DE DE GRUYTER OPEN Textural diversity in selected Retisols of Opalenica Plain 11 SCIENCE ANNUAL DOI: 10.1515/ssa-2017-0002 Vol. 68 No. 1/2017: 11–18

MICHA£ KOZ£OWSKI*, JOLANTA KOMISAREK

Poznan University of Life Sciences, Department of and Land Reclamation, Pi¹tkowska 94 Str., 60-649 Poznañ, Poland

Textural diversity in selected Retisols in the catena of the Opalenica Plain (western Poland)

Abstract: The investigation was carried out in the catena of Retisols within the Opalenica Plain. The aim of the study was to characterize the variation in texture of selected Retisols formed from ground moraine glacial till of Leszno Phase of Vistulian glaciation. The analyzed are characterized by a similar degree of soil material segregation, which is characteristic for the typical glacial till. Particle size distribution and granulometric indices lead to conclusion that soils located in the catena on summit and shoulder positions, have vertical texture distribution formed primarily by lessivage process. Sandy texture of eluvial horizons noted in the Retisol of the slope pediment can be a consequence of not only lessivage but also of slope forming processes that led to the appearance of lithic discontinuity. The cluster analysis using Ward’s method and 1-rPearson as the distance measure can be helpful for identification the lithogenic uniformity and/or non-uniformity of soil parent material. Keywords: Retisols, lithic discontinuity, catena

INTRODUCTION MATERIALS AND METHODS

One of the fundamental features of soil, determining The study was carried out in the area of Granowo its properties, is the texture. Determination of particle commune, on arable land in southern and central part size distribution, including distinction of fractions of of Poznan Lake District in the Opalenica Plain. The subfractions in certain horizons of soil profile is the study area is located at about 38 km SE from Poznan main indicator of the genesis and taxonomy of a given (Fig. 1). The field work was carried out in two stages. soil and makes the basis for interpretation of the con- In the first one the variation of soils was established ditions of parent material deposition, its lithological by the method of scattered points (pits and boreholes) uniformity or non-uniformity (Dobrzañski et al. 1977, and then representative pedons were localised. In the Kowalkowski and Borzyszkowski 1977, Konecka- second stage the “Granowo” transect of 1200 m in Betley 1979, Prusinkiewicz and Proszek 1990, Polish length was delineated. In 25 open pits along the transect 2011). Of particular importance is and 4 pedons of the stationary measurements, the soil the vertical differentiation in the texture for Retisols morphology was determined by identification of inherited from glacial materials, that has been many genetic and diagnostic horizons, boundaries between times related not only to the lessivage process but horizons, soil colour, structure, consistency, reaction also with lithogenesis (Prusinkiewicz and Kowalkow- with chloric acid and taxonomic classification of soils. ski 1964, Kowalkowski and Ludwikowska 1993, Pedons of the stationary measurements were instru- Zagórski 1995, 2003; D¹bkowska-Naskrêt and Jaworska mented with moisture sensors and piezometer to measure 1997, Œwitoniak 2006). That is why for Retisols a the profile content and the water table. thorough analysis of particle size distribution should In terms of geomorphology, the Granowo transect make the basis for evaluation of their properties, genesis runs through flat ground moraine originating from and systematic classification. Leszno Phase of Vistulian glaciation (Krygowski The study presented in this paper is aimed at 1953, 1961; Starkel 1987). The upland is cut with determination of genesis and variations in texture of subglacial channels in which at present run the rivers selected Retisols formed from ground moraine glacial Mogilnica and Struga Kamieniecka, flowing to the till of Leszno Phase of Vistulian glaciation. The Warciañsko-Odrzañsk proglacial stream valley. The particle size analysis was performed using the sedi- parent material of the soils in the study area is carbonate mentological indices (Folk and Ward 1957) and gra- glacial till that has been decalcified and has sandy nulometric indices (Prusinkiewicz and Proszek 1990, texture in upper layers. IUSS Working Group WRB 2015).

* Dr in¿. M. Koz³owski, [email protected] http://ssa.ptg.sggw.pl/issues/2017/681 12 MICHA£ KOZ£OWSKI, JOLANTA KOMISAREK

FIGURE 1. Location of investigated area and distribution of wells in the toposequence: S – summit, S2 – shoulder, T –pediment, A – footslope, CZ – , PW – Luvisols, PA – Retisols; Texture Classes (According to PTG 2009): 1, 2 – , 3 – loamy sand, 4, 5 – sandy , 6 – loam, 7 – sandy loam

In laboratory studies, the and clay fractions proposed by Folk and Ward (1957) expressing the were determined by the aerometric method, according particle diameters in the phi scale. The granulometric to the norm PN-R-04032 (1998), while the sand particles indices were calculated after Prusinkiewicz and Pro- were distinguished by the sieve method with wet szek (1990): A – (0.25–0.1 mm)/(0.5–0.25 mm), B – fractioning. The division into textural classes was (0.25–0.1 mm)/(1.0–0.5 mm); C – (0.25–0.05 mm)/ made according to the PTG (2009). (0.5–0.25 mm); D – (0.25–0.02 mm)/(1.0–0.25 mm); The sedimentological indices and cumulative curves E – (0.5–0.05 mm)/(1.0–0.5 mm). In order to identify of soil particle size were determined by the procedure the primarily non-uniformity of the soil parent material, Textural diversity in selected Retisols of Opalenica Plain 13 the criteria referring to granulometric indices proposed RESULTS AND DISCUSSION by IUSS Working Group WRB (2015) were applied. Lithic discontinuities were identified if (i) the diffe- The pedons analysed were labelled as Ga14, Ga12, rence in the ratio of coarse to medium sand between Ga10 and Ga6 and classified as Eutric Albic Glossic two layers reaches at least 25% and the absolute Retisol (Abruptic, Epiarenic, Endoloamic, Aric, Cutanic, difference in the content of coarse and/or medium Ochric) (gleba p³owa zaciekowa typowa acc. PSC sand between them is at least of 5%, or (ii) if the 2011) – Ga14 and Ga10, Eutric Albic Glossic Retisol difference in the ratio of coarse to fine sand between (Abruptic, Arenic, Aric, Cutanic, Ochric) (gleba p³owa two layers reaches at least 25% and the absolute zaciekowa spiaszczona acc. PSC 2011) – Ga12, and difference in the content of coarse and/or fine sand is at Eutric Albic Glossic Endogleyic Retisols (Abruptic, least of 5%, or (iii) if the difference in the ratio of Epiarenic, Endoloamic, Aric, Cutanic, Ochric) (gleba medium to fine sand between two layers is at least of p³owa zaciekowa spiaszczona „z cechami gruntowego 25% and the absolute difference in the content of oglejenia” acc. PSC 2011) – Ga6. The soils studied medium and/or fine sand is at least of 5%. showed well-developed eluvial horizons, which in To evaluate the degree of similarity or difference profiles Ga14, Ga12 and Ga10 show the texture of in the particle size distribution in the sand separate, loamy , while in pedon Ga6 – the texture of fine the cluster analysis using Ward’s method and sands. The horizons with albeluvic glossae properties 1-rPearson as a distance measure was used. The paper and the argic horizon that lie below the above- presents results of laboratory determination of particle mentioned eluvial horizons, usually show sandy loam size distribution and granulometric indices calculated texture. The boundary between the eluvial sandy for four representative Retisols profiles: Ga14, Ga12, horizons and clay illuvial ones was observed in the Ga10 and Ga6 (Fig. 1). form of tongue-shaped patches of E horizon into Bt

TABLE 1. Particle size distribution of analyzed soils

-iroH htpeD mmniretemaidtanoitcarfliosfoegatnecreP ssalcerutxeT noz )mc( 1–2 5.0–1 52.0–5.0 1.0–52.0 50.0–1.0 20.0–50.0 500.0–20.0 200.0–500.0 200.0< GTP ADSU

41aG pA 82–0 9.1 5.7 5.81 1.34 21 6 6 5 0 rdgp SL E 34–82 3.3 5.8 4.61 8.44 01 6 7 4 0 rdgp SL E/B 08–34 2.1 4.8 2.61 2.73 11 4 8 4 01 rdpg LSF tB 011–08 1.1 6 7.31 2.93 01 5 8 0 71 rdpg LSF 1C 551–011 5.1 8.5 4.21 3.63 21 7 7 4 41 rdpg LSF 2kC –551 5.1 1.6 7.21 7.93 01 5 11 3 11 rdpg LSF 21aG pA 52–0 3.1 8 3.71 4.74 01 6 6 4 0 rdgp SL 1E 04–52 2.1 4.7 2.91 2.44 21 6 5 5 0 rdgp SL 2E 85–04 9.0 8 4.71 7.64 01 7 5 5 0 rdgp SL B/E 07–85 2.1 8.6 71 34 01 7 5 5 5 rdgp SL E/B 001–07 1.2 9.6 9.31 1.33 21 6 7 4 51 rdpg LSF tB 031–001 4.2 1.6 3.11 2.73 6 7 8 5 71 lg LSF 01aG pA 82–0 7.0 8.7 6.71 9.84 9 6 5 5 0 rdgp SL E 73–82 3.1 6.7 1.61 34 21 5 8 6 1 rdgp SL B/E 85–73 8.1 2.7 8.41 2.14 8 21 5 4 6 rdpg LSF E/B 56–85 6.1 4.5 2.21 8.43 31 5 8 4 61 rdpg LSF 1tB 001–56 5.1 9.5 5.21 1.73 11 6 8 3 51 rdpg LSF 2tB 051–001 5.1 8.5 4.21 3.83 11 6 8 4 31 rdpg LS 6aG pA 82–0 9.0 31 82 1.14 9 3 3 1 1 rdlp S E 05–92 2.1 4.9 13 4.14 9 4 4 0 0 rdlp S E/B2 56–05 4.1 3.6 3.41 04 01 5 01 2 11 rdpg LSF gtB2 511–56 1.1 7.5 3.31 9.43 31 7 6 3 61 rdpg LSF gC2 031–511 2.1 4.5 21 4.63 31 6 11 2 31 rdpg LSF

Explanation: pldr – piasek luŸny drobnoziarnisty, pgdr – piasek gliniasty drobnoziarnisty, gpdr – glina drobnopiaszczysta, gl – glina lekka, S – sand, LS – loamy sand, FSL – fine sandy loam, SL – sandy loam. 14 MICHA£ KOZ£OWSKI, JOLANTA KOMISAREK one, leasing to development of a albeluvic glossae 16–19%. In the pedons localised higher in the relief, properties (Bouma et al. 1968, Spiridonova et al. the profile differences in the content of silt separate 1999). After Thoms (1993), Frederick et al. (2002) were not so much pronounced as in Ga6 soil (Table 1). and Staff (2010), the abrupt smooth or The content of clay fraction did not exceed 1% in the wavy boundary change appearing between eluvial and eluvial horizons of the soil studied, but in the deeper illuvial horizons can be related to lithological heterogenity illuvial horizons the content of this fraction varied of the soil parent material. from 11 to 17%. The particle size composition of the Retisols studied The Retisols studied showed poor sorting of shows the domination of sand fraction whose content mineral material of eluvial horizons whose segregation in the eluvial horizons in soils of Ga14, Ga12 and coefficient (GSO) varied from 1.77 to 2.14 in pedons Ga10 varies from 80 to 84%, while in Ga6 soil it Ga14, Ga12, Ga10, while in pedon Ga6 this coefficient reaches 92% (Table 1). The fine sand is dominant varied from 1.31 to 1.40. The deeper horizons were and the second most abundant is medium sand. In the characterised by very poor (E/B horizon) or extremely profile distribution of the sand particle-size classes poor sorting of soil material, which can be related to in Ga14, Ga12 and Ga10 no significant differences primeval uniformity of the parent material. According were noted between the horizons. Only in the Ga6 to Prusinkiewicz and Proszek (1990), as well as a significant difference in the content of medium sand Zagórski (1996) poor, very poor or extremely poor was apparent. In the eluvial horizons of this pedon sorting is characteristic feature of glacial till. Commonly the medium sand content varied from 28 to 31%, while observed for Retisols is the profile variation in GSO, in deeper horizons it varied from 12 to 14.3%, which evident when comparing the values for eluvial horizons can indicate the profile non-uniformity of the parent (A and E) with illuvial ones or parent materials. The GSO material. This observation is confirmed by the profile values indicate a slightly better sorting of eluvial distribution of silt fraction, whose content in eluvial horizons in which the mean grain diameter d varies from horizons was 7–8%, while in deeper horizons it was 0.109 to 0.209 mm, while in the deeper argic horizon

FIGURE 2. Cumulative texture curves of investigated soils Textural diversity in selected Retisols of Opalenica Plain 15 the diameter d varies from 0.023 to 0.053 mm. It is E indices are slightly lower in eluvial horizons than related to the accumulation in illuvial horizons of fine in the deeper argic horizon. This small diversity does fractions washed out from higher eluvial horizons in the not justify a conclusion about different genesis of eluvial process of lessivage. A confirmation of this inter- and illuvial deposits. This observation is confirmed pretation can be the different shape of cumulative by the results of application of the above defined criteria texture curves for these horizons (Fig. 2). In eluvial consistent with those of the IUSS Working Group horizons, the cumulative texture curves are leptokurtic WRB (2015). In Ga12 and Ga10 soils no significant (Ga6) (GSP:1.26–1,31) or very leptokurtic (Ga12, differences in granulometric indices across the profile Ga10, Ga14) (GSP:1.63–1.21) while for the argic were noted. Also the application of IUSS Working diagnostic horizon this distribution is extremely Group WRB (2015) criterion on the contributions of leptokurtic (GSP:3.46–4:63). These profile differences sand particle-size classes did not permit identification in particle size distribution in Retisols is often of non-uniformity of the parent material. On the basis interpreted as a result of not only but also of the results obtained it can be concluded that in the lithogenesis (Baraniecka and Konecka-Betley 1993, Retisols studied Ga14, Ga12 and Ga10, the mineral Kowalkowski and Ludwikowska 1993, Œwitoniak 2008). materials were diversified mainly in the process of Therefore, often granulometric indices are used for lessivage into the sand eluvial part and the deeper identification of the profile diversity of parent material illuvial part with accumulated clay fraction. Similar (Zagórski 1996). results have been obtained by Marcinek and Wiœlañ- Table 2 and Figure 3 present the granulometric ska (1984), Komisarek (2000) and Komisarek and indices determined for the soils studied. In the ground Sza³ata (2008). In the profile Ga6 the granulometric moraine upland soil analysed (Ga14), there are no index A took the values of 1.47 and 1.37, at the Ap significant differences in the values of A, B and C and E horizons, respectively, while in deeper horizons indices between horizons. Only the values of D and the values of this index varied in the range 2.63–3.04. The distribution of B, C and D indices across the profile TABLE 2. Sedimentological indices of analyzed soils was similar. From these data it can be concluded that within the pediment of the ESE exposition slope there noziroH htpeD SSG OSG KSG PSG d are Retisols with lithic discontinuity separating the ]mc[ ]mm[ sandy eluvial zone from deeper illuvial horizon. This 41aG conclusion is corroborated by the values of granulo- pA 82–0 68.2 98.1 72.0 46.1 831.0 metric indices used by IUSS Working Group WRB E 34–82 18.2 19.1 42.0 17.1 341.0 E/B 08–34 08.3 70.6 76.0 46.4 270.0 (2015). Significant differences were noted in the content tB 011–08 04.5 64.8 18.0 36.4 420.0 of medium sand, which was 28% and 31% in Ap and 1C 551–011 05.4 64.7 27.0 61.4 440.0 E horizons, respectively, while in deeper horizons this 2kC -551 89.3 33.6 96.0 28.3 360.0 content varied from 12 to 14%. The smaller GSO 21aG values in the eluvial horizons of Retisol in Ga6 than pA 52–0 97.2 77.1 52.0 58.1 541.0 those determined for Ga14, Ga12 and Ga10, indicate a 1E 04–52 97.2 18.1 62.0 07.1 541.0 slightly better sorting and longer deposition path of 2E 85–04 68.2 68.1 03.0 49.1 831.0 B/E 07–85 32.3 62.2 24.0 56.1 701.0 the surface deposits of the slope pediment than those E/B 001–07 14.4 45.7 17.0 50.4 740.0 for the material deposited in higher parts of the slope. tB 031–001 34.5 94.8 97.0 64.3 320.0 These differences should be related to slope forma- 01aG tion processes in which the material transport was very pA 82–0 08.2 08.1 82.0 01.2 441.0 short, while the deposition was rapid and of poor E 73–82 02.3 41.2 63.0 36.1 901.0 segregation (Smolska 2008, Mycielska-Dowgia³³o and B/E 85–73 82.3 24.3 15.0 06.2 301.0 E/B 56–85 36.4 76.7 47.0 08.3 140.0 Ludwikowska-Kêdzia 2011). 1tB 001–56 34.4 44.7 37.0 71.4 740.0 Within Retisols of this slope pediment, lithic 2tB 051–001 42.4 59.6 27.0 12.4 350.0 discontinuities were also observed (Koz³owski 2007). 6aG Figure 4 presents results of the cluster analysis. pA 82–0 62.2 04.1 31.0 13.1 902.0 This method permits determination of differences in E 05–92 92.2 13.1 41.0 62.1 402.0 the character of the frequency curves of particle size E/B2 56–05 58.3 92.6 86.0 24.4 960.0 distribution for the sand fraction between different gtB2 511–56 06.4 86.7 47.0 85.4 140.0 gC2 031–511 31.4 97.6 96.0 40.4 750.0 horizons and thus can be used as identification of lithic discontinuities. As follows from the data obtained, in Explanation: GSS – average particle size, GSO – standard deviation, Ga6 profile the eluvial Ap and E horizons show the GSK – skewness, GSP – kurtosis. particle size distribution in sand fraction different from 16 MICHA£ KOZ£OWSKI, JOLANTA KOMISAREK

FIGURE 3. Granulometric indices of analyzed soils those obtained for deeper horizons. The distance be- by Ahr et al. (2012, 2013) for sandy mantle of tween two clusters, one made of Ap and E and the the Texas Gulf Coastal Plain. other comprising 2Btg and 2Cg exceeds 0.21, which means that the correlation coefficient of particle size CONCLUSIONS distribution in the sand fraction is close to 0.79. For the Retisols in Ga14, Ga12 and Ga10 profiles, the 1. The Retisols studied show similar degree of soil differences in particle size distributions in the sand material segregation which is characteristic of fraction between different horizons or clusters of typical glacial till. horizons do not exceed 0.02 of the measure applied. 2. The vertical differences in particle size distribution Results of the Ward clustering confirmed that the and granulometric indices, confirmed the dominant profile differences in particle size distribution in Retisols contribution of the process of lessivage in deve- is mainly a result of translocation of the finest particles lopment of textural vertical contrast of Retisols from the eluvial horizons to illuvial ones (Marcinek located on summit and shoulder catenal positions. and Wiœlañska 1984, Komisarek 2000, Komisarek and 3. Sandy texture of eluvial horizons noted in the Sza³ata 2008), although in the pedons studied an abrupt Retisol of the slope pediment can be a consequen- change in particle size distribution is found. This ce of not only lessivage but also of slope forming interpretation is in agreement with the results reported processes that led to the appearance of lithic discon- tinuity. Textural diversity in selected Retisols of Opalenica Plain 17

FIGURE 4. Dendrograms of hierarchical cluster analysis of sand fraction

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Zró¿nicowanie sk³adu granulometrycznego w wybranych glebach p³owych zaciekowych Równiny Opalenickiej

Streszczenie: W pracy przedstawiono wyniki badañ zró¿nicowania uziarnienia w glebach p³owych zaciekowych uk³adu katenal- nego Równiny Opalenickiej. Celem pracy by³o okreœlenie genezy zró¿nicowania sk³adu granulometrycznego w wybranych glebach p³owych zaciekowych wytworzonych z gliny zwa³owej dennomorenowej zlodowacenia ba³tyckiego fazy leszczyñskiej. Analizowane gleby p³owoziemne cechuj¹ siê s³abym lub skrajnie s³abym stopniem segregacji materia³u glebowego, który charakterystyczny jest dla typowych glin morenowych. Uzyskane wyniki zró¿nicowania sk³adu granulometrycznego i wskaŸników uziarnienia w profilach analizowanych gleb kulminacji i stoku swobodnego wyniesienia dennomorenowego, wskazuj¹ na g³ówny udzia³ procesu lessiwa¿u w kszta³towaniu siê profilowego zró¿nicowania sk³adu granulometrycznego. Silne spiaszczenie poziomów eluwialnych w jednym profilu gleby p³owej zaciekowej pedymentu stoku, mo¿e wynikaæ nie tylko z procesu lessiwa¿u, ale tak¿e z procesów stokowych, które doprowadzi³y do powstania nieci¹g³oœci litologicznej. Analiza skupieñ metod¹ Worda z miar¹ odleg³oœci 1-rPearson mo¿e byæ pomocna przy identyfikacji jednorodnoœci i/lub niejednorodnoœci materia³u glebowego. S³owa kluczowe: gleby p³owe zaciekowe, nieci¹g³oœæ litologiczna, katena