Zbigniew Klimowicz, Jerzy Melke Department of Soil Science Institute of Earth Sciences Maria Curie-Sklodowska University Lublin, Poland

Wyprawy Geograficzne na Spitsbergen UMCS, Lublin 1991

ю THE INFLUENCE OF LITHOLOGY AND TERRAIN RELIEF ON THE SOIL OF CALYPSOSTRANDA

I N T R O D U C T I O N

. The first studies on the soils of Bellsund region were carried out by Klimowicz and Uziak in the summer of 1986 (1988). They covered mainly the soil of Calypsostranda. In the following years Melke, Chodorowski, and Uziak (1990) studied the soils in the region of Lyellstranda, Chamberlindalen, Dyrstad, and Logne.

The primary aim of the present article is to show the relations between lithology and terrain relief and soil properties in the arctic conditions. The method used is the method of cross-section. The same method was used by Steven et al. (1984) for the soils of Broggerhalvoya (Spitsbergen).

T H E C H A R A C T E R I S T I C S O F T H E S T U D I E D T E R R A I N

The soil was studied on the cross-section across Calypsostranda — from the beach to the Bohlinryggen slopes (Fig. 1). In the bedrock of Calypsostranda that forms a coastal plain there appear Tertiary sandstone and mudstone (Flood et al. 1971). Quaternary sediment with the thickness up to several meters are mainly of gravel-sandy type in the area of lower terraces; whereas on the more raised terrain these are formations of a more complex origin, mainly clay, sand with sea fauna, boulder clay and gravel-sandy series (Troitsky et al. 1979, Pękala 1987, Rępelewska-Pękalowa 1987, Pękala, Repelewska-Pękalowa 1990).

The region of Bohlinryggen represents, according to Dallmann et al. (1990) mainly Kapp Lyell sequence rock (Upper Proterozoic) with „uncertain" stratigraphic pattern. In the highest areas of Bohlinryggen diamictites (called tillites earlier by, among others, Hauser) with dolomite and quartzite clasts can be found together with phyllites. It is very important in case of soils, because the main mineral component of tillites are carbonates, predominately calcium carbonates with dolomite admixture (CaMg(C03)2) — Chlebowski 1989. It is well known that any admixture of these compounds in the soil influences not only its reaction but also other soil chemical properties.

135

As it has been already mentioned, the studied cross-section begins on the beach, then about 100 m away from the fiord it runs across dead sea cliff with solifluction tongue. Further on it crosses raised sea terraces, and in the neighbourhood of the so-called „lake", enters partial fen called depression. Then the terrain raises markedly, and at the hight of 60-70 m above the sea level there appear first rock outliers of the bedrock (Szczęsny et al. 1989). After leaving the system of terraces the cross-section line runs to the north-west Bohlinryggen slope with weathering cover. The terrain inclination is the greatest there.

»Such factors as: hight above the sea level, slope inclination and exposition and type of bedrock have the greatest influence on the topoclimatic differentiation of Calypsostranda (Siwek, Paczos 1990). The fen in the cross-section area does not cover too large a surface. Its appearance and reach depends, among others, on the relief and lithology, and it is the subject of seasonal variations (Bartoszewski 1987, Michalczyk 1990). In the region of the Bellsund south coast there are-two dominating groups of tundra ecologic-floristic plants, that is dry and mezophyl-lic moss and lichen-like group, and wet moss group. The latter group appears on Spitsbergen rather seldom. Relations between vegetation and microhabitats are most visible in the spotted tundra type (Święs 1988).

RESULTS

The studied cross-section starts in the area devoid of soil (Fig. 1, Tab. 1, 2). These are deposits with markedly predominating sand in the earth fraction (> 90%). The contents of carbonates is also very high, and the reaction very alkaline. The main reason for the lack of soil is the young age of these deposits together with high sea activity (with stormy waves).

Terrain relief is the forming factor on the dead cliff slope. Inclination of about 20° makes the thawed material flow down by the law of gravity and according to the highest inclination. The soil also gets shifted. The profile No 2 representing stripped soil has been recognized on the solifluction tongue.. The properties of the soil being described here are also influenced by lithology. Heavy silty loam that appears in the lower part of the profile makes the soil moisture contents higher influencing vegetation cover at the same time (colonies of algae). The organic carbon contents in the initial humus level is higher than in the neighbouring brown soil (profile No 3). In the deaper levels, however, this situation is reversed. The contents of CaC0 3 and pH is high in both profiles.

At a distance of 150-200 m from the sea a higher sea terrace — widespread and flat — starts with a clear-cut edge. In the neighbourhood of the edge, in the zone 200 m \yide that is more-or-leSs parallel to it, there appear classic polygons with a system of frost fissures. They have a diameter of several meters and fitted lines of fissures. Brown soils are predominant (Melke, Uziak 1989). Then the

136

cross-section runs across dry mossy tundra that is non-differentiated on the surface or with little differentiation. The predominating soils there are poorly developed soils, or, less frequently, brown soils (Klimowicz, Uziak 1988).

In the neighbourhood of the so-called „lake", in the area of the solifluction kettle there appear (on the north side) classic polygons with stone circles and earth inner part (with small amounts of stones and gravel). To the south of the „lake" there is a system of typical frost fissures. The profile No 5 representing brown soil is localized there. The A, level in the above mentioned profile has a considerable, as for arctic conditions, thickness, and contains the highest amounts of organic carbon. The soil pit No 4 was made on a small holm, on the lake. In the conditions of excessive wettness gley soils were formed. They are covered mainly by brown-pinkish algae. In the close neighbourhood of the above mentioned profiles, in the region of solifluction kettle there are seven turf hillocks more or less convex. Shallow peat soils or peaty soils underlayered with loamy sand (Klimowicz, Uziak 1988).

In the section between the profiles 4-5 and 6 tundra is wet in some regions, and the frost fissures are hardly noticeable. Some part of little fissures and slots originates probably from the ground drying and shrinking. Close to the profile No 6 there are bedrock outliers. Among rocks in the low ground fine non-sorted rock debris is predominant. Polygons covered on the inside with a thin layer of gravel are also noticeable (not always clearly). Stone circles do not project but are rather sunk into the ground. In this latter part of the cross-section there appear also „earthly outflows" with a diameter of 20-50 cm without stone circles and without any framing plant cover. Flat and levelled surface together with the presence of heavy clay with low permfeability in the subsoil makes the soil profile No 6 wet and gleyed.

In the direction of the site 7 polygons with less or more visible stone circles can be Ąpund. In the inside parts of the circles there is debris, stones and gravel. Sporadically, on the surface there appear (outside the circles) fine fragments of bedrock. The profile No 7 (Fig. 1, Tab. 1,2) is situated on a shelf that is an outlier of denudated bedrocks, mainly tillites. There is no soil surface differentiation here. On the slope, below the flatness there are debris streaks (consisting mainly of slates) that often cover ground parts.

Profile No 8 was made in the bottom of a flat depression. There are clear-cut polygons with stone circles and great amounts of small, flat stones and gravels inside the circles there which cannot be observed in the fragment of the cross-section that is situated lower. Primitive stripped soil is accompanied in more inclined places (an evident influence of the relief) by slates. The studied soil profile No 8 forced on loam is saturated with water and gleyed. The contents of organic carbon is significantly lower than in the formerly discussed profiles. Among (other) plants there appear algae.

On the Bohlinryggen slope there is weathering cover with a considerable

137

amount of rock blocks and stones. In the nearest neighbourhood of the soil pit on the flatness at the foot of the ridge being described there are little marked polygons with stone circles. The studied initial soil (profile No 9) contains far below 1% of organic carbon. Plant cover takes only 15% of the surface.

The Bohlinryggen slope from the hight of about 200 m (above the sea level) has a very sharp inclination. It is covered by stones and boulders, in between which there appears soil here and there. Plant cover is also fragmentary (soil pit No .10). The soil of the profile No 11, on the opposite side of the ridge (EES exposure) is initial (similarly to the former soil) and without any plant cover. The organic carbon contents is very low, and the content of carbonates — high.

The following conclusions may be drawn from the analysis of the soil environment of the studied cross-section:

1. Mainly brown soils are formed from the parent rocks represented by mainly light loamy sands, in the environment of Calypsostranda (predominantly on the terraces 18-30 m, and partially 35-45 m above the sea level).

2. Soils originating from the formations with low permeability mainly heavy loams, have excessive moisture content and are characterized by the domination of gleying processes.

3. Lighter bedrocks predispose for the formation of soil with system of frost fissures or non differentiated on the surface. Bedrocks with heavier granulomet-ric composition favour the formation of soils with polygons and stone circles.

4. In the lower parts of the cross-section the terrain inclination favours the formation of stripped soils. Whereas on the Bohlinryggen slopes, where the terrain declines are significantly greater, initial soil dominates (lithosols). Moreover, considerable parts of the surface of these slopes are devoid of any soil cover. Scarcity of vegetation or its complete lack is a logical consequence of this situation.

5. The richest in organic carbon are the soils originating mainly from the formations with lighter granulometric composition.

6. The soils situated in places with considerable declines are, as a rule, the richest in carbonates. The reaction of the studied soils (high pH values) was not related either to the terrain relief or to the lithology.

More detailed conclusions on the interrelations between the character of the soil cover and other components of the geographical environment would be presented in the draft of the soil-levelling cross-section carried out in the region of the south Bellsund in 1990.

Translated by Ewa Gnyp

138

REFERENCES

Bartoszewski S., 1987: Charakterystyka hydrograficzna strefy południowego obrzeżenia Bellsun-du i fiordu Recherche (Spitsbergen Zachodni). XIV Sympozjum Polarne, Lublin.

Chlebowski R., 1989: Charakterystyka petrograficzno-mineralogiczna skał formacji Hecla Hoek w rejonie południowego obramowania Bellsundu, Zachodni Spitsbergen. Wyprawy Geograficzne na Spitsbergen, UMCS Lublin.

Dallmann W. K., Hjelle A., Ohta Y., Salvigsen O., BjornerudM. В., Hauser E. C., Maher H. D., Craddock C„ 1990: Geological Map of Svalbard 1:100 000, sheet В 11G, Van Kculcnfjordcn. Norsk Polarinstitutt, Oslo.

Flood В., Nagy J., Winsnes T. S„ 1971: Geological map Svalbard, 1:500 000, sheet 1G, Spitsbergen Southern part. Norsk Polarinstitutt, Skr. 154 A.

Klimowicz Z., Uziak S., 1988: Soil-forming processes and soil properties in the Calypsostranda Region (Western Spitsbergen). Polish Polar Research, vol. 9, 1.

Melke J., Chodorowski J., Uziak S., 1990: Soil formation and soil properties in the areas of Lyellstranda, Dyrstad and Logne in the region of Bellsund (West Spitsbergen). Polish Journal of Soil Science, vol. XXIII/2.

Michalczyk Z., 1990: Hydrological characteristics of Calypsostranda. Wyprawy Geograficzne na Spitsbergen, UMCS Lublin.

Pękala К., 1987: Rzeźba i utwory czwartorządowe przedpola lodowców Scotta i Renarda (Spitsbergen). XIV Sympozjum Polarne, Lublin.

Pękala K., Repelewska-Pękalowa ./., 1990: Relief and stratigraphy of Quaternary deposits in the region of Recherche Fiord and southern Bellsund (Western Spitsbergen). Wyprawy Geograficzne na Spitsbergen, UMCS Lublin.

Repelewska-Pękalowa J., 1987: Rozwój równiny nadmorskiej pod wpływem procesów erozji (na przykładzie Calypsostrandy, rejon Bellsundu, Zachodni Spitsbergen). XIV Sympozjum Polarne, Lublin.

Siwek K., Paczos .S'., 1990: Differentiation of Calypsostranda thermal and humidity conditions in the summer 1989 (Western Spitsbergen). Wyprawy Geograficzne na Spitsbergen, UMCS Lublin.

Steven L., Forman and Gifford H. Miller, 1984: Time-dependent soil morphologies and pedogenic processes on raised beaches, Broggerhalvoya, Spitsbergen, Svalbard Archipelago. Arctic and Alpine Research, vol. 16, 4.

Szczęsny R., Dzierżek J., Harasimiuk M., Nitychoruk J., Pękala К., Repelewska-Pękalowa J., 1989: Photogeological map of Renardbreen, Scottbreen and Blomlibreen forefield (Wedel Jarlsberg Land, Spitsbergen) 1:10000, Wyd. Geol. Warszawa.

Święs F., 1988: Zróżnicowanie geobotaniczne tundry na południowym wybrzeżu Bellsundu (Zachodni Spitsbergen). Wyprawy Geograficzne na Spitsbergen, UMCS Lublin.

Troitsky L., Punning J. M., Htitt G., Rajamae R., 1979: Pleistocene glaciation chronology of Spitsbergen. Boreas, vol. 4.

STRESZCZENIE

W pracy podjęto próbę przedstawienia związków i zależności pomiędzy litologią i rzeźbą a właściwościami gleb (w tym ich zróżnicowania powierzchniowego) w warunkach arktycznych. Posłużono się do tego celu metodą przekroju prowadzonego od fiordu po stoki Bohlinryggen i obejmującego gleby od inicjalnych (prymitywnych), głównie w miejscach o większych spadkach i nad samym morzem, po gleby o wykształconej morfologii i znacznej zawartości węgla organicznego. Ważną rolę w kształtowaniu właściwości omawianych gleb odegrały stosunki wodne (zależne w dużej mierze od rzeźby i litologii). Z warunkami glebowymi w „strefie" przekroju wyraźnie koreluje charakter pokrywy roślinnej.

139

Tab. 1. Characteristics of natural environment along the cross section: Beach of Calypsostranda — Bohlinryggen.

Profile number, Location, altitude /a.s.l./, soil name distance from fiord /along the cross Predominant species of plants

section/ x

1. Gravel and sandy deposits, loose sand interlayered of slightly loamy sand

2. Poorly developed stripped soil, light loamy sand on heavy silty loam

3. Lrown soil non-differentia-ted on the surface, light loamy sand

4. (-ley soil with polygons and stone circles, light loamy sand

5. Brown soil witl\ system of frost fissures, light loamy sand

The sandy beach with considerable admixture of gravels, 14 m

Slo-oe of a dead cliff of 20° inclina-tion and EKE exposition, 15 m a.s.l., 120 m, solifluction tongue Slope of a dead cliff of 20° inclina-tion and 3NE exposition, i5 m a.s.l., 120 m

Flat holm in the shallow water, near by stone circles, about 50 m a.s.l., 750 m /wet/ Flattened hillock within frost fis-sures, about 50 m a.s.l., 7S0 га /relatively dry/

No vegetation

Colonies of rosy-gray-brown algae

Plants cover 80-90 %. Saxifraga oppo-sitifolia L., Polygonum viviparum L., Salix polaris L., Silene acaulis L., Cerastium areticura Lange, Saxifraga caespitosa L. Colonies of brown-rosyish algae /about 40?•'/( moss - 155Ł /mainly last year' s/' Plants cover - 505i. Salix polaris L. , Saxifraga oppositifolia L., Silene acaulis L., Cerastium arcticum Lange, brown and white lichens

Gley soil Kith polygons arid stone circles, light silty loam ok heavy silty loam brown soil, nondifferentiatcd on the surface, light silty loan on heavy silty loamy sand Gley soil v.ith polygons and stone circles, light silty loam on medium loam Initial soil /lithosol/, light silty loam

10. Initial soil /lithosol/, light silty loam

11. Initial soil /lithosol/, light silty loam

Little flatness aLove the first root, outliers, SO n a.s.l., 1.3 kra

Slightly convex: elevation on lifted marine terrace, 144 m a.s.l., 1.6 l;m

Y/lde and flat depression declining toivards KNE, 140 m a.s.l., 1.65 km /fairly viet/

The flatness of the foot of Bohlin-ryggen, 165 r.i a.s.l., 1.9 km

fountain - side of HHV exposition, 250 m a.s.l., 2.35 km

fountain - side of 3ES exposition, Ибо ш a.s.l., 2.16 km x /

Cotraria sp., Saxifrage opnositifolia L., Salix polaris L., Silene aoai'lis L., Cerastium arcticun Lange, noss Plants cover - 2 5 D r y a s oc to petal a L., Saxifraga oppositifolia L., Salix polaris L., Polygonum viviparum L., Silone acaulls L., lichens Plants cover - 40fi. Saxifraga opnositi-folia L., Cerastium arcticum Lan-:e, lichens, algae Plants cover - 15f. Saxifraga opposi-tifolia L., Dryas octopetala L., Salix polaris L., Sileni acaulis L., Cetra-ria sp. Vegetation fragmentarily: Saxifraga oppositifolia L., Cetraria sp., Saxi-fraga caespitosa L., Cerastium arcticum Lange, moss Го vegetation

x/ distance in a straight line

Tab. 2. Granulometric composition and some chemical properties of the soils studied (1990).

Pro- Horizon, . Grain size content, 1-. „ „„ .. file depth Colour ' C a C 0 3 p H N o * / с и / ske- 1- 0.1- ^ ^ % /КС1/

leton 0.1 0.02 0.02 0.002 >1

1 0-6 10 УП 6/1 39 97 1 2 0 43.5 8.4 -

12-25 10 УН 6/1 41 91 2 6 1 45.0 8.5 -

32-43 10 YR 6/1 1 97 о 1 0 48.8 8.4 -

2 /А. / 0-1 10 YH 5/2 66 69 21 10 0 20.9 7.6 1.42 c 1 2-8 10 УК 6/3 96 72 18 10 1 19.2 8.0 0.47 D 20-30 10 У 7/1 85 17 29 54 17 30.2 8.1 0.41

3 0-2 10 УН 5/2 91 71 18 11 1 21.8 7.6 1.14 id 3-9 10 УЕ 6/3 70 57 30 13 0 21.8 7.6 0.87 С 13-20 2.5 У 6/2 43 71 16 13 1 22.0 7.9 0.72

4 0-3 2.5 У 5/3 67 72 15 13 0 2.7 7.6 1.09 cJ 5-12 5 У 5/2 64 54 35 11 0 2.7 7.6 1.56 CG 20-30 2.5 У 6/4 78 62 24 14 1 12.0 7.9 0.87

5 0-3 10 YR 4/3 61 60 30 10 2 0.4 6.2 1.69 (И1 5-Ю 10 УН 5/4 24 60 28 12 0 3.5 7.3 1.05 С 30-40 10 YH 6/3 58 80 7 13 1 30.1 7.9 0.54

6 А. С 0-3 5 У 5/2 38 36 34 30 3 10.8 7.6 0.93 ьЬ 10-15 5 У 6/2 40 20 27 53 12 12.4 7.7 0.62 DG 20-30 7.5 У 7/2 42 24 25 51 10 17.3 7.8 0.43

7 А1 0-3 10 У Р. 5/2 34 47 33 20 0 8.7 7.6 0.93 (HĆ Г.-12 10 УН 5/3 42 44 31 25 1 9.5 7.7 0.85

8 А. С 0-3 7.5 У 6/2 31 53 26 21 2 16.8 7.7 0.46 ci 10-1 5 2.5GY 6/1 27 38 24 38 5 17.4 7.9 0.29

9 АЧС 0-2 2.5 Y 6/3 44 37 30 33 1 17.2 7.7 0.78 С1 10-20 2.5 У 6/4- 37 37 31 32 2 10.0 7.7 0.51

10 А. С 0-3 5 V 5/2 57 46 27 27 0 14.4 7.6 1.29 С1 5-10 5 Y 6/2 78 49 25 26 0 16.8 7.6 0.99 С2 15-25 5 Y 6/2 88 40 34 26 1 20.2 7.9 0.42

11 А.С 0-2 2.5 Y 6/3 59 54 26 20 1 31.0 7.5 0.67 с 1 5-12 2.5 У 6/4 70 52 29 19 1 29.1 7.8 0.46

after Standard Soil Colour Charts /by II. Oyama, II. Talcehara, 1967/

142

Fig. 1. Cross section: Beach of Calypsostranda — Bohlinryggen. 1-11 — investigation sites, (A,) — humus horizon (initial), A t — humus horizon, AjC, A,(B), (B)C — transitional horizons, G — gley horizon, C, C p C2 — parent rock, D — underlying material.

u>