleb p³owych zaciekowych z obszaru Wielkopolski. Szymañski W., Skiba S., 2012. Micromorphological Properties Nauka Przyroda Technologie 2(2): 1–14. (In Polish). of the Fragipan Horizon in Albeluvisols of the Carpathian Komisja V Genezy, Klasyfikacji i Kartografii Gleb PTG, 2011. Foothills. Polish Journal of Soil Science, vol. XLIV. no. 2: Systematyka Gleb Polski, wyd. 5, Roczniki Gleboznawcze – 193–200. Soil Science Annual, 62(3): 1–193. (In Polish). Turski M., Witkowska-Walczak B., 2004. Fizyczne w³aœciwoœci Konecka-Betley K., Zagórski Z., 1994. Wp³yw interglacjalnych gleb p³owych wytworzonych z utworów py³owych ró¿nej ge- procesów glebotwórczych na cechy mikromorfologiczne gleb nezy. Acta Agrophysica, 101, s. 56. (In Polish). kopalnych wytworzonych z lessów. Roczniki Gleboznawcze Walczak R., 1984. Modelowe badania zale¿noœci retencji wod- – Soil Science Annual, 45(3/4): 85–95. (In Polish). nej od parametrów fazy sta³ej gleby. Problemy Agrofizyki, Kühn P., 2003. Micromorphology and Late Glacial/Holocene 41. (In Polish). genesis of Luvisols in Mecklenburg–Vorpommern (NE-Ger- Walczak R., Ostrowski J., Witkowska-Walczak B., S³awiñski C., many). Catena, 54(3): 537–555. 2002a. Hydrofizyczne charakterystyki mineralnych gleb or- Marcinek J., Komisarek J., KaŸmierowski C., 1995. Degradacja nych Polski. Acta Agrophysica, 79: 1–64. (In Polish). fizyczna gleb p³owych i czarnych ziem intensywnie u¿ytko- Walczak R., Ostrowski J., Witkowska-Walczak B., S³awiñski C., wanych rolniczo w Wielkopolsce. Zeszyty Problemowe Po- 2002b. Spatial characteristic of hydro-physical properties in stêpów Nauk Rolniczych, 418(1): 141–147. (In Polish). arable mineral soils in Poland as illustrated by field water ca- Marcinek J., Komisarek J., 2004. Antropogeniczne przekszta³ce- pacity (FWC). International Agrophysics, 16: 151–159. nia gleb Pojezierza Poznañskiego na skutek intensywnego ich Van Ranst E., De Coninck F., 2002. Evaluation of ferrolysis in u¿ytkowania rolniczego. Wydawnictwo Akademii Rolniczej im. soil formation. Eurasian Journal Soil Science, 53: 513–519. Augusta Cieszkowskiego w Poznaniu, Poznañ. (In Polish). Zaleski T., 2012. Rola pedogenezy w kszta³towaniu w³aœciwoœci Paluszek J., 2011. Kryteria oceny jakoœci fizycznej gleb upraw- hydrofizycznych, retencji, re¿imu i bilansu wodnego gleb nych Polski. Acta Agrophysica, Rozprawy i Monografie, 191: wytworzonych z utworów py³owych Karpat. Zeszyty Nauko- s. 139. (In Polish). we UR w Krakowie 494, s. 114. (In Polish). Polskie Towarzystwo Gleboznawcze, 2009. Klasyfikacja uziar- nienia gleb i utworów mineralnych PTG 2008. Roczniki Gle- Received: October 25, 2013 boznawcze – Soil Science Annual, 60(2): 5–16. (In Polish). Accepted: January 8, 2014

Fizyczne i wodne w³aœciwoœci gleb p³owych zaciekowych Dolnego Œl¹ska

Streszczenie: Sk³ad granulometryczny, gêstoœæ objêtoœciowa i w³aœciwa, porowatoœæ ca³kowita, pojemnoœæ wodna w zakresie pF 0–2.7 oraz zapas wody u¿ytecznej w profilu przy pF 2.2 zosta³y okreœlone w glebach p³owych, zaciekowych z silniej lub s³abiej zaznaczon¹ nieci¹g³oœci¹ litologiczn¹ w profilu. Profile glebowe zlokalizowane zosta³y w pó³nocno-wschodniej czêœci Niziny Œl¹- skiej, na równinie denudacyjnej, gdzie na powierzchni glin moreny dennej zlodowacenia Odry powszechnie wystêpuj¹ utwory pokrywowe ró¿nej genezy, g³ównie piaski. We wszystkich badanych profilach wystêpuj¹ zacieki materia³u albic o uziarnieniu piasz- czystym w stropie gliniastego poziomu iluwialnego, a tak¿e silne oglejenie odgórne na styku poziomów eluwialnych i iluwialnych oraz w poziomach iluwialnych. Najni¿sze wartoœci gêstoœci objêtoœciowej stwierdzono w poziomach ornych, natomiast najwy¿sze w podornych poziomach EBw lub w zaciekowych poziomach E/Bt. Ca³kowita porowatoœæ jest najwiêksza w poziomach ornych, na- stêpnie skokowo maleje w poziomach E i na powrót roœnie z g³êbokoœci¹. Pojemnoœæ wodna (przy ka¿dej mierzonej wartoœci pF) jest najsilniej skorelowana z zawartoœci¹ i³u i skokowo roœnie w poziomach E/Bt. Najwy¿sza pojemnoœæ wodna przy pF 2.2 wystêpuje w poziomie E/Bt, przy niewielkiej liczebnoœci zacieków poziomu eluwialnego albo w g³êbszych czêœciach poziomu Bt, w przypadku du¿ej intensywnoœci wnikania zacieków eluwialnych w strop poziomu iluwialnego. Zapas wody (przy polowej pojemnoœci wodnej) w górnej, 100 cm warstwie gleb p³owych zaciekowych z nieci¹g³oœci¹ litologiczn¹, zale¿y od g³êbokoœci styku strefy eluwialnej i iluwialnej, podobnie jak w glebach p³owych typowych z podobnym zró¿nicowaniem uziarnienia w obrêbie profilu glebowego.

S³owa kluczowe: gleby p³owe zaciekowe, w³aœciwoœci wodne, sk³ad granulometryczny, nieci¹g³oœæ litologiczna