soil sequences atlas 2014

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SOILSEQUENCES

ATLAS


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SOIL SEQUENCES ATLAS

EDITED BYMARCIN WITONIAK

PRZEMYSAW CHARZYSKI

NICOLAUS COPERNICUS UNIVERSITY PRESS

TORU 2014


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Edi , Nica Ceic Uiei, T, Pad , Nica Ceic Uiei, T, Pad

Reiee:f. , DiecfIie f Si ad Pa Sciece,Laia Uiei f Agice, Jegaa, Laiaf. , Secea f Pih Scie f Si Sciece, Waa Uiei f Life Sciece

Lagage ediig

Ce deig

Phgah he ce

WYDAWNICTWO NAUKOWEUNIWERSYTETU MIKOAJA KOPERNIKAREDAKCJA: . Gagaia 5, 87100 TTe. (56) 611 42 95eai: daic@k.

DYSTRYBUCJA: . Reja 25, 87100 TTe./fa (56) 611 42 38eai: [email protected]: Wdaic Nake UMK. Gagaia 5, 87100 T

ISBN 9788323132820

Cfded b

The ie eeed i hi k ae he f he cib ad d eceai efec he fhe Eea Cii.

Si Seece AaM. iiak, P. Chaki (Edi)Fi Edii


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CHAPTER 10 141S L T MZBIGNIEW ZAGRSKI,MONIKA KISIEL

CHAPTER 11 155S ( S M, P)JAROSAW WAROSZEWSKI,CEZARY KABAA,PAWE JEZIERSKI

CHAPTER 12 169F B F (H)MARCIN WITONIAK,TIBOR JZSEF NOVK,PRZEMYSAW CHARZYSKI,KLAUDYNA ZALEWSKA,RENATA BEDNAREK

CHAPTER 13 181A SN, E HTIBOR JZSEF NOVK,GBOR NGYESI,BENCE ANDRSI,BOTOND BUR

CHAPTER 14 197U HGBOR SNDOR,GYRGY SZAB

CONTRIBUTORS 210


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FOREWORD

To understand the soil-landscape relation it is necessary to study the spatial diversity of soil cover.

This variability is partly predictable due to the substantial repeatability of soil units. Depending on

dominant soil-forming factor affecting the repeated soil patterns, different types of soil sequences can

be distinguished. The influence of relief on the repeated variability of soil cover was first noticed by

Milne in 1935 in East Africa. He proposed the term catena to describe a transect of soils that are

related to the topography. Sommer and Schlichting in 1997 distinguished several archetypes of

catenas depending on the mobilization processes and hydrological regimes. The impact of climate on

the variability of soil cover is described as climosequences. The diversity of soils due to the different

time of development - chronosequences are a suitable tool for investigating rates and directions of soil

and landscape evolution.

This book provides an extensive database of soil sequences of various types from the followingcountries: Hungary, Latvia, Lithuania and Poland. The main objective of this study was to present

a great diversity of soil-landscape/climate/hydrology relations and its effect on patterns in soil cover.

Most recent edition of the World Reference Base classification system was used to classify presented

soils (2014). FourteenReference Soil Groups are represented in this publication.

The collected data will be a useful tool in soil-science teaching, helping to understand reasons of

variability of soil cover and influence of various soil-forming factors on directions and degree of de-

velopment of Earth skin. Presented data can also be used for comparison purposes.

Marcin witoniak

Przemysaw Charzyski


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LIST OF ACRONYMS

A aii eaced b a acid ai aae iA i eaced b i f HCO4HFBS bae aaiCEC cai echage caaci

CECca CEC f he caEC1:2 eecica cdcii f a 1:2 iae eacEC1:2.5 eecica cdcii f a 1:2.5 iae eacECe eecica cdcii f he i aai eacEh ed eia eaed he adad hdge eecdeESP echageabe di eceageFAO Fd ad Agice Ogaiai f he Uied NaiFed i eaced b a dihiieciaebicabae iFe i eaced b a acid ai aae iFe i eaced b i f HCO4HFHA eia (hdic) acidi (H8.2) b he Kae ehdIUSS Ieaia Ui f Si Sciece

N a igeOC gaic cabHa H eaee efeed he aca i ieHe H f aai aeH H eaee afe icbai f i ae de aba cdii ihi hH H eaee afe idai ih 30% H2O2H he ide ed ae ed cdii i ae ad i cacaed f Ha ad Eh ae (egaie

gaih f he hdge aia ee)SAR di adi aiSP ie ce a aai (aai eceage)S a hTEB a echageabe bae

METHODS

The i ee caified accdig WRB 20141. The i hg decii ad b f i hi aegie afe Gideie f Si Decii

2. The ae ee ake f eeced i hi ad afe eaai

(dig, eaai f ad ad faci >2 b ieig) i a aaed i he aba. Tee a deeied b (i) cbiig he Bc3hdee ad iee ehd (ii) b iee ad iee ehd. Ogaiccab (OC) ce a deeied b he e dichae idai ehd, ad a ige (N) ce bhe Kjedah ehd. The eaci a eaed i H2O ad 1 M KC i 1:2.5 ei f iea ae, ad1:10 ei f gaic ae. Caci cabae (CaCO3) ce a deeied b Scheibe eicehd. Peia (hdhic) acidi (HA) a deeied b Kae ehd ad echageabe cai (bae)ce a eiaed b eachig ih 1 M ai aceae ih a bffe i H 8.2. Pedgeic f fi ad ai ee eaced: Fead Fed b HCO4HF, Fedb di dihiieciaebicabae4ad Fead Ab ai aae bffe i

5. Ohe i aae ee efed accdig he adad eh

d6. C ha bee decibed accdig Me

7. I a ecded (i) i he ie cdii (ige ae)

(ii) i he d ad ie cdii (dbe ae).

1IUSS Wkig G WRB, 2014. Wd Refeece Bae f i ece 2014. Ieaia i caificai e f aig iad ceaig eged f i a. Wd Si Rece Re N. 106. FAO, Re.

2FAO, 2006. Gideie f Si Decii, Fh edii. FAO, Re.

3Bc, G.M., 1951. Paice aai b hdee ehd. Ag Ja 43, 434438.

4Meha, O.P., Jack,M.L., 1960. I ide ea fi ad ca. Dihiieciae e bffeed ih di bicabae.

Ca ad Ca Miea 7, 313327.5Mckeage, J.A., Da, J.H., 1966. Ai aae ad DCB eaci f Fe ad A. Caada Ja f Si Sciece 46, 1322.

6

Va Reeijk, L.P. 2002. Pcede f i aai. 6h Edii. Techica Pae 9. Wageige, Nehead, ISRIC Wd Si Ifai.

7Me Si C Cha, 2009. Gad Raid, Michiga USA.


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SOIL REFERENCE GROUPS INDEX

SOIL REFERENCE GROUP COUNTRY PAGE1 ALISOLS POLAND 1422 ARENOSOLS LITHUANIA 24

POLAND 48,50,68,86,110,112114,128,130,156

HUNGARY 182,184,186,2043 CAMBISOLS POLAND 144,148,1644 GLEYSOLS POLAND 38,40,42,94,96

HUNGARY 1905 HISTOSOLS LITHUANIA 32

POLAND 54,56,1346 LUVISOLS LATVIA 18

POLAND 64,66,80,82,84HUNGARY 170,172

7 PHAEOZEMS LATVIA 12,14

POLAND 100

HUNGARY 1888 PLANOSOLS POLAND 1629 PODZOLS LITHUANIA 26,28,30

POLAND 50,52,116,118,126,15810 REGOSOLS POLAND 78,9811 RETISOLS LATVIA 16

POLAND 6212 STAGNOSOLS POLAND 102,146,16013 TECHNOSOLS POLAND 132

HUNGARY 198,200,20214 UMBRISOLS POLAND 70,130

HUNGARY 174


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STUDY AREAS

NUMBER OF CHAPTER REGION AND COUNTRY:

1BOREONEMORAL ZONE,LATVIA

2DAINAVA GLACIOFLUVIAL LOWLAND,LITHUANIA

3PUCK LAGOON,POLAND

4TUCHOLA FOREST,POLAND57BRODNICA LAKE DISTRICT,POLAND

89TORU BASIN,POLAND

10WITOKRZYSKIE MOUNTAINS,POLAND

11STOOWE MOUNTAINS,POLAND

12BKKALJA FOOTHILL,HUNGARY

1314SOUTHNYRSG AND DEBRECEN,HUNGARY


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Soils of Quercus robur L. stands on parent material withdifferent genesis in the boreo-nemoral zoneRaimonds Kasparinskis, Vita Amatniece, Oerts Nikodemus

The distribution range of Q. robur L. covers allof Europe and extends to the Ural Mountainsin Russia, reaching its northern distributionrange in Scotland, Sweden and Estonia (Hyt-teborn et al., 2005). In the context of climatechange, it is important to understand the lim-iting factors for the distribution of each tree

species. Not only climate but also soil is one ofthe main limiting factors in the distribution ofmany tree species. Our research was conduct-ed in Latvia, located in the boreo-nemoraltransition region between the boreal andnemoral zones (Sjrs, 1963), near the north-ernmost distribution limit of oaks (Quercusrobur L.). In Latvia, about 9734,38 hectares arecovered by oak stands, i.e. 0.34% of the total area of forests (State Forest Service, 2011).

In the boreo-nemoral transition region, Q. robur forms mixed stands on rich soils with nemoral

tree species: linden (Tilia cordata Mill.), maple (Acer platanoides L.), elm (Ulmus glabra Huds.), whiteelm (Ulmus laevis Pall.) and common ash (Fraxinus excelsior L.), and boreal conifers pine (Pinussylvestris L.) and spruce (Picea abies (L.) H.) (Hytteborn et al., 2005).

Lithology and topographyLithology and topographyLithology and topographyLithology and topographyIn Latvia, forests occur on soils of relativity high diversity, formed on different, mainly unconsolidat-ed Quaternary deposits, in some places also on weakly consolidated pre-Quaternary terrigenous orhard carbonate sedimentary rocks (Kasparinskis, Nikodemus, 2012). The presented soils occur ona glaciolacustrine plain (Profile 1), glaciofluvial deposits (Profile 2), a glacigenic till hummock (Profile3) and a glacigenic till plain (Profile 4) (Fig. 1).

ClimateClimateClimateClimateLatvia is located in the transition zone of the nemoral and boreal zones (Ozenda, 1994), or the boreo-nemoral zone (Sjrs, 1963). The climate is between transitional maritime and continental with a meantemperature of -5.3C in January and 14.8C in July. Annual precipitation is 700800 mm, of whichabout 500 mm falls in the warm period (data from the Central Statistical Bureau of Latvia, 2013).Theclimate is more continental towards the east. The forest area is about 55% and the dominant speciesare pine (Pinus sylvestris L.), birch (Betula pendula L.) and spruce (Picea abies (L.) H.), which repre-sent 43%, 28% and 15% of the total growing stock volume, respectively (State Forest Service, 2008).Only about 1.1% of the forest area is dominated by nemoral tree species, such as oaks (Quercus roburL). An increase in the climate continentality from west to east is one of the main factors determininga decrease in the oak abundance with the increasing distance from the Baltic Sea (Krampis, 2010).

F. 1. L S Q L (afe Gegica a f Laia,1981)


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Soils of Quercus robur L. stands on parent material with different genesis in the boreo-nemoral zone

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P 1 SagicP(Aeic, Ric)L: EaLaia ad, gaciacie ai, fa eai 00.2%, ak fe, 111 a...

N600910, E204726

O

A

AE

EB

B

BC

2C

M:

20 c, igh deced gaic aeia;

018 c, hi, ad a, e dakga (10YR 3/1), i, deae gaa adbaga bck fie, edi ad cae ce, diffe ad h bda;

1828 c, hi, ad a, e dakgaih b (10YR 3/2), i, g gaaad baga bck fie, edi ad cae

ce, diffe ad a bda;

2844 c, ad, ae b (10YR 6/3), i,eak baga ad aga bck edi adcae ce, eie, edcig cdii, c ie eiide caig,diffe ad a bda;

4462 c, ad, ae b (10YR 6/3), e,eak baga ad aga bck edi adcae ce, abda ie eiide caig, eie, edcig cdii, c edcihic e, diffe ad

a bda; 6292 c, ad, ae b (2,5Y 7/3), e,eak baga ad aga bck edi adcae ce, eie, edcig cdii, c ie eiide caig,c edcihic e, cea adh bda;

92(109) c, ae aeia, ,a ad, geeih ga (GLEY2 5/5), e e,eak baga ad aga bck edi adcae ce, edcig cdii, e feie edcihic e, deae

cacae.

[c] 0

50

110


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Raimonds Kasparinskis et al.

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T 1. T

HD[]

P [] T2.00.05 0.050.002 < 0.002

Ah 018 55 44 1 SL

AEh 1828 64 35 1 SL

EBg 2844 87 11 2 S

Bg 4462 92 3 5 S

BCg 6292 88 10 2 S

2Ck 92(109) 72 25 3 LS

T 2. C

HD[]

OC[

1]

N[

1]

C/NHKC

CCO3[

1]

A3+ F2+ M2+

[1]

Oi 20 760 112 7 5.9 4.5 1.69 32.0

Ah 018 22.0 4.80 5 5.5 50.7 4.77 2.93

AEh 1828 10.0 0.90 11 5.3 16.9 2.29 0.74

EBg 2844 4.8 2.9 0.97 0.22

Bg 4462 4.9 1.2 0.12 1.07

BCg 6292 6.0 1.4 0.37 0.23

2Ck 92(109) 7.3 + 0.6 0.23 6.10

CaCO3 abe; + CaCO3 ee

T 3. S

HD[]

C2+

M2+

K+

N+

TEB TA CEC CEC BS[%][(+)

1]

Oi 20 35.6 4.56 0.350 0.083 40.6 0.050 40.6 100

Ah 018 9.38 1.07 0.102 0.053 10.6 0.563 11.2 350 95

AEh 1828 5.73 0.74 0.018 0.032 6.52 0.188 6.71 321 97

EBg 2844 2.25 0.49 0.109 0.138 2.99 0.033 3.02 151 99

Bg 4462 4.30 0.75 0.077 0.154 5.28 0.013 5.29 106 100

BCg 6292 2.07 0.62 0.142 0.151 2.98 0.015 3.00 150 99

2Ck 92(109) 4.22 1.00 0.076 0.039 5.33 0.007 5.34 178 100


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P 2 Haic P(Laic)

L:WeKa ad, gacifia eace, ge ig 25, ak fe, 67 a...

N57295, E205210

O

A

AE

AEB

B

BC

2C

M:

60 c, deae deced gaicaeia;

010 c, hi, a ad, dakb (7.5YR 3/2), deae gaa caead e cae ce, ab ad abda;

1033 c, hi, a ad, edak gaih b (10YR 3/2), deaebaga bck edi ad cae ce, gada ad iega bda;

3353 c, ad a, e igh eih b (2.5Y 6/3), g bagabck e cae ce, gada adiega bda;

5394 c, i a, eih b (10YR5/6), g baga bck cae ade cae ce, c diic eiide caig, gada ad iegabda;

94124 c, ad, igh eih b(10YR 6/4), g iaic e cae ce, eie, ab ad hbda;

124(134) c, ae aeia, , ad ca, gaih b (10YR 5/2),eak baga bck cae ce, cdii, g cacae.

[c] 0

50

100


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T 4. T

HD[]

P [] T2.00.05 0.050.002 < 0.002

A 010 77 21 2 LS

AE 1033 76 22 2 LS

AEB 3353 65 33 2 SL

B 5394 48 50 2 SiL

BCg 94124 89 6 5 S

2Cgk 124(134) 50 8 42 SC

T 5. C

HD[]

OC[

1]

N[

1]

C/NHKC

CCO3[

1]

A3+ F2+ M2+

[1]

Oe 60 560 180.0 3 5.7 3.0 0.80 69.5

A 010 20.0 3.51 6 4.3 52.4 0.61 6.16

AE 1033 13.0 1.92 7 4.1 208 10.2 0.89

AEB 3353 2.00 0.43 5 4.8 51.0 2.30 1.06

B 5394 5.1 31.0 1.32 0.98

BCg 94124 5.4 10.3 2.60 2.49

2Cgk 124(134) 7.8 + 1.7 0.14 0.54

T 6. S

HD[]

C2+

M2+

K+

N+


1]

Oe 20 24.7 3.56 1.19 0.118 29.6 0.050 29.6 100

A 018 3.84 0.680 0.145 0.100 4.76 0.563 5.32 0 89

AE 1828 1.34 0.381 0.095 0.259 2.07 0.188 2.26 0 92

AEB 2844 1.01 0.234 0.031 0.034 1.31 0.033 1.34 32.0 98

B 4462 0.71 0.185 0.024 0.025 0.944 0.013 0.957 47.9 99

BCg 6292 2.27 0.566 0.052 0.028 2.92 0.015 2.94 58.8 99

2Cgk 92(109) 8.22 0.909 0.079 0.043 9.25 0.007 9.26 22.0 100


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P 3 Eic Sagic Gic R (Abic, Siic, Caic)L:Agee ad, gacigeic i hck, ig i 510%, ak fe,

178 a... N594857, E183010

O

A

EB

B

B

M:


022 c, ad a, b (10YR 5/3),d, deae gaa fie ad edice, cea ad a bda;

2237 c, aiia hi, i a,ae b (10YR 6/3), d, deae gaa fie ad edi ce, e

ie, cea ad iega bda;

3767 c, hi, ca a, b(7.5YR 5/4), igh i, g iaicedi ad cae ce, eie, edcig cdii, c diiceiide ad ca caig, diffe ada bda;

67(91) c, hi, i a, gb (7.5YR 4/6), igh i, g iaic edi ad cae ce, eie, edcig cdii, c

diic eiide ad ca caig, deae cacae.

90

[c] 0

50


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T 7. T

HD[]

P [] T2.00.05 0.050.002 < 0.002

Ah 022 46 49 5 SL

EBg 2237 19 62 19 SiL

Bg 3767 30 33 37 CL

Bgk 67 (91) 23 52 25 SiL

T 8. C

HD[]

OC[

1]

N[

1]

C/N H KCCCO3[

1]

A3+

F2+

M2+

[1

]

Oi 10 830 344 2 5.9 4.40 1.98 127

Ah 022 19.0 4.00 5 4.5 80.8 2.84 34.7

EBg 2237 4.5 87.7 0.67 4.31Bg 3767 5.6 1.6 0.87 6.51

Bgk 67 (91) 7.8 + 0.9 0.16 0.52

T 9. S

HD[]

C2+

M2+

K+

N+


1]

Oi 10 36.5 12.6 2.77 0.109 52.0 0.049 52.0 100

Ah 022 3.42 1.37 0.232 0.047 5.07 0.897 5.97 0.00 85

EBg 2237 3.14 1.75 0.094 0.046 5.03 0.975 6.01 31.6 84

Bg 3767 9.42 4.91 0.185 0.067 14.6 0.018 14.6 39.5 100

Bgk 67 (91) 9.82 3.48 0.125 0.053 13.5 0.010 13.5 54.0 100


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P 4 Edcacaic Edagic L(Laic, Caic, Heeic)L:WeKa ad, gacigeic i ai, e fa 0.20.5%, ak fe, 69.2 a...

N571426, E20376

O

A

AEB

B

B

B

C

M:


011 c, i a, dak gaih b(10YR 4/2), g baga bck fie adedi ce, cea ad a bda;

1125 c, i a, gaih b (10YR5/2), g aga bck edi adcae ce, e fe fai eiide

caig, gada ad iega bda;

2544 c, hi, i ca a,b (10YR 4/3), g baga adaga bck fie ad edi ce,c fai eiide caig, ceaad a bda;

4461 c, hi, i ca a,dak gaih b (10YR 4/2), g iaic edi ad cae ce, eie, edcig cdii, a diiccaeiide caig, cea ad a

bda; 6199 c, aeia, i ca a,dak gaih b (10YR 4/2), g iaic cae ce, eie,edcig cdii, a diic caeiide caig, gada ad iegabda;

99(110) c, aeia, aeaeia, i ca a, (GL15/10Y), eakiaic edi ad cae ce, fefai eiide caig, eee cacae.

[c] 0

50

100


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T 10. T

HD[]

P [] T2.00.05 0.050.002 < 0.002

Ah 011 2 82 16 SiL

AhEB 1125 12 63 25 SiL

B 2544 5 62 33 SiCL

Bg 4461 0 67 33 SiCL

Bgk 6199 2 72 26 SiCL

Ck 99(110) 1 63 36 SiCL

T 11. C

HD[]

OC[

1]

N[

1]

C/N H KCCCO3[

1]

A3+

F2+

M2+

[1

]

Oi 10 222 13.4 17 5.3 6.40 1.50 158

Ah 011 21.0 4.5 5 4.3 168 0.32 21.5

AhEB 1125 9.00 1.8 5 4.8 69.9 0.84 19.5

B 2544 5.7 1.40 0.45 4.61

Bg 4461 7.0 1.20 0.39 1.28

Bgk 6199 7.7 + 0.60 0.10 0.60

Ck 99(110) 7.9 + 1.40 0.09 0.66

T 12. S

HD[]

C2+

M2+

K+

N+


1]

Oi 10 35.0 11.8 2.43 0.148 49.4 0.072 49.5 100

Ah 011 4.74 1.89 0.32 0.298 7.25 1.872 9.12 11.1 79

AhEB 1125 6.07 2.49 0.188 0.090 8.84 0.776 9.62 25.9 92

B 2544 15.3 5.77 0.181 0.134 21.4 0.016 21.4 64.8 100

Bg 4461 17.3 6.83 0.155 0.131 24.4 0.014 24.4 73.9 100

Bgk 6199 16.2 3.74 0.158 0.103 20.2 0.007 20.2 77.7 100

Ck 99(110) 13.8 3.82 0.180 0.132 17.9 0.015 17.9 49.7 100


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F. 2. C Q

L


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Influence of environmental factors on soil genesis and propertiesInfluence of environmental factors on soil genesis and propertiesInfluence of environmental factors on soil genesis and propertiesInfluence of environmental factors on soil genesis and propertiesQuaternary deposits, their granulometric and chemical composition have the strongest bearing on thespatial distribution of soil groups (according to FAO WRB classification (2014)) in Latvia. Further-more, soil texture is the most important factor determining the forest soil diversity in the Late Weich-selian glacial deposits and Holocene sediments (Kasparinskis, Nikodemus, 2012), and soil processes

(e.g. accumulation of organic matter, podzolization and lessivage) may also be affected by differentland-use changes (Nikodemus et al., 2013). Large-scale afforestation measures have been targeted atplanting secondary Q. roburforests on former agricultural lands, and most of the Q. roburforest areasin many European countries are distributed on former agricultural lands (Brunet et al., 2011).

The most common soil groups in the Q. roburstands in Latvia are LuvisolsLuvisolsLuvisolsLuvisols (Ikauniece et al., 2013).Glaciolacustrine, glaciofluvial and glacigenic deposits (glacial till) are distributed on a relatively largearea in Latvia (Fig. 1). The conceptual model of the soil lithosequencelithosequencelithosequencelithosequence (Fig. 2) on Quaternary depositsunder Quercus robur L.stands in Latvia shows the occurrence of Phaeozems on glaciolacustrine andglaciofluvial deposits formed by sandy material, but an increase in the clay content leads to the occur-rence of Retisols in glacial tills related to an undulated topography, as well as Luvisols in glacial till

plains. The range of soil groups in the Q. roburstands indicates a fairly wide edaphic niche, which istypical in its range (Jones, 1959).

Previous studies of forest soils in Latvia according to FAO WRB (2007) showed a close correlationbetween Quaternary deposits, forest site types, dominant tree species and soil groups within nutrient-poor sandy sediments (e.g. ArenosolsArenosolsArenosolsArenosols) and very rich deposits containing a relatively high content ofclay, silt and free carbonates (e.g. LuvisolsLuvisolsLuvisolsLuvisols and AlbeluvisolsAlbeluvisolsAlbeluvisolsAlbeluvisols) (Kasparinskis and Nikodemus, 2012).Previous studies in Latvia indicated that mixed Q. roburstands with larger cover of the boreal conifersP. abiesand P. sylvestrisoccurred on mesic habitats with a higher silt content. A typical nemoral herblayer with greater proportion of ant-dispersed species and hemicryptophytes was associated with soilsthat had a higher clay content (Ikauniece et al., 2013).

Typical features of the soils in this study include: reducing conditions, weakly expressed stagnicproperties, free carbonates and relatively high base saturation (>50%) (Profiles 14).

Reducing conditions and stagnicproperties were observed at a depth of 92 cm in Profile 1; in Pro-file 2, however, this is related to an increase in the clay content in subsoil ( Table 4). Reducing condi-tions and stagnicproperties were detected closer to the soil surface in the glacigenic till hummock(Profile 3) and the glacigenic till plain (Profile 4) where surface water filtration is disturbed by a rela-tively heavy soil texture (silt loam, clay loam and silty clay loam), resulting in stagnicandgleyicprop-erties that morphologically indicate StagnicStagnicStagnicStagnic and EndostagnicEndostagnicEndostagnicEndostagnic qualifiers.

Free carbonates and relatively high base saturation (>50%) are provided by soil parent material re-sulting in EutricEutricEutricEutric and HypereutricHypereutricHypereutricHypereutric qualifiers. Free carbonates and relatively high base saturation(>50%) were detected in deeper horizons of PhaeozemsPhaeozemsPhaeozemsPhaeozems (Profiles 1, 2) i.e. at a depth of 92 cm and124 cm than in RetisolRetisolRetisolRetisol (Profile 3) and LuvisolLuvisolLuvisolLuvisol (Profile 4) 67 cm and 99 cm, respectively.

pHpHpHpHKClKClKClKClof the mineral soilsoilsoilsoil ranges from 4.1 to 7.9 in the studied soil profiles (14) (Table 2, 5, 8, 11).Lower pHKClvalues are detected in the mineral topsoil layers, thus indicating the edaphic role of oakQ. roburstands and possible initialization of the podzolization process (increase in exchangeable Al3+concentration) (Profile 14, Table 2, 5, 8, 11).

Cation exchange capacityCation exchange capacityCation exchange capacityCation exchange capacity varies from 5.3 to 11.2 [cmol(+)kg-1] in mineral topsoil, in the O hori-zon from 29.6 to 52.0 [cmol(+)kg-1] (Table 3, 6, 9, 12). These results showed that cation exchangecapacity is higher in the O horizon of RetisolRetisolRetisolRetisol (Profile 3) in the glacigenic till hummock and LuvisolLuvisolLuvisolLuvisol(Profile 4) in the glacigenic till plain. These properties in the topsoil could be explained by the influ-ence of the root system and litter of oak Q. roburstands.


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Depth of the organic matter accumulation horizon in mineral topsoil ranges between 28 cm (Pro-file 1 Ah and AEh horizons) and 33 cm (Profile 2 A and AE horizons) in glaciolacustrine andglaciofluvial deposits, to 22 cm (Profile 3 Ah horizon) and 11 cm (Profile 4 Ah horizon) in theglacigenic till hummock and the glacigenic till plain. This shows that the development of the organicmatter accumulation horizon is disturbed in relatively heavy soils (silt loam, clay loam and silty clay

loam).Organic carbon content varies from 19 to 22 [gkg -1] in mineral topsoil in all the studied soil pro-

files, however the highest content is detected in the O horizon (from 830 [gkg-1] in RetisolRetisolRetisolRetisol formed onthe glacigenic till hummock (Profile 3, Table 8) to 222 [gkg-1] in LuvisolsLuvisolsLuvisolsLuvisols formed on the galcigenic tillplain (Profile 4, Table 11).

ReferencesReferencesReferencesReferences

Brunet, J., Falkengren-Grerup, U., Rhling, ., Tyler, G., 1997. Regional differences in floristic change in SouthSwedish oak forests as related to soil chemistry and land use. J. Veg. Sci. 8. 329336.

Geological map of Latvia, scale 1 : 500 000. 1981. State Geological Survey. Rga. Available: kartes.geo.lu.lv (inLatvian).

Hytteborn, H., Maslov, A.A., Nazimova, O.J., Rysin, L.P., 2005. Boreal forests of Eurasia. In: Andersson, F. (Ed.),Ecosystems of the World 6: Coniferous Forests. Elsevier, Amsterdam, The Netherlands. 2399.

Ikauniece, S., Brmelis, G., Kasparinskis, R., Nikodemus, O., Straupe, I., Zari, J. 2013. Effect of soil and canopyfactors on vegetation of Quercus robur woodland in the boreo-nemoral zone: A plant-trait based approach. ForestEcology and Management. 295, 4350.

IUSS Working Group, 2007. World Reference Base for Soil Resources 2006, first update 2007. World SoilResources Reports 103. FAO, Rome. 103116.

IUSS Working Group WRB, 2014. World Reference Base for soil resources 2014. International soil classificationsystem for naming soils and creating legends for soil maps. World Soil Resources Report No. 106. FAO, Rome.

Jones, E.W., 1959. Quercus L. J. Ecol. 47, 169222.

Kasparinskis, R., Nikodemus, O., 2012. Influence of environmental factors on the spatial distribution anddiversity of forest soil in Latvia. Estonian Journal of Earth Sciences. 61(1), 4864.

Krampis, I., 2010. Regional distribution of boreal and nemoral biome tree plants in Latvia. Doctoral thesis. Uni-versity of Latvia, Faculty of Geography and Earth sciences. Rga. (In Latvian).

Krauklis, ., Zaria, A., 2002. Parastais skbardis sava arela ziemeu robeas ainav Latvij. eogrfiski rakstiFolia Geographica. Latvijas eogrfijas biedrba, 10, 1647.

Nikodemus, O., Kasparinskis, R., Kukuls, I., 2013. Influence of Afforestation on Soil Genesis, Morphology andProperties in Glacial Till Deposits. Archives of Agronomy and Soil Science. 59(3), 449465.

Ozenda, P., 1994. Vgtation du Continent Europen. Delachaux et Niestl, Lausanne, Swizerland.

Sjrs, H., 1963.Amphi-Atlantic zonation, nemoral to Arctic. North Atlantic biota and their history. The Macmil-lan Company, New York. 109125.

State Forest Service, 2008. Forest statistics 2007 (MS Excel spreadsheets), CD ROM.


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Forested areas within sandy lowlands and continentaldunes of South-Eastern LithuaniaRimantas Vaisvalaviius, Jonas Volungeviius, Vanda Buivydait

The territory of South-Eastern Lithu-ania lies on the north-western edgeof the East European plain (Soil Atlasof Europe, 2005). Its landscape hasbeen smoothed by edge deposits ofthe Medininkai and Nemunas Glaci-ations (Fig. 1). The southern Lithua-

nian glaciation edge deposits stretchas a wide strip along the western edgeof Auktaii and the northern edgeof Sduva Upland. The largest areasof South-Eastern Lithuania are occu-pied by glaciofluvial and glaciolacus-trine formations (Eidukeviien andVasiliauskien, 2001).

Lithology and topographyLithology and topographyLithology and topographyLithology and topography

The presented soils are located in Dzkijos dune hills and Ula-Katra glaciolacustrine plain areas of theDainava glaciofluvial lowland (Guobyt, 2010). In terms of age, this is a fairly homogeneous territoryassociated with the Nemunas Glaciation Grda phase formations (17,000 to 19,000 years old). Alt-hough the territory is covered by the same soil parent material of genetic origin, the diversity of itsrelief (abs. altitude 122147 m) is largely associated with the epigenetic surface (aeolian processes)transformation and anthropogenic influences.

Land useLand useLand useLand useThe majority of areas within the Dainava glaciofluvial lowland are covered with coniferous forests.The canopy layer is dominated by pine (Pinus sylvestris) and spruce (Picea abies). Because of the rela-tively low soil fertility, only the vast minority of lands are nowadays used for agricultural purposes.

ClimateClimateClimateClimateThe climate of South East Lithuania, which ranges between maritime and continental, is relativelymild. Average annual air temperature is +6.2 C. Compared to other regions of Lithuania, however,the local climate is characterized by much larger seasonal temperature contrasts. Usually the wind isblowing unevenly but in gusts (Galvonait, 2013). Westerlies and south-westerlies dominate in thearea throughout the year. The average annual amount of precipitation is 673 mm. Although theamount of precipitation can vary a lot in different years, the highest monthly amount occurs in Julyand August. Average annual relative humidity in the area does not vary much (from 80 to 81%).

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P 1 Dic Pic A (Aeic) e Bic AL: Daiaa gacifia ad, back e, ie ce

N 5357'293", E02423'060"

O

A

B1

B2

B3

BC

A

B1

B2

M:


08 c, h hi, fie ad, back(10YR 2/1), igh i, eak gaa fiece, fie ad edi c ,cea ad a bda;

817 c, fie ad, eddih e (7.5YR6/6), igh i, eak gaa e fie/ige gai ce, cae fe ,gada ad h bda;

1731 c, fie ad, igh b (7.5YR 6/4),igh i, ige gai ce, cea adh bda;

3145 c, fie ad, igh b (7.5YR 6/3),igh i, ige gai ce, cea adh bda;

4570 c, aiia hi, fie ad,igh b (7.5YR 6/3), igh i, igegai ce, ab ad a bda;

7081 c, bied h hi, fie ad,e dak ga (7.5YR 3/1), igh i,eak gaa fie ce, fie fe ,ab ad a bda;

8194 c, fie ad, g b (7.5YR5/8), igh i, ige gai ce,gada ad h bda;

94(100/120) c, fie ad, eddih e(7.5YR 6/8), igh i, ige gai ce.

[c] 0

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100


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T 1. T

HD[]

P []T

2.01.0

1.00.5

0.50.25

0.250.106

0.1060.053

0.0530.038

0.0380.002


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P 2Bahihegeic Fic Abic P (Aeic)L: Daiaa gacifia ad, f e, ie ce,

N 5357'21.3", E02422'47.6"

O

AE

E

B

B

B

B

B

M:


015 c, h hi ih feae feiai ce, fie ad, ga (10YR 5/1),igh i, eak gaa fie ce,fie ad edi c , gada adh bda;

1523 c, eia hi ih aeia, fie ad, hie (10YR 8/1), igh i,ige gai ce, cea ad hbda;

2351 c, iia hi, fie ad, eddihe (7.5YR 6/8), igh i, ige gaice, edi e fe i eeci, cea ad h bda;

5167 c, hi, fie ad, eddihb (5YR 5/3), i, ige gai ce,cea ad h bda;

6781 c, hi, fie ad, e

dak ga (5YR 3/1), i, ige gai ce, a eak ceeed b iagaeeeiide, a ihic e, ceaad h bda;

7080 c, hi, fie ad, back(5YR 2.5/1), i, ige gai ce, adeae ceeed b iagaeeeiide, a ihic e, ceaad h bda;

81103/110 c, fie ad, dak eddihb (5YR 2.5/2), e, ige gai ce,a eak ceeed b iagaee

eiide, ihic cdii.

[c] 0

50

100


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T 3. T

HD[]

P []T

2.01.0

1.00.5

0.50.25

0.250.106

0.1060.053

0.0530.038

0.0380.002


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P 3 Fic Abic P (Aeic)L: Daiaa gacifia ad, e e (hde), ie ce,

N 5357'22.8", E02422'44.1"

O

AE

E

B1

B2

B3

BC

M:


026 c, h hi ih feae feiai ce, fie ad, ga (7.5YR 5/1),igh i, eak gaa fie ce,fie ad edi e fe , cea adh bda;

2641 c, eia hi ih aeia, fie ad, igh ga (7.5YR 7/1), ighi, ige gai ce, edi e fe, cea ad h bda;

4149 c, hi, fie ad, eih ed (5YR 5/6), igh i, ige gaice, edi e fe , gada adh bda;

4969 c, fie ad, eddih e(5YR 6/6), igh i, ige gai ce,fie e fe , gada ad hbda;

6998 c, fie ad, eddih e(5YR 7/6), igh i, ige gai ce,gada ad h bda;

98109 c, aiia hi, fie ad,ikih ga (7.5YR 7/2), igh i, igegai ce.

[c] 0

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100


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T 6. T

HD[]

P []T

2.01.0

1.00.5

0.50.25

0.250.106

0.1060.053

0.0530.038

0.0380.002


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P 4 Geic Hiic Abic P (Aeic)L: Daiaa gacifia ad, f e, ce ce,

N 5357'32.9", E02419'16.1"

O

A

AE

E

B

B

2C

M:


08 c, h hi, a fie ad,back (10YR 2/1), igh i, eak gaafie ce, fie ad edi fe ,cea ad h bda;

817 c, h hi ih feae feiai ce, a fie ad, ga(10YR 5/1), igh i, eak gaa fie/ige gai ce, edi e fe, gada ad h bda;

1738 c, eia hi ih aeia, fie ad, igh ga (10YR 7/2), ighi, ige gai ce, cea ad abda;

3849 c, hi, fie ad, b(7.5YR 5/2), i, ige gai ce,g idai, fie e fe , ceaad a bda;

4953 c, hi, fie ad, eih ed (5YR 4/6), i, ige gai ce, a eak ceeed b iagaee eiide, cea ad hbda;

5375/110 c, fie ad, igh ga (5Y 7/2),e, ige gai ce, g edcigcdii.

[c] 0

50


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T 8. T

HD

[]

P []T

2.01.0

1.00.5

0.50.25

0.250.106

0.1060.053

0.0530.038

0.0380.002


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P 5 Dic Daiic HeicHL: Daiaa gacifia ad, ai deei ih bigeic dei,

N535711,51, E241903,68

O

H

H1

H2

H3

2C

M:


515 c, hi, high decedgaic aeia, back (10YR 2/1), i,eak gaa fie ce, fie c, cea ad a bda;

1525 c, hi, deae deced gaic aeia, back (10YR 2/1),i, eak gaa fie ce, fie fe, cea ad h bda;

2550 c, hi, deae deced gaic aeia, back (10YR 2/1),e, eak gaa fie/ aie ce,fie e fe , cea ad h bda;

5070 c, hi, deae deced gaic aeia, back (10YR 2/1),e, aie ce, fie e fe ,cea ad h bda;

7085/120 c, fie ad, igh ga (5Y 7/2),e, ige gai ce, g edcigcdii.

[c] 0

50


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T 10. T

HD[]

P []T

2.01.0

1.00.5

0.50.25

0.250.106

0.1060.053

0.0530.038

0.0380.002


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F.2.H

SEL


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Soil genesis and systematic positionSoil genesis and systematic positionSoil genesis and systematic positionSoil genesis and systematic position

The common feature of the south-eastern Lithuanian sandy lowlands is the extensive occurrence ofArenosolsand Podzolscharacteristic soils of the region (Motuzas et al., 2009). According toWRB2014 (IUSS Working Group, 2014),Arenosolscomprise sandy soils, including both soils developed inresidual sands after in situ weathering of usually quartz-rich sediments or rock, and soils developed inrecently deposited sands (such as dunes and beach lands). According to the same WRB system, Pod-zolsare soils with a typically ash-grey upper subsurface horizon, bleached by the loss of organic matterand iron oxides, on the top of a dark accumulation horizon with brown, reddish or black illuviatedhumus and/or reddish Fe compounds.The predominance of Arenosols and Podzols in the studied area is determined by the abundance ofsandy sediments (massifs of the continental aeolian sand dunes) covered with the forest stands. Threeof five soil profiles were excavated in places with complex, but at the same time consistent soil struc-ture that formed on the continental sand dunes. On the other hand, it was done in order to highlightboth a genetic relationship between Arenosols and Podzols and the increasing problems with theirclassification in Lithuania (Vaisvalaviius et al., 2013). Primarily, there are different patterns in theformation of these soils depending on the exposition and on the slope of sandy dunes. It is obviousthat the inhibited process of soil formation, and hence rather poorly developed soils occur on thesouthern slopes of the dunes due to microclimates that are much warmer compared to the northernslopes.In addition, due to the south-eastern/southern axis of the dunes, intensive deflation processesoccurred in this area (even today in some isolated smaller sections) and layered soil profiles (buriedsoils) developed. Dystric ProticDystric ProticDystric ProticDystric ProticArenosolArenosolArenosolArenosol (Aeolic) over BrunicBrunicBrunicBrunicArenosolArenosolArenosolArenosol (Profile 1) with some weak-ly expressed features of the podzolization process is a characteristic example of such soil formationconditions on the local sands. The northern slopes of the dunes, particularly covered with old, matureand even premature forest stands, have deeper and much more strongly developed soil profiles. In

general, while receiving a smaller amount of heat and at the same time having a higher moisture con-tent, the soils undergo rather intensive formation processes. Folic AlbicFolic AlbicFolic AlbicFolic AlbicPodzolPodzolPodzolPodzol (Arenic)(Arenic)(Arenic)(Arenic)(Profile 3)are a significant example of such soil formation conditions. However, deeper spots between dunes arecovered either with high moor soils (FibricFibricFibricFibric HistosolsHistosolsHistosolsHistosols) or Bathihypergleyic Folic AlbicBathihypergleyic Folic AlbicBathihypergleyic Folic AlbicBathihypergleyic Folic Albic PodzolPodzolPodzolPodzol(Arenic)(Arenic)(Arenic)(Arenic)formed just on the footsteps of the dunes (Profile 2).The place for the fourth profile was selected on the outskirts of the glaciolacustrine basin near thevillage of Kabeliai (Fig. 1). The soil here was classified as Gleyic Histic AlbicGleyic Histic AlbicGleyic Histic AlbicGleyic Histic AlbicPodzolPodzolPodzolPodzol (Arenic)(Arenic)(Arenic)(Arenic) (Profile4). It well represents soils that have formed from aleurite sands on the glaciolacustrine plains underthe conditions of wooded marshy landscape.The central part of the glaciolacustrine basin is represented by Dystric Drainic HemicDystric Drainic HemicDystric Drainic HemicDystric Drainic HemicHistosolHistosolHistosolHistosol(Pro-

file 5). In the former wetlands (marshes), the deposits of organogenic origin occur directly on theshallow aleuritic sand sediments in the glaciolacustrine basin. However, the former wetlands havebeen intensively drained in the second half of the twenty century, thus the current Histosols arestrongly mineralized.

Soil sequenceSoil sequenceSoil sequenceSoil sequence

All presented soils are characterized by rather similar lithogenesis. They are developed from glaciola-custrine deposits covered by eolian material. The main differences responsible for different directionsof soil-forming processes are associated with the topography and the influence of ground water. Thespatial arrangement of pedons represent a typical hydrohydrohydrohydro----topotopotopotoposequencesequencesequencesequence. The slopes and the middleparts of dunes are covered by automorphic soils (Dystric Arenosolsand Albic Podzols), developed innon-carbonaceous sands. In the lower parts of the dunes or depressions between dunes, the hydro-


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morphic soils occur (Gleyic Podzolsand Histosols). Although slightly eroded soils are quite common(16.6%) in the sandy south-eastern plain (Buivydait, 1999), nowadays the coniferous forest standswith some admixture of birch and alder species protect soils within the studied area against the ero-sion. This is the case even on steep slopes, as it has been observed in the undulating hilly topographyof the emaiiai Uplands in Western Lithuania (Jankauskas and Fullen, 2002).


Buivydait, V., Vaiys, M., 1996. Conformation of soil classification of Lithuania to the World Soil Map legend.Geografija T. 32: Vilnius. 4357 (in Lithuanian with English summary).

Buivydait, V., 1999. Soil survey and available soil data in Lithuania.In: Bullock, P., Jones, R.J.A. and Montana-rella L. (Eds.), Soil Resources of Europe. Office for Official Publications of the European Communities, Luxem-bourg. 211223.

IUSS Working Group WRB, 2014. World Reference Base for soil resources 2014. International soil classificationsystem for naming soils and creating legends for soil maps. World Soil Resources Report No. 106. FAO, Rome.

Jankauskas, B., Fullen, M.A., 2002. A pedological investigation of soil erosion severity on undulating land in Lith-uania. Can. J. Soil Sci. 82, 311321.

Galvonait, A. (Eds.), 2013. Climate Atlas of Lithuania. Vilnius, 175 p. (in Lithuanian and English).

Guobyt, R. 2010. Geomorphological areas and districts. Nature of Lithuania.Vilnius, 1618.

Eidukeviien, M., Vasiliauskien V. (Eds.), 2001. Lithuanian Soils. Science and Arts in Lithuania, Vilnius,1244 p. (in Lithuanian with English summary).

Eidukeviien, M., 2009. Geography of Lithuanian Environment.Klaipda, 162 p. (in Lithuanian).

Motuzas, A.J., Buivydait, V.V., Vaisvalaviius, R., leinys, R.A., 2009. Soil Science,Vilnius: Enciklopedija, 335 p.

(in Lithuanian).

Mavila, J., Vaiys, M., Buivydait, V., 2006. Macromorphological diagnostics of Lithuanian Soils. Akademija(Kdaini r.): Lithuanian Institute of Agriculture. 283 p. (in Lithuanian with English summary).

Mavila, J. (Eds.), 2011. The productivity of Lithuanian lands. Lithuanian Research Centre for Agriculture andForestry, Akademija, Kdaini r., 280 p. (in Lithuanian with English summary).

Soil Atlas of Europe, 2005. European Soil Bureau Network European Commission. Office for Official Publica-tions of the European Communities, L-2995 Luxembourg. 128 p.

Vaisvalaviius, R., Volungeviius, J., Eidukeviien, M., Motuzas, A., 2013. The characteristics of soil cover inDainava plain. Akademija. 31 p. (in Lithuanian).


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Flat coastal plain of the Hel Peninsula(Puck Lagoon, Poland)Piotr Hulisz

The Puck Lagoon is a north-western subregion of GdaskBay (Northern Poland), separated from the waters of PuckBay by a partly submerged sandy barrier (Rybitwia Mielizna Seagull Shallows). The Hel Peninsula constitutes a border-line with the open waters of the Baltic Sea (Fig.1).

Lithology and topographyLithology and topographyLithology and topographyLithology and topographyThe Hel Peninsula is a narrow, 36 km long spit. Its widthranges from ca. 200 m to 3 km. The Holocene series of de-posits are fully developed only in the eastern part of thePeninsula where its thickness reaches 100 m. In the westernpart there are Holocene deposits only of the Littorina peri-od, forming a relatively thin cover of 1012 m thickness(Tomczak, 1994). On the surface, there are marine and aeolian sands. The shores are mostly destroyedduring storm surges. Sometimes, the inflow of seawaters from the open Baltic Sea into the Puck La-goon is also observed (Wrblewski, 2008). Three soil profiles representing the coastal soils of thewestern part of the Hel Peninsula (Wadysawowo) were selected (Hulisz, 2013). The first one was

located in the small wetland depression, the second one on the beach ridge and the third one with-in a very narrow beach zone. The analysed section of the seashore is very flat (the altitude do not ex-ceed 1 m a.s.l.).

Hydrology and climateHydrology and climateHydrology and climateHydrology and climateThe coastal zone is affected mainly by the water level in Puck Lagoon, with the average annual value of502 cm for the period of 19512000. Extreme deviations from the mean sea level range from +1.5 to-1.0 m. Minimum values occur in March and April, and the maximum during the autumn and win-ter storms (XIII). The water salinity is on average ca. 7.07.5 (Majewski and Lauer, 1994). Theregion is located in the warm temperate, fully humid climate zone with warm summer (Kottek et al.,2006). The average annual air temperature for the period 19712000 is 8.7C and the average annual

precipitation is 515 mm (Filipiak et al., 2004). Winds from SW, W and NW directions prevail in theLagoon. Strong winds (above 10 ms-1) occur for ca. 70 days a year (Kwiecie, 1990).

VegeVegeVegeVegetationtationtationtationThe presented soils constituted an integral part of the unique habitats protected within the Natura2000 network, including the dominant Atlantic salt meadows Glauco-Puccinellietalia, code 1330(Herbich, 2004). In the surroundings of the soil profiles, two plant communities dominated, i.e. therush community with Schoenoplectus tabernaemontaniand Bolboschoenus maritimus(Profile 1 and 3)and saline meadow withJuncus gerardi(Profile 2). The former was characterized by a relatively highcontribution of Phragmites australis. The rare occurrence of halophytes such as: Atriplex prostrata

ssp.prostrata var.salina, Aster tripolium, Spergularia salina, Glaux maritimaand Triglochin mariti-mumwas observed in all locations.

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P 1 Fic G(Aeic, Hic, Paic, Sdic)L:Wada, Pck Lag, He Peia, Pad, fa caa ai (beach), h c

i f ad , 0.1 a...,

N544714.2, E182539.1

C1

H

C2

M:

aeia: 02.5 c, eie, edi adih agae ca; geeih ga (10Y 5/1), e,ige gai ce, fe he, cedcihic e;

2.59 c, accai f achhgaic ae, back (10YR 2/1), e fehe;

9(20) c, eie, edi ad,geeih ga (10GY 6/1), e, ige gaice, fie ad edi c ,c edcihic e.

[c] 0

20


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T 1. P

HD[]

M[% /]

H HE

[V]H

SO42

C

[100 1

]

C1 02.5 21.5 7.3 4.7 291 24 13.8 49.6

Hi 2.59 490 7.1 4.4 237 22 340 1100

C2 9(20) 27.6 7.4 4.5 272 24 14.9 62.9

T 2. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

< 0.002

C1 02.5 0 1 18 74 7 0 0 0 0 0 MS

C2 9(20) 0 2 31 63 4 0 0 0 0 0 MS

T 3. C

HD[]

OC[

1]

N[

1]

S[

1]

C/N C/SH CCO3

[%]H2O KC

C1 02.5 1.9 0.3 0.2 7 12 7.1 6.6 0.2

Hi 2.59 253 20.2 7.2 13 35 6.9 6.4 2.1

C2 9(20) 1.5 0.1 0.1 12 12 7.4 6.7 0.2

T 4. P

HD[]

H EC

[S1]

SP[%]

S [%]1

SARESP

2

[%]

C1 02.5 7.0 9.63 25.3 0.62 0.16 18 20

Hi 2.59 7.3 11.0 498 0.70 3.51 21 23

C2 9(20) 7.5 9.14 26.6 0.58 0.16 20 22

1cacai accdig Si Se Laba Saff (1996):

a ce i eac = 0.064 ECe

a ce i i = 0.064 ECe SP/1002

eiaed f SAR (a Reeijk, 2002)


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P 2 Fic G(Aeic, Hic, Paic, Sdic)L: Wada, Pck Lag, He Peia, Pad, fa caa ai (beach idge), aie

ead ih , 0.4 a..., N544714.6, E182539.2

A

A/C

A

C

C

C

M:

06 c, h hi, edi ad; dakgaih b (10YR 3/1), i, ige gaice, e fie ad fie c ;

aeia:

616 c, aeed i aeia, edi adad d, deae deced gaicaeia, i, e fie ad fie c;

1623 c, accai f achhgaic ae (high deced ea add), adie f ad, back (10YR 2/1),i;

2328 c, edi ad, igh b (10YR 6/3),i, ige gai ce;

2831 c, accai f achhgaic ae, edi ad, gaih b(2.5Y 5/2), i, ige gai ce;

be 31 c, eie, ediad, igh geeih ga (10Y 8/1), e, ige

gai ce, c edcihice.

[c] 0

50


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41

T 5. P

HD[]

M[% /]

H HE

[V]H

SO42

C

[100 1

]

Ah 06 64.6 7.2 4.8 433 29 59.7 96.4

A/C 616 27.3 7.2 4.8 364 27 28.5 89.0

Ah 1623 104 6.7 4.4 115 17 71.5 170

C 2328 14.1 6.7 4.3 309 24 27.3 23.2

Ch 2831 53.2 6.6 4.4 391 26 9.90 38.9

C >31 16.0 7.2 4.5 237 22 5.50 27.9

T 6. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

31 0 2 15 73 10 0 0 0 0 0 MS

T 7. C

HD[]

OC[

1]

N[

1]

S[

1]

C/N C/SH

H2O KC

Ah 06 68.6 5.4 1.3 13 52 7.1 5.8

A/C 616 19.7 1.6 0.4 12 51 7.2 6.0

Ah 1623 94.9 7.5 2.4 13 39 6.6 5.5

C 2328 1.2 0.1 0.2 6 12 6.7 5.6

Ch 2831 21.1 1.9 0.4 11 53 6.5 5.4

C >31 1.0 0.1 0.1 10 15 7.1 6.0

T 8. P

HD[]

H EC

[S1

]SP[%]

S [%]1

SARESP

2

[%]

Ah 06 7.2 2.18 89.4 0.14 0.12 14 16

A/C 616 7.3 2.55 54.3 0.16 0.09 14 16

Ah 1623 6.9 5.35 113 0.34 0.39 21 23

C 2328 7.0 2.71 30.5 0.17 0.05 11 13

Ch 2831 6.5 3.85 54.8 0.25 0.08 15 17

C >31 7.4 3.21 25.9 0.21 0.05 12 14

1cacai accdig Si Se Laba Saff (1996):


a ce i i = 0.064 ECe SP/1002eiaed f SAR (a Reeijk, 2002)


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42

P 3 HiicG (Aeic, Paic, Sdic, Hefidic)L: Wada, Pck Lag, He Peia, Pad, fa caa ai (a ead dee

i), h ci ih ad ,

0.3 a..., N544714.5,E182541.1

H

H

C

M:

06 c, aeia, high deced ea (aic), dd, dakgaih b (10YR 3/2), e, fie ad edi c ;

630 c, hi, igh deced ea (fibic), dd, b(10YR 4/3), e e, e fie ad e fe

; be 30 c, eie, aeia, edi ad, geeih ga (10Y 5/1),e e, ige gai ce, c edcihic e.

[c] 0

25


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43

T 9. P

HD[]

M[% /]

H HE

[V]H

SO42

C

[100 1

]

Ha 06 547 6.3 4.2 85 15 379 1040

Hi 630 295 6.0 1.6 20 13 487 530

C >30 20.8 6.2 1.5 15 13 38.6 56.6

T 10. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

< 0.002

C >30 1 2 14 60 20 2 2 0 0 0 MS

T 11. C

H D[]

OC[1]

N[1]

S[1]

C/N C/S H

H2O KC

Ha 06 339 241 116 14 29 6.3 5.3

Hi 630 237 160 156 15 15 4.7 4.2

C >30 2.5 0.2 0.4 11 7 3.9 3.4

T 12. P

HD[]

H EC

[S1

]SP[%]

S [%]1

SARESP

2

[%]

Ha 06 5.3 16.5 552 1.04 5.83 24 25Hi 630 4.5 11.8 301 0.76 2.27 15 17

C >30 3.4 6.52 25.2 0.42 0.11 10 12

1 cacai accdig Si Se Laba Saff (1996):


a ce i i = 0.064 ECe SP/1002eiaed f SAR (a Reeijk, 2002)


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44

F.2.H(HP

,PL,P)


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Piotr Hulisz

45

Soil genesis and systematic positionSoil genesis and systematic positionSoil genesis and systematic positionSoil genesis and systematic position

Coastal marsh soils in the Baltic zone have unique characteristics that result mainly from a brackishand heterogeneous salinity gradient of waters, climate conditions, land relief and minimal tides(Dijkema, 1990; Majewski and Lauer, 1994; Feistel et al., 2010; Hulisz, 2013). The presented soils arevery shallow (up to several tens of cm) and affected both by surface and ground water (gleyicproper-ties). They developed from stratified deposits (fluvic material Profiles 12), which reflected thechanging conditions of mineral and organic matter sedimentation (both geogenetic and pedogeneticprocesses). Accumulation of soil organic matter in those soils could have occurred in different envi-ronments: autochthonous (histichorizon Profile 3) and allochthonous (HumicHumicHumicHumicsupplementary qual-ifier Profiles 12). The rate and the nature of soil formation processes was dependent on landscapepositions. The soil located along the beach stretch (within the zone of the most dynamic seawater Profile 1) was defined as an initial soil. The others were classified as semi-mature (Hulisz et al., 2012;Hulisz, 2013).

The salinity (ECe 6.516.5 dSm-1) and sodicity level (ESP 1225%) of the analysed soils reflectedthe brackish nature of the Baltic waters (ProtosalicProtosalicProtosalicProtosalicand SodicSodicSodicSodicsupplementary qualifiers). It was alsosignificantly affected by other environmental factors (i.a. distance from the sea, seawater floodingfrequency, microrelief) and basic soil properties (texture and the content of organic matter). The rela-tively large differences between pH values measured in Profile 3 (Hinz and Cgz horizons): (i) underfield conditions (pHa), (ii) after two months of incubation of samples and (iii) after treatment withH2O2can suggest that this soil is particularly susceptible to acidification (hypersulfidicmaterial).

According to the WRB system (IUSS Working Group WRB, 2014), the studied coastal soils wereclassified as follows: Profiles 1 and 2 FluvicFluvicFluvicFluvic GleysolGleysolGleysolGleysol (Arenic, Humic, Protosalic, Sodic)(Arenic, Humic, Protosalic, Sodic)(Arenic, Humic, Protosalic, Sodic)(Arenic, Humic, Protosalic, Sodic), Profile 3HisticHisticHisticHisticGleysolGleysolGleysolGleysol (Arenic, Protosalic, Sodic, Hypersulfidic)(Arenic, Protosalic, Sodic, Hypersulfidic)(Arenic, Protosalic, Sodic, Hypersulfidic)(Arenic, Protosalic, Sodic, Hypersulfidic).

Soil sequenceSoil sequenceSoil sequenceSoil sequence

The analysed soils were characterized by small-scale diversity of morphology and other properties,depending on local geomorphological and hydrological conditions. They presented a specific spatialdistribution pattern within the selected transect, which can be referred to as a hydrohydrohydrohydro----toposequencetoposequencetoposequencetoposequence.The narrow section of the beach and the beach ridge are covered by FluvicFluvicFluvicFluvic GGGGleysols,leysols,leysols,leysols, while HisticHisticHisticHisticGleysolsGleysolsGleysolsGleysols can be found in the small depression farthest from the waterline (3040 m) Fig. 2. Sucha spatial arrangement of pedons is typical of soils in the South Baltic coastal zone (Hulisz, 2013). Inaccordance with the concept of Huggett (1975), it can also be called soil-landscape system where soilproperties vary along a specific gradient, conditioned by a combination of local environmental fac-tors. The soil salinity level and sulphur dynamics were mainly affected by the recharge of the coastalareas with seawater during high water levels or storms, and seawater intrusions into shallow ground-water. That is why those soils can be considered as a geochemically independent. It should be noted,however, that the lack of regular sea transgressions (tides) and the presence of small depressions filledwith organic sediments (reservoirs of the saline water) contributed to the fact that salinity of the stud-ied soils in the narrow zone increased with the distance from the waterline (Table 4, 8 and 12). Underthe conditions of the study, this pattern was observed within a limited area (up to about 50 m fromthe sea). It should be assumed that under other conditions of a local environment in the sequences ofcoastal soils, the direction of the salinity changes may be reversed. This was evidenced by, among oth-ers, the results obtained by Giani (1992) and Hulisz et al. (2013) for the clayey salt marsh soils exposedto regular tidal flooding in the North Sea area.


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Dijkema, K.S., 1990. Salt and brackish marshes around the Baltic Sea and adjacent parts of the North Sea: theirvegetation and management.Biological Conservation 51, 191209.

Feistel, R., Weinreben, S., Wolf, H., Seitz, S., Spitzer, P., Adel, B., Nausch, G., Schneider, B., Wright, D.G., 2010.

Density and absolute salinity of the Baltic Sea 20062009. Ocean Science. 6, 324.

Filipiak, J., Mitus, M., Owczarek, M., 2004. Meteorological conditions.In: Krzymiski, W., ysiak-Pastuszak, E.,Mitus, M., (Eds.), Environmental conditions of Polish zone of the southern Baltic Sea in 2001. MateriayOddziau Morskiego IMGW, Gdynia, 932 (in Polish).

Giani, L., 1992. Entwicklung und Eigenschaften von Marschbden im Deichvorland der sdlichen Nordseekste.Habilitationsschrift. Oldenburg (in German).

Herbich, J., 2004: Coastal salt marshes (GlaucoPuccinellietalia, part coastal communities). In: Herbich, J.,(Ed.), Tutorials protection of habitats and species Natura 2000 sites Methodological manual, Volume 1. Marineand coastal habitats, coastal and inland salt flats and dunes. Ministerstwo rodowiska, Warszawa, 7985(in Polish).

Huggett, R., 1975. Soil landscape systems: a model of soil genesis.Geoderma 13, 122.

Hulisz, P., 2013. Genesis, properties and systematics position of the brackish marsh soils in the Baltic coastal zone.Rozprawy habilitacyjne. Wyd. UMK, Toru (in Polish with English summary)

Hulisz, P., Gonet, S.S., Giani, L., Markiewicz, M., 2013. Chronosequential alterations in soil organic matter dur-ing initial development of coastal salt marsh soils at the southern North Sea. Zeitschrift fr Geomorphologie 57,4, 515529.

Hulisz, P., Krzelak, I., Karasiewicz, T., 2012. Characteristics of sedimentary environments in brackish marshsoils in relation to organic matter properties (Puck Lagoon, Northern Poland). Ecological Questions 16, 8797.

IUSS Working Group WRB, 2014. World Reference Base for Soil Resources 2014. International soil classification

system for naming soils and creating legends for soil maps.World Soil Resources Report No. 106, FAO, Rome.

Kottek, M., Grieser, J., Beck, C., Rudolf, B., Rubel, F., 2006. World Map of the Kppen-Geiger climate classifica-tion updated.Meteorologische Zeitschrift 15, 259263.

Kwiecie, K., 1990. Climate.In: Majewski, A., (Ed.). Gdask Gulf.Wyd. Geologiczne, Warszawa, 66119 (in Polish).

Majewski, A., Lauer, Z., (Eds.) 1994.Atlas of the Baltic Sea . IMGW, Warszawa (in Polish).

Soil Survey Laboratory Staff. 1996. Soil Survey Laboratory Methods Manual.USDA.

Tomczak, A., 1994. Hel Peninsula - relief, geology, evolution.In: Rotnicki, K., (Ed.). Changes of the Polish CoastalZone. Guide-Book of the Field Symposium. Symposium on Changes of Coastal Zone Polish Coast, Gdynia,Poland, August 27th - September 1st, 1994. Quaternary Research Institute, Adam Mickiewicz University, Poz-na: 7071.

van Reeuvijk, L. P., (Ed.). 2002. Procedures for Soil Analysis.ISRIC, Wageningen.

Wrblewski, R., 2008. Changes in the western part of the Hel Peninsula. Landform Analysis 9, 226227(in Polish).


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Forested areas within the outwash plain in Poland(Tuchola Forest)Piotr Hulisz, Marta Kowalczyk, M. Tomasz Karasiewicz

The Tuchola Forest (Bory Tucholskie) is one of the largestforest complexes in Poland which lies between the Brda andWda Rivers (north-central Poland). It covers the vast out-wash plain of over 3.000 km2 area located in front of thePomeranian phase of the Vistulian glaciation (Marks, 2012;Fig.1). The relief in this part of the Polish Lowland is verydiverse. Other landforms occurring in that area are flat and

undulated moraine remnants, kames, eskers, subglacial tun-nels, kettle-holes, dunes, river valleys and peat plains (Galon,1953 and 1958).

Lithology and topographyLithology and topographyLithology and topographyLithology and topographyThe presented soil sequence is located in the northeasternpart of the Tuchola Forest (Popwka site) within the smallkettle-hole (0.23 ha) formed in the outwash plain. The sitelies on the edge of the intersection of the subglacial tunnelsand therefore there are significant height differences in theimmediate vicinity (154 m a.s.l. on the northern side, 144 m a.s.l. in the central part of the kettle-holeand about 149 m a.s.l. on the southern side). The maximum inclinations of slopes reach about 7. Theslope deposits are represented by sands and fine gravels. The bottom of the kettle-hole is covered bythe ombrogenous (highmoor) peat bog.

VegetationVegetationVegetationVegetationThe current vegetation cover of the Tuchola Forest is a result of changes and transformations takingplace over many centuries (Filbrandt-Czaja, 2009). The forest cover in the region is as much as 64%and represents 96% of the coniferous forest habitats (Kliczkowska and Zielony, 2012). The slopes ofthe kettle-hole were overgrown with Scots pines (Pinus sylvestris) and the most common forest floorspecies were: Entodon schreberi, Dicranum polysetum, Vaccinium vitis-idaea, Vaccinium myrtillus,Festuca ovina.However, thebog vegetation included Sphagnumsp., Vaccinium uliginosum, Oxycoccus

palustris, Polytrichum strictum, Eriophorum vaginatumwith an admixture of Pinus silvestris and Betu-la pubescens.

ClimateClimateClimateClimateThe region is located in the warm temperate, fully humid climate zone with warm summer (Kottek etal., 2006). The average annual air temperature for the period of 19511970 is about 7C.The aver-age temperature of the warmest month (July) is 16.6C, while the coldest month is January (-2.2C).The average annual precipitation is 580 mm. As much as 375 mm of precipitation falls in the periodfrom April to September (Wjcik, Marciniak, 1987a, b). Westerlies prevail in the region and average

annual wind speed is 4 ms-1 (Atlas of the climate of Poland, 2005).

F. 1. L


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48

P 1 Dic Abic Bic AL: Pka (Tcha Fe), ah ai, keehe,e e (hde), feh cife

fe, 147 a..; N 535622.86, E17485.82

O

O

O

AE()

B

BC

C1

C2

C3

M:



20 c, high deced gaic aeia;

018 c, feae f ghig dibacei he a, dici aeia i hee a, fie ad, dak ga (10YR 5/1;10YR 4/1), d, ige gai ce, fie adc , ab ad a bda;

1840 c, fie ad, eih b(10YR 6/6; 10YR 5/6), d, ige gai ce, fie ad fe , gada ad abda;

4049 c, fie ad, bih e(10YR 7/6; 10YR 6/6), d, ige gai ce, e fie ad e fe , ab ada bda;

4965 c, fie ad, igh ga (10YR 8/2;10YR 7/2), d, ige gai ce, ceaad h bda;

6571 c, fie ad ih adie f gae, igh eih b (10YR 7/4; 10YR 6/4),d, ige gai ce, ab ad iega bda;

71(90) c, fie ad, igh bih ga(10YR 7/2; 10YR 6/2), d, ige gai ce.

[c] 0

50

90


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Piotr Hulisz et al.

49

T 1. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

< 0.05

AE 018 1 3 21 43 27 4 2 MS

B 1840 3 5 25 44 20 4 2 MS

BC 4049 1 2 10 56 31 1 0 MS

C1 4965 1 1 8 60 30 1 0 MS

C2 6571 9 7 16 48 28 1 0 MS

C3 71(90) 0 0 2 58 39 1 0 MS

T 2. C

HD[]

OC[

1]

N[

1]

C/NH

H2O KCOe 62 348 10.2 34 3.9 2.8

Oa 20 338 9.75 35 3.2 2.2

AE 018 7.90 0.20 40 5.0 4.2

B 1840 2.20 0.10 16 4.9 4.6

BC 4049 4.8 4.7

C1 4965 5.0 4.9

C2 6571 5.1 4.8

C3 71(90) 5.3 4.9

T 3. C

HD[]

F F A A

[1

]

AE 018 1.19 4.15 0.73 11.1

B 1840 1.06 6.20 2.13 16.2

BC 4049 0.62 4.99 0.96 10.3

C1 4965 0.42 4.04 0.27 11.2

C2 6571 0.85 7.56 0.55 14.0

C3 71(90) 0.35 4.69 0.45 11.9


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P 2 Dic Bic Abic FicA e Geic AbicP (Aeic)L: Pka (B Tchkie), ah ai, keehe,idde e (back e), feh c

ife fe, 145 a...; N535623.94, E17485.1

O

O

O

EA

BA

A

E

B1

B2

C

M:

126 c, igh deced gaicaeia;



03 c, aeia, fie ad, ighbih ga (10YR 7/2; 10YR 6/2), d, ige gai ce, fie ad edi c, ab ad h bda;

325 c, fie ad, b (10YR 6/3;10YR 5/3), d, ige gai ce, e fiead fe , ab ad h bda;

2534 c, fie ad, ga (10YR 6/1; 10YR5/1), d, ige gai ce, fie ad fe, ab ad h bda;

3440 c, aeia, fie ad, ighga (10YR 8/1; 10YR 7/1), d, ige gaice, ab ad h bda;

4043 c, hi, fie ad, dakb (10YR 4/3; 10YR 3/3), d, ige gaice, e fie ad fe , ab adh bda;

4358 c, hi, fie ad,bih e (10YR 7/6; 10YR 6/6), d,ige gai ce, edi ad fe ,gada ad h bda;

58(80) c, fie ad, ae e (2.5Y 8/3;2.5Y 7/3), igh i, ige gai ce,fe ihic e.

[c] 0

50

80


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Piotr Hulisz et al.

51

T 4. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

< 0.05

EA 03 2 4 27 51 13 2 1 MS

BA 325 >1 5 24 50 16 2 3 MS

Ab 2534 >1 3 21 50 21 2 3 MS

Eb 3440 >1 3 13 60 22 2 0 MS

Bb1 4043 >1 2 16 59 20 2 1 MS

Bb2 4358 1 3 14 57 24 2 0 MS

C 58(80) >1 1 8 71 19 1 0 MS

T 5. C

H D[]

OC[

1]

N[

1]

C/N H

H2O KC

Oi2 106 420 11.3 37 3.5 2.4

Oe 61 412 11.3 37 3.2 2.1

Oa 10 3.7 2.4

EA 03 9.4 0.32 29 4.2 3.1

BA 325 9.2 0.28 33 4.9 4.0

Ab 2534 8.7 0.22 40 4.8 3.9

Eb 3440 5.2 4.2

Bb2 4358 3.9 0.15 4.9 4.8

C 58(80) 4.9 4.8

T 6. C

HD[]

F F A A

[1

]

EA 03 0.36 1.99 0.16 8.24

BA 325 0.83 3.09 0.66 10.8

Ab 2534 0.48 2.88 0.56 13.3

Eb 3440 0.16 1.03 0.22 6.28

Bb2 4358 1.56 4.91 6.58 16.4

C 58(80) 0.11 3.12 0.78 13.2


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P 3Geic Abic Oeiic P (Aeic)L: Pka (B Tchkie), ah ai, keehe,e e (f e), e cife

fe, 144 a..., N535624.00, E17484.8

O

O

O

O/A

E

B1

B2

B1

B2

M:




011 c, fie a ad, e dak ga(10YR 4/1; 10YR 3/1), d, ige gai ce, edi ad cae , ab adh bda;

1130/44, aeia, fie ad, ighga (10YR 8/1; 10YR 7/1), d, ige gaice, diffe ad iega bda;

30/4455 c, hi, fie ad,e dak b (10YR 4/2; 10YR 2/2), d,deae aie (chee) ce, ceaad h bda;

5566 c, hi, fie ad, edak b (7.5YR 4/3; 7.5YR 2,5/3), d,

deae aie (chee) ce,gada ad h bda;

6684 c, hi, fie ad, dakeih b (10YR 5/4; 10YR 4/4), d,deae aie (chee) ce, aihic e, cea ad hbda;

be 84 c, hi, edi ad,e dak b (10YR 4/4; 10YR 2/2), d,deae aie (chee) ce, aihic e.

[c] 0

50

90


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53

T 7. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

< 0.05

O/A 011 0 12 20 32 20 8 8 LS

E 1130/44 2 3 20 48 23 3 3 MS

B1 30/4455 >1 6 19 48 22 3 2 MS

B2 5566 >1 4 13 48 33 1 1 MS

B1 6684 >1 2 15 48 33 2 0 MS

B2 >84 2 8 45 19 26 1 1 CS

T 8. C

HD

[]

OC

[

1

]

N

[

1

]

C/NH

H2O KCOe 51 429 145 30 3.9 2.8

Oa 10 426 129 33 3.0 2.2

O/A 011 136 4.06 34 3.9 3.1

E 1130/44 2.4 0.15 16 5.3 3.9

B1 30/4455 37.1 1.21 31 4.1 3.2

B2 5566 19.4 0.48 40 4.8 4.1

B1 6684 7.8 0.23 34 4.7 4.2

B2 >84 9.0 0.22 41 4.7 4.1

T 9. C

HD[]

F F A A

[1

]

O/A 011 6.00 10.0 4.50 27.6

E 1130/44 0.06 0.88 0.06 3.73

B1 30/4455 0.43 1.64 1.90 10.3

B2 5566 0.18 4.97 5.20 14.2

B1 6684 0.04 2.89 1.31 9.56

B2 >84 0.09 2.01 1.93 13.8


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P 4 Dic Obic Heic HL: Pka (B Tchkie), bda beee he ah ai ad he keehe, e

e (f e), bge ea bg (he agg e), 143 a...;N535623.94, E17484.98

H1

H2

H1

H2

C

M:

hi:

04 c, ie e (2.5Y 8/6; 2.5Y 6/6),igh deced gaic aeia (D1),dd, e;

415 c, ie b (2.5Y 5/3; 2.5Y 4/3),igh deced gaic aeia (D2),dd, e;

1545 c, e dak gaih b(2.5Y 5/2; 2.5Y 3/2), deae decedgaic aeia (D5), e;

4565 c, e dak gaih b(2.5Y 4/2; 2.5Y 3/2), deae decedgaic aeia (D5), e;

be 65 c, fie ad, igh geeih ga(10Y 8/1; 10Y 7/1), e, ige gai ce, eie.

[c] 0

50


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Piotr Hulisz et al.

55

T 10. T

HD[]

P []T

> 2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

< 0.05

C >65 >1 5 30 48 14 2 1 MS

T 11. C

HD[]

OC[1]

N[1]

C/NH

H2O KC

Hi1 04 424 9.0 47 4.3 3.0

Hi2 415 452 10.8 42 4.0 2.8

He1 1545 445 11.6 39 3.8 2.7

He2 4565 402 7.5 54 3.8 2.5

C >65 2.5 0.1 28 4.8 3.2

T 12. C

HD[]

F A

[1]

Hi1 04 2.42 13.0

Hi2 415 2.64 4.53

He1 1545 0.98 1.30

He2 4565 0.44 0.84

C >65 0.50 2.50


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56

P 5 Dic Obic Fibic HL: Pka (B Tchkie), kee he, b, bge ea bg, 142.5 a...,

N535625.13, E17484.48

H1

H2

H3

M:

hi:

03 c, igh eih b (2.5Y 7/4; 2.5Y 6/4), e ighdeced gaic aeia (D1), e;

312 c, igh ie b (2.5Y 6/4; 2.5Y 5/4), igh deced gaic aeia (D1), e;

12 c, ie b (2.5Y 5/3; 2.5Y 4/3), igh deced gaic aeia (D2), e.

T 13. C

HD[]

OC[

1]

N[

1]

C/NH

H2O KC

Hi1 03 425 8.7 49 4.2 2.9

Hi2 312 424 8.2 52 3.6 2.4Hi3 1235 422 11.5 37 3.5 2.3

[c] 0

35


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F.2.H

P(TF)


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Soil genesis and systematic positionSoil genesis and systematic positionSoil genesis and systematic positionSoil genesis and systematic positionSoil properties of outwash plains were affected by processes of morpho- and lithogenesis at the end ofPleistocene. Holocene erosion phenomena initiated the denudation of land surface, and processes oflithogenesis were replaced by pedogenesis, which largely modified the initial properties of the rockmaterial (Bieniek, 2013). Most of the soils occurring in the outwash areas were characterized by the

sandy texture. Dystric Albic BrunicDystric Albic BrunicDystric Albic BrunicDystric Albic BrunicArenosolsArenosolsArenosolsArenosols IUSS Working Group WRB (2014), represented byProfile 1, was the dominant soil unit in this landscape. The Bw horizon of these acid soils had specific,yellowish brown colour resulting from the presence of humus complexes containing sesquioxideswhich form coatings around mineral grains. Properties of this horizon met most of the criteria for thecambichorizon except for the texture criterion, and therefore the BrunicBrunicBrunicBrunicprincipal qualifier was ap-plied. In the topsoil (transformed as a result of agricultural treatments), the albicalbicalbicalbic material (few cmthick, discontinuous horizon) was present as a consequence of the podzolization process commonlyoccurring in these soils. This process is affected by pine monocultures introduced in place of conifer-ous or mixed forests (Sewerniak et al., 2009). Furthermore, the described soil was characterized by theoccurrence of a few cm thick sandy horizon with an admixture of gravels (wind-worn stones; 6571

cm) Fig 2.Two other soils (Profile 2, 3) were described as Podzols.Podzols.Podzols.Podzols. This RSG was distinguished based on the

presence of the spodicspodicspodicspodichorizon, in the formation of which ground water contributed. The groundwa-ter level in the past could be much higher than today (e.g. 2 m below the surface level). The soils hada well-developed horizons which met the criteria for the albicalbicalbicalbicmaterial. The genesis of the first soilwas significantly affected by slope processes, which resulted in the presence of a 25 cm layer of collu-via. The presence of these sediments could provide evidence of periods with intensified erosion pro-cesses in the past, induced by human activity (Sinkiewicz 1998; Kowalkowski 1999). Surface sedimentswere transformed by pedogenetic processes and consequently, a sequence of two soils developed,which according to the WRB classification (IUSS Working Group WRB, 2014) can be defined as DyDyDyDys-s-s-s-trictrictrictric Brunic Albic FolBrunic Albic FolBrunic Albic FolBrunic Albic Folicicicic ArenosolArenosolArenosolArenosol over Gleyic AlbicGleyic AlbicGleyic AlbicGleyic AlbicPodzolPodzolPodzolPodzol (Arenic)(Arenic)(Arenic)(Arenic).

The latter pedon (Profile 3) was classified as Gleyic Albic OrtsteinicGleyic Albic OrtsteinicGleyic Albic OrtsteinicGleyic Albic OrtsteinicPodzolPodzolPodzolPodzol (Arenic)(Arenic)(Arenic)(Arenic).... This soilhad a mixed surface horizon (O/A), which was a primeval organic horizon developed as a result ofmixing between the former organic horizon and deluvia during the soil preparation for pine planting.A distinguishing feature of this soil was ortstein (OrtsteinicOrtsteinicOrtsteinicOrtsteinic principal qualifier) occurring froma depth of 30 cm strongly cemented soil material enriched with humus, iron and aluminium com-pounds, building the illuvial horizon (B). The formation of ortstein can be associated with an inten-sive process of podzolization in cooler and more humid climate compared to climate today (Prus-inkiewicz, Norykiewicz, 1966), or with a relatively shallow groundwater level (Wang et al., 1978;

Chodorowski, 2000 and 2009). On the one hand this process at the studied site should be related to anintensive podzolization process, which covers upper genetic horizons, but on the other witha ground-gleyic process covering the middle and the lower part of the profile. On the borderline be-tween the two zones, elements eluted from the upper genetic horizons through infiltrating rainwaterare precipitated together with elements uplifted by the capillary water from the lower endopedons,covered by the gleyic process (GleyicGleyicGleyicGleyic principal qualifier).

The last profiles (4, 5) were represented by organic soils (Histosols)Histosols)Histosols)Histosols) and recharged mainly byprecipitation waters (OmbricOmbricOmbricOmbric principal qualifier). Profile 4 was defined as Dystric Ombric HemicDystric Ombric HemicDystric Ombric HemicDystric Ombric HemicHistosolHistosolHistosolHistosol according to WRB criteria. The total thickness of organic sediments was 65 cm, and organicmatter (slightly decomposed peat, D1) occurred from this depth up to 15 cm. Peat located at a depth

of 1565 cm was highly decomposed (D5, HemicHemicHemicHemic principal qualifier). This sequence of peat depositswith a varying degree of decomposition could indicate a relatively high groundwater level fluctua-


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tions, typical of the lagg zone. Profile 5 was classified as Dystric Ombric FibricDystric Ombric FibricDystric Ombric FibricDystric Ombric Fibric HistosolHistosolHistosolHistosol. The decom-position rate of organic matter in this soil is very slow, therefore it is characterized by the presence ofpoorly and very poorly decomposed plant remnants (D1 and D2, FibricFibricFibricFibric principal qualifier). Sphag-num sp. was the dominant peat-forming species.

Soil sequenceSoil sequenceSoil sequenceSoil sequenceSpatial variability of the soil properties along the analysed transect was determined mainly by suchfactors as relief, rainwater and groundwater. Nowadays, due to the presence of dense vegetation cover(pine forest), the impact of denudation processes on the soil cover is rather very small. The spatialarrangement of pedons located on the slope and within the kettle-hole represents hydrohydrohydrohydro----topotopotopotoposssseeeequencequencequencequence (Fig. 2). The Albic BrunicAlbic BrunicAlbic BrunicAlbic Brunic ArenosArenosArenosArenosolsolsolsols were typical of the relatively flat upper parts ofthe slopes, whereas the semi-hydrogenic soils occurred in the lower slope locations (GleyicGleyicGleyicGleyic AlbicAlbicAlbicAlbicPodzols)Podzols)Podzols)Podzols). In some places they were covered by colluvial deposits ((((BrunicBrunicBrunicBrunicArenosols)Arenosols)Arenosols)Arenosols), the thickness ofwhich decreased towards the footslope.The soils in that part of the slope also had a strongly cementedspodicspodicspodicspodichorizon (GleyicGleyicGleyicGleyic AlbicAlbicAlbicAlbic OrtsteinicOrtsteinicOrtsteinicOrtsteinic PodzolsPodzolsPodzolsPodzols). The kettle-hole was filled with the peat deposits

characterized by a different degree of decomposition. The soils there were classified as Dystric ODystric ODystric ODystric Om-m-m-m-bric Hemicbric Hemicbric Hemicbric Hemic HistosolsHistosolsHistosolsHistosols and Dystric Ombric FibricDystric Ombric FibricDystric Ombric FibricDystric Ombric FibricHistosols.Histosols.Histosols.Histosols.

ReferencesReferencesReferencesReferencesAtlas of the climate of Poland. 2005. (Ed. H. Lorenc). IMGW. Warszawa (in Polish).

Bieniek, A., 2013. Soils of inner outwash plains in North-Eastern Poland. Wydawnictwo Uniwersytetu Warmi-sko-Mazurskiego, Olsztyn (in Polish with English abstract).

Chodorowski, J., 2000. Characterization of occurrence conditions and morphology of ortstein soils in the area ofthe Lasy Janowskie Landscape Park. Rocz. Glebozn. 51, 1/2, 113124 (in Polish with English abstract).

Chodorowski, J., 2009. Origin, age and diagnostic properties of ortstein in the light of a study of sand soils in the San-donierz Basin. Wydawnictwo Uniwersytetu Marii Curie-Skodowskiej, Lublin (in Polish with English summary).

Filbrandt-Czaja, A., 2009. Studies on the history of vegetation and landscape of the Tuchola Forest. Wyd. Nauk.UMK, Toru (in Polish with English summary).

Galon, R., 1953. Morphology of the the Brda valley and outwash sand plain. Stud. Soc. Sci. Toruniensis 1, 6,150 (in Polish with English abstract).

Galon, R., 1958. New geomorphological studies on the Brda outwash plain. Zesz. Nauk. UMK, Geografia 1, 4,16 (in Polish with English abstract).

Kottek, M., Grieser, J., Beck, C., Rudolf, B., Rubel, F., 2006. World Map of the Kppen-Geiger climate classifica-tion updated.Meteorologische Zeitschrift. 15, 259263.

IUSS Working Group WRB, 2014. World Reference Base for Soil Resources 2014. International soil classificationsystem for naming soils and creating legends for soil maps.World Soil Resources Report No. 106, FAO, Rome.

Kliczkowska, A., Zielony, R., 2012. Nature and forest regionalisation of Poland 2010. Centrum Informacji LaswPastwowych, Warszawa (in Polish).

Kowalkowski, A., 1999. Soil evolution in the Holocene. In: Starkel, L., (Ed.) Geografia Polski. rodowisko przy-rodnicze. PWN Warszawa, 127137 (in Polish).

Marks, L., 2012. Timing of the Late Vistulian (Weichselian) glacial phases in Poland. Quaternary Science Re-views. 44, 8188.


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Prusinkiewicz, Z., Norykiewicz, B., 1966. Problem of age of podzols on brown dunes of bay bars of river wina inthe light of a palynological analysis and dating by radiocarbon C14. Zesz. Nauk. UMK w Toruniu, Nauki Ma-tematyczno-Przyrodnicze, Geografia 5, 14, 7587 (in Polish with English abstract).

Sinkiewicz, M., 1998. Development of anthropogenic denudation in the central part of Northern Poland.Wyd.UMK Toru (in Polish with English summary).

Wang, C., Beke, G. J., McKeague, J. A., 1978. Site characteristics, morphology and physical properties of selectedorstein soils from the Maritime Provinces. Canadian Journal of Soil Science, 58, 405420.

Wjcik, G., Marciniak, K., 1987a. Thermal conditions in central part of the North Poland in the years 19511970.AUNC. Geogr. 20, 2950 (in Polish).

Wjcik, G., Marciniak, K., 1987b. Precipitations in central part of the North Poland in the years 19511970 .AUNC. Geogr. 20, 5169 (in Polish).

Sewerniak, P., Gonet, S.S., Piernik, A., 2009. Relations between features of forest floor vegetation and surface soilhorizons properties in Scots pine (Pinus sylvestris L.) stands in southwest Poland. Polish Journal of Soil Science42,2, 193202.


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Forested areas within hummocky moraine plateausof Poland (Brodnica Lake District)Marcin witoniak, Przemysaw Charzyski, ukasz Mendyk

The young morainic area of North Poland is part of theNorth European Plain and lies within the maximum range ofthe Vistulian Glaciation (Fig. 1) defined as the Leszno Phasein western Poland and the Pozna Phase in the central andeastern part of the country (Marks, 2012). The BrodnicaLake District represents typical young glacial landscapes andis located between the limits of the two major Vistulian gla-

cial phases: Pozna and Pomeranian Phases. The generaloutline of the relief was formed during the late glacial peri-od, i.e. ca. 1617 ka CE (Niewiarowski, 1986; Niewiarowskiand Wysota, 1986). The Brodnica moraine plateau is cut bylongitudinal subglacial channels filled by numerous lakesand two sandy outwash plains (West and East Brodnica;Niewiarowski, 1986).

Lithology and topographyLithology and topographyLithology and topographyLithology and topographyThe presented soils were located in the south-eastern part of the Brodnica Lake District within a typi-

cal hummocky moraine plateau. The differences in terrain altitudes are associated with numerouskettles, irregular and elongate or roundish in shape. Among the surface sediments, ablation sandsdominate with a thickness of tens of centimeters on glacial till. Slopes with an inclination > 10 repre-sent about 16% of the total surface. The maximum inclinations of slopes reach about 30. The denive-lations are relatively high and in many places range up to 20 m.

Land useLand useLand useLand useOnly small areas of moraine plateaus within the Brodnica Lake District are covered by mixed forest.Because of a relatively high fertility of soils, the vast majority of them was converted into arable lands.Lack of profitability of agricultural production in currently forested areas is associated with intensiverelief. The canopy layer is dominated by pines (Pinus sylvestris). Species typical of hornbeam forest

(Carpinus betulus, Tilia cordata, andQuercus sp) dominate in the understory, the herb layer and theforest floor.

ClimateClimateClimateClimateThe region is located in the zone of moist and cool temperate climate (IPCC, 2006). According toKppenGeiger Climate Classification, the region is located in the fully humid zone with temperateand warm summer (Kottek et al., 2006). The average annual air temperature is about 7C. The warm-est month is July (17.6C). The mean air temperature during January (coldest winter month) is about-4C. The average annual precipitation is 552 mm. July is the wettest month with average precipita-tion around 90 mm (Wjcik and Marciniak, 1987a, b, 1993).

F. 1. L


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P 1 Eidic Abic Necabic Gic R(Abic, Caic, Ric)L:hck aiic aea, fa eai ih e < 1, ied fe, 121 a...

N 532012, E192718

O

O

A

B

E

E/B

2B

2C

M:



020 c, h hi, ad a, dakb (10YR 5/3; 10YR 3/3), d, deaegaa edi ce, fie ad edic , diffe ad bke bda;

2055 c, hi, ad a, dakeih b (10YR 6/4; 10YR 4/5), d,eak baga e fie ce, e fiead e fe , cea ad h bda;

5570/65 c, eia hi ih aeia, ad a, igh eih b(10YR 7,5/3; 10YR 6/4), d, eak bagae fie ce, ab ad bke bda;

70/6580 c, aiia hi, iefi

geig f aeia i hi; 80115 c, hi, ad ca a,g b (7.5YR 6/6; 7.5YR 4/6), ighi, g aga cae ce, c fai ca caig, gada ad hbda;

115(130) c, ae aeia, ad a,dak eih b (10YR 5/6; 10YR 4/6),igh i, deae aga cae ce.

[c] 0

50

100


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T 1. T

H D[]

P []T

> 2.0

2.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

2.02.01.0

1.00.5

0.50.25

0.250.1

0.10.05

0.050.02

0.020.005

0.0050.002

28,3 gkg-1), dark colour, well developed soilstructure, significant thickness and low base saturation, the humus horizon has been classified as um-bric. Because no other diagnostic horizons were present, the soil was classified as UmbrisolsUmbrisolsUmbrisolsUmbrisols. Thedescribed soil has strong reducing conditions and gleyic properties below 35 cm from the surface(GleyicGleyicGleyicGleyic principal qualifier) and is exceptionally rich in organic carbon. Horizon B, in addition to re-ducing colours caused by ascending groundwater (l), includes illuvial concentrations of humus onaggregates surfaces. High base saturation (>50%) of this horizon is indicated by the EndoeutricEndoeutricEndoeut

soil sequences atlas 2014

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