Stefan Bartoszewski, Zdzisław Michalczyk Wyprawy Geograficzne na Institute of Earth Sciences UMCS, Lublin 1991 Maria Curie-Sklodowska University Lublin, Poland Jan Magierski Institute of Soil Sciences Agricultural College Lublin, Poland

THE HYDROCHEMICAL CHARACTERISTICS OF THE NORTHERN PART OF WEDEL JARLSBERG LAND

In 1986-1990 the hydrological and hydrochemical studies were carried out on Spitsbergen during the Geographical Expeditions, UMCS. The field studies took place in the northern area of Wedel Jarlsberg Land bordered by the Bellsund coast in the West and Van Keulen Fiord in the North as well as the Dunder Valley in the South. The aim of the studies were hydrological and hydrochemical features of the area. The collected material was used for the preliminary characteristics of spatial and seasonal differentiations of physicochemical properties of water in different circulation phases: rainfall, glacial, surface and underground waters. The hydrochemical map (Fig. 1) presents the cartographic picture of different water qualities. Besides glaciers and mountain ridges, it shows the course of isoline of the water mineralization 100 mg/1 and water chemical structure. The water chemical structure was also presented in the records (Tables 1,2).

PROFILES OF GEOLOGICAL STRUCTURE AND RELIEF

The western part of the studied area is built of rocks of the Upper Proterozoic and Lower Paleozoic making the Hecla Hoek geological formation (Flood et. al. 1971, Dallmaun et. al 1990). The forms of the older foundation are strongly, tectonically disordered. Besides faults and thursts of WNW-SSE and NW-SE directions there are numerous folds. The geological configuration is close to the southern direction (Ohta 1982). The main types of rocks are tillits, phyllites and quartzites. Tillits are very differentiated as far as texture and mineralogy are concerned. Their main component is calcium carbonate (mostly calcite) but quartz, sericite and mica are also found (Chlebowski 1989). The geological medium is rich in calcium, magnesium and silica. In the upper and middle areas of the Chamberlin and Dunder Valleys besides tillits there are found large amounts of phyllites. Dolomites and quartzites occur along the eastern coast of the Recherche Fiord. 123 Between the entrance to the Van Keulen Fiord and Hornsund there is a boundary between the Caledonian structures and younger forms. Its course is characterized by unconformity, thrusts and faults resulting from the Tertiary folding (Dallmann et al. 1990). The eastern part of the studied area, the southern periphery of the Van Keulen Fiord is built of the series of the Upper Paleozoic and Mesozoic sediments. At the entrance of the Van Keulen Fiord there can be found the rocks of the Gipsdalen formation shaped as gypsum or dolomite coming from the and periods. Sandstones shales and mudstones Kapp Toscana Group from Trias and periods adjoin them in the eastern part. The rivers collecting water from the area of gypsums, dolomites and sandstones are of the increased mineralization. The mounatain massifs surrounding the Finsterwalder Glacier is built of shales, mudstones and sandstones (Janusfjellet Formation series) (Birkenmajer, Pugaczewska 1975, Różycki 1959). The maritime plains are built of loose Quaternary sediments formed as gravel, sand, marine silt, boulder clay (Dallmann et. al. 1990, Landvik, Salvigsen 1985, Pękala, Repelewska-Pękalowa 1990, Pękala, Reder 1989, Troicki et. al. 1979). Tectonics and geological structure constitute the relief. The course of main unglaciated valleys Dunder and Chamberlin resembles the system of faults and thrusts (Dallmann et. al. 1990). Their lower parts are the previous bays filled wit h delta sediments. The northern part of Chamberlindalen and Dunderdalen (from Grytdalselva outwash) is made of lifted marine terraces (Pękala 1988, Pękala, Repelewska-Pękalowa 1989). This type of relief can be also found in the maritime plains: Lognedalsflya, Dyrstadflya, Lyellstranda and Calypsostranda which surround the centre of the studied area. The middle part is occupied by the mountain massif, 500-800 m high and glaciers covering the mountain valleys: Renard, Scott, Blomli, Tjórn, Ringar, Logne and Crammer. The largest of them Renardbreen similar to the glaciers situated further to the East: Recherchebreen, Antoniabreen and Finsterwalderbreen has been in the stage of strong recession for the last decade (Koriakin 1974, Jania 1988).

METHODS

Water samples to be analyzed and measured were taken into plastic containers. While taking it, the temperature was measured and colour as well as transparency were determined in a visual way. The water ionic composition was determined in the field hydrochemical laboratory in Calypsobyen. Some samples were examined in the laboratory of the Soil Institute, Agriculture Academy, Lublin. In the field laboratory determination was made by titration (Markowicz, Pulina 1979). Water hardness and calcium content were determined by the versenate method while magnesium content was caculated from the

124 difference of general hardness and calcium amount. Hydrocarbons were determined using hydrochloric acid in the presence of methyl orange, chlorides by the argentometric method and sulfides by the versenate method with barium chloride. The water reaction was measured using the pH-meter Mera-Elwro N-5123. Sodium and potassium were calculated from ionic balance but some groups were determined in Lublin by the flame photometry using spectro- photometer Zeiss AAS-1 in the mode of the emission work. General mineralization was determined as a sum of ions from the electric conductivity measurement using the battery conductometer N-571 with PS-2 electrode. From the chemical compositions analysis and water conductivity measurements there was determined the numerical parameter 0.825 allowing to calculate water mineralization from the measured conductivity. The formula used was as follows:

M = к • 0.852 where M is the indicator of water mineralization in mg/1, к is the electric conductivity of water at 25°C in us/cm.

MATERIALS

Problems of differentiation and changeability of water physicochemical characteristics were presented in the papers by participants of the Geographical Expeditions to Spitsbergen, UMCS (Bartoszewski 1988, Bartoszewski, Repelew- ska-Pękalowa 1988, Bartoszewski, Magierski 1989, Bartoszewski et. al. 1988, Repelewska-Pękalowa, Magierski 1989, Michalczyk, Magierski 1990). The collected materials show spatial and seasonal differentiation of physicochemical characteristics of surface and underground waters. The stationary studies carried out in the basins of the Scott and Wydrzyca River (as being representatives) of different supply sources show almost identical seasonal rhythm of each period or studies. Similar conclusions can be drawn from the patrol measurements. The data analyzed in the paper were collected in the active hydrological season mainly in the polar summer. The waters of glacial origin were characterized by the lowest conductivity. The conductivity of waters coming from precipitation was 30-70 |iS/cm which was caused by the presence of sea water aerosols. The electrical conductivity was increased in the water contact with the bedrocks. The water from the molten ice taken from the land glaciers and the ice floating in the fiord had a conductivity of several |xS/cm. In the supraglacial underflows it increased to a dozen or so ^S/cm and in the waters flowing out of the glacial gates it was 60-90 |iS/cm. A farther contact with the background and permafrost water inflow showed increase in

125 conductivity up to 75-130 (iS/cm. In the rivers collecting waters from the unglaciated area the water electrical conductivity was 70-250 |iS/cm and in some cases it even exceeded 400 (iS/cm. Permatrost undeground waters flowing out of springs and taken from shallow piezometers were characterized by higher conductivity than the river waters. In the Calypsobyen region the undeground water conductivity in the measurement sites was from 200 to 350 |iS/cm and did not show great seasonal changes. The lowest conductivity was found at the beginning of studies and the highest in the end. In the initial stage of spring existance, conductivity might be higher due to dissolution of chemical com- pounds precipitated from the water while it was getting frozen. Intensity of hydrological and hydrochemical processes is dependent on air and water temperatures. The temperature of waters flowing over the glacier and flowing out of the glacier gates was about 0.5°C. A slow temperature increase was observed with the farther river course e.g. in the estuary profile of the glacial River Scott the mean temperature was 2.8°C with the extreme values 0.4 and 4.6°C. The temperature in small periglacial rivers was several degrees, most frequently below 5°C. In small lakelets the temperature in the active hydrological season was from 0.8 to 13.2°C and in those of small water exchange from 0.4 to 8.0°C. The temperature of permafrost waters taken from piezometers was 1-2°C and those outflowing in springs 1-4°C (Michalczyk, Magierski 1990). The waters occurring in the studied area of Spitsbergen are poorly minerali- zed. Most frequently they are ultrasweet waters. The waters coming from glaciers are of the lowest mineralization — several mg/1. The waters are more concentrated with the components in a contact with the material deposited on the glacier and the bedrock. Mineralization of the waters flowing out from glaciers in most cases did not exceed 100 mg/1. Similar mineralization is found in the waters flowing in the rubble covering the mountain sides. The map (Fig. 1) shows the course of mineralization isoline 100 mg/1, characteristic for the polar summer. It covers mountain sides and ridges as well as valley glaciers i.e. areas of the water lowest mineralization. At the beginning of the active hydrological season, the isoline probably runs closer to the coasts. After significant diminishing of snow supply, the isoline gets farther from the sea. The highest mineralization of waters is observed in the end of the active hydrological season. The chemical composition of waters flowing in the northern part of Wedel Jarlsberg Land is related to the kinds of feeding and the ground geological structure. The proglacial waters are characterized by the least differentiation of physicochemi- cal features. It is particulary evident in the case of proglacial underflows, the water mineralization of which is about 20 mg/1. In its chemical compositon besides anions, there can be found HC03 which takes up about 2/3 of milival sums of anions. Among cations, the amounts of calcium, magnesium and sodium are low and on the same level (Tab. 1). Much lower mineralization of proglacial waters than those from precipitations found in the coast area is observed.

126 The waters flowing out in the glacial gates come from the drainage in- and subglacial system. The total mineralization of the waters is 68-117 mg/1 with the the average 94 mg/1. Despite a large lithological differentiation of the forms being the background of the glaciers studied only in the case of Antoniabreen the water mineralization was different from the average which may by coused by readily soluble dolomites occurring in the basin. In the chemical composition of glacial waters HC03 ion is predominant constituting 70-80% of milival sums of anions and Ca ion which constitutes half of milival sums of cations. The share of magnesium is 30-45% and sodium a few per cent of milival sums of cations. The average chemical composition of the waters flowing out from glaciers is as follows:

HCO74 CI20 SOf M0-09 - - Ca50 Mg37 Na10 K3

The chemical composition of glacial river waters is given in Tab. 2. In the case of the waters flowing directly from the glacier, the increase of total mineraliza- tion is observed due to the background leaching and inflow of more mineralized permafrost waters. The isoline 100 mg/1 separates the areas of greater snow- -glacial - low mineralization water supply from those of permafrost supply (Fig. 1). The position of the isoline changes with the development of hydrological processes dependent on air temperature. The glacial rivers are mostly transit in their low parts and they do not accept large inflows. The escape of river waters in to gravel forms padding the valley bottom is observed. The glacial rivers transport large amounts of material particularly during freshed periods. The waters are of bright brown colour from the suspensions being transported and weak transparency. The water is weakly alkaline and the total mineralization is 90-140 mg/1. Similar to superglacial waters, HC03 ion whose share is 76-85% of milival sums of anions is predominant. Among cations, the greatest number are Ca ion 34-60% and Mg 33-45% (in the Blomli River waters the amount of magnesium was 69%) of milival sums. The average chemical composition the river waters carried away from the glaciers is:

HCO7,9 CI16 SO,5 0.11 M Ca51 Mg40 Na8 K2

The waters of peri glacial rivers transport less dissolved or suspended material and are characterized by great transparency and weak alkaline reaction. Their total mineralization is 150-200 mg/1 which is much higher than in the glacial rivers. The quantity of hydrocarbons and calcium increases. Among anions, the share of HC03 ion is greater up to 77-87% of milival sums. The share of Ca ion

127 is 40-60% and Mg 20-50% of milival sums of cations. The water chemical composition of the rivers collecting waters from unglaciated areas is as follows:

HCO8,1 CI15 sot jyjo.16 Ca56 3 Mg36 Na47 K1

The relation between physicochemical characteristics of water and geological structure can be seen in the unglaciated basins. Dunderelva is a characteristic example. In its upper part, it is supplied by numerous streams dewatering cryoplane terraces as well as rock glaciers. Water mineralization increases from a spring to a characteristic ravine through outcrops of chlorite shales. Below the ravine as a result of water inflow from small glaciers, the amount of the dissolved substances decreases. The eastern part of valley built mainly of dolomites supplies more mineralized waters of 200-350 mg/1. In the lower part the total mineralization of the river water increased in spite of inflow of less mineralized waters from the Crammer Glacier. This phenomenon was recorded for the first time in 1986 (Bartoszewski 1988). The chemical composition of permafrost waters was studied in a more detailed way only in the region of Calypsostranda. Mineralization of permafrost waters was from 180 to 300 mg/1, temperature was kept at 1-3°C and the water reaction was weakly alkaline, pH was about 8. In most water samples taken from springs and piezometers HC03 ion which constitutes 68-88% of milival sums of anions is predominant. The share of CI ion is several per cent of milival sums of anions. Among cations, Ca ion takes more than half of milival sums. The share of Mg ion is 30-40% and Na ion is several per cent of milival sums of cations. The chemical composition of the underground waters is as follows: the spring in Calypsobyen, September 10, 1988

HCO85 C11S M0.23 3 Ca53 Mg40 Na6 K1 the spring in Klokke, September 12, 1988

HCO88 CI12 jy[0.23 Ca57 Mg35 Na7 K1

CONCLUSIONS

The waters circulating in the northern part of Wedel Jarlsberg Land show little physicochemical differentiation. A relatively small petrographic variety of

128 the rocks near the surface causes the quantitative but not qualitative character of the changes. The water total mineralization depends on the kind of feeding. The smallest amount of the dissolved substances is transported by the waters coming from the surface flow within the glaciers (superglacial waters). The waters coming from the subglacial drain system are enriched in the substances leached from the glacier grounds. Further increase of proglacial water mineralization is due to inflow of the water of permafrost origin. The air temperature affects hydrological and hydrochemical processes. The boundary of the area with predominant glacial-snow and permafrost supply is of a zone character. Its situation during the polar summer is illustrated by the isoline of mineralization 100 mg/1. Lower mineralization is observed in the mountain i.e. in the area of glacial and snow supply. All waters in the studied area are poorly mineralized, of weakly alkaline reaction and low temperature. The analysis of their chemical composition show that independent of their origin, a hydrocarbon ion among anions and calcium and magnesium ions among cations are predominant. The gratest changes of chemism occur at the beginning and in the end of the active hydrological season. In the polar summer the chemical composition of waters was stable in each measurement site. The relation between the hydrochemical features and ground geological structure is most obvious in the unglaciated basins. The waters are characterized by higher mineralization and higher HC03, Ca, Mg ions concentration than proglacial waters.

REFERENCES

Bartoszewski S., 1988: Water balance, temperature and mineralization of periglacial waters in Bellsund region, Spitsbergen, summer 1986. Pol. Polar Res., 9, 4. Bartoszewski S., Repelewska-Pękalowa J., 1988: Mineralizacja ogólna i zmętnienie w wybranych zlewniach rzek rejonu Bellsundu. Wyprawy Geograficzne na Spitsbergen, UMCS Lublin. Bartoszewski S., Rodzik J., Wojciechowski K., 1988: The outflow of water in permafrost enviroment — Spitsbergen. V International Conference on Permafrost, Tróndheim, . Birkenmajer K., Pugaczowska H., 1975: Jurassic and Lower marine fauna of SW Torell Land, Spitsbergen. Studia Geologica Polonica 44. 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., Ćraddock C., 1990: Geological map of 1:100 000, Sheet В 11G Van Keulenfjorden. Norsk Polarinstitutt, Oslo. Flood J., Nagy J., Winsnes T. S„ 1971: Geological map of Svalbard 1:500 000, Sheet 10. Spitsbergen southern part. Norsk Polarinstitutt Oslo. Jania J., 1988: Dynamiczne procesy glacjalne na południowym Spitsbergenie w świetle badań fotointerpretacyjnych i fotogrametrycznych. Prace Naukowe UŚ 955, Katowice.

129 Koriakin W. S., 1974: Izmenenie rozmierow lednikow Szpicbergena (Svalbarda). Materiały issledowanij oblastii oledenenia Szpicbergena (Svalbarda). Akademia Nauk SSSR, Moskwa. Landvik J. Y., Salvigsen O., 1985: Glaciation development and interstadial sea-level on central Spitsbergen. Polar Research, 3. Markowicz M., Pulina M., 1979: Ilościowa półmikroanaliza chemiczna wód w obszarach krasu węglowego. Prace Naukowe UŚ, 289, Katowice. Michalczyk Z., Magier ski J., 1990: Physicochemical properties of waters as well as chemical and mechanical denudation of Calypsostranda region (Western Spitsbergen). Wyprawy Geograficzne na Spitsbergen, UMCS Lublin, Pękala К., 1987: Rzeźba i utwory czwartorzędowe przedpola lodowców Scotta i Renarda (Spitsbergen). XIV Sympozjum Polarne, Lublin. Pękala K., Reder J., 1989: Rzeźba i osady czwartorzędowe Dyrstaddalen i Lognedalen (Zachodni Spitsbergen). Wyprawy Geograficzne na Spitsbergen. UMCS Lublin. Pękala K., Repelewska-Pękalowa J., 1988: Główne rysy rzeźby i osady czwartorzędowe doliny Chamberlin (Spitsbergen). Wypawy Geograficzne na Spitsbergen, UMCS Lublin. Pękala K., Repelewska-Pękalowa J., 1990: Relief and of Quaternary deposits in the region of Recherche Fiord and southern Bellsund (Western Spitsbergen). Wyprawy Geograficzne na Spitsbergen. UMCS Lublin. Repelewska-Pękalowa J., MagierskiJ., 1989: Czynna warstwa zmarzliny, dynamika i właściwości chemiczne wód, Calypsostranda, sezon letnio-jesienny 1988. Wyprawy Geograficzne na Spitsbergen UMCS Lublin. Różycki S. Z., 1959: Geology of the north-western part of Torell Land, Vest Spitsbergen. Studia Geologica Polonica, 2. Troicky L., Punning J. M., Hiitt G., Rajamae R., 1979: Pleistocene glaciation chronology of Spitsbergen. Boreas. 4.

STRESZCZENIE

Wody krążące w północnej części Ziemi Wedel Jarlsberga wykazują małe zróżnicowanie cech fizykochemicznych. Stosunkowo niewielkie urozmaicenie petrograficzne skał powoduje, że stwier- dzone różnice mają przede wszystkim charakter ilościowy, a nie jakościowy. Mineralizacja ogólna wód wiąże się z rodzajami alimentacji. Najmniejszą ilość substancji rozpuszczonych transportują wody pochodzące ze spływu powierzchniowego w obrębie lodowców. Wody pochodzące z drenażu subglacjalnego wzbogacają się w substancje ługowane z podłoża lodowców. Dalszy wzrost mineralizacji wód proglacjanych następuje wskutek dopływu wód zmarzlinowych. O przebiegu procesów hydrologicznych i hydrochemicznych decyduje przede wszystkim temperatura powietrza. Granica obszarów o przewadze zasilania lodowcowo-śnieżnego i zmarzlinowego ma charakter strefowy. Jej położenie w okresie lata polarnego ilustruje izolinia mineralizacji 100 mg/l. Wszystkie wody występujące na badanym obszarze są słabo zmineralizowane, mają odczyn słabo zasadowy i wykazują niską temperaturę. Analiza składu jonowego świadczy, że niezależnie od pochodzenia wód, wśród anionów dominuje jon wodorowęglowy, a wśród kationów jony wapnia i magnezu. Największe zmiany chemizmu wód stwierdzono na początku i w końcowym okresie czynnego sezonu hydrologicznego. Pcfdczas polarnego lata skład chemiczny wód w poszczególnych punktach pomiarowych był ustabilizowany. Związek cech hydrochemiczych z budową geologiczną podłoża jest najbardziej widoczny w zlewniach niezlodowaconych. Wody w nich występujące cechują się znacznie większą mineralizacją, wyższą koncentracją jonów: wodorowęglanowego, wapniowego i magnezowego niż wody proglacjalne.

130 Tab. 1. Chemical composition of the precipitation, glacial and ground water

Ions № Water from Date M нсо3 CI so4 Ca Mg Na К mg/1

1 Iceberg Recgerchebreen 30 9 88 23 8 9 0 1 1 3 1 2 Dead ice Recherchebreen 28 7 89 66 29 6 11 6 1 13х Supraglatial streams: 3 Scottbreen 29 8 88 26 15 4 0 3 2 2 0 4 Renardbreen 5 9 88 20 12 2 0 2 1 3х 5 Tjornbreen 24 7 90 17 6 Antoniabreen 11 7 90 59 23 12 5 1 2 16х Subglatial streams: 7 Scottbreen 18 7 88 95 63 8 2 11 7 2 2 8 Renardbreen 18 8 88 79 57 7 0 10 4 1 о х 9 Tjornbreen 24 7 90 103 63 7 5 13 2 13 10 Antoniabreen 11 7 90 117 58 14 13 15 4 13х 11 Ringarbreen 29 7 88 87 55 9 0 9 3 11х 12 Lognebreen 24 7 88 86 55 9 0 7 4 11х х 13 Glottfonna 24 7 88 104 57 14 5 7 4 17 14 Recherchebreen 23 7 90 101 57 8 5 15 8 8х 15 Finsterwalderbreen 23 8 88 68 46 6 1 9 4 1 1 Calypsobyen - rain 16 7 88 65 31 17 2 5 5 4 1 х Wi jkanderberg. - snow 12 9 88 53 31 8 0 3 4 7 Permafrost water: Calypsobyen - spring 16 7 88 221 151 15 4 ,32 11 7 1 х Calypsobyen - piezometer 20 .7 90 315 209 24 0 35 10 37 16 Klokkefiellet - spring 12 .9 88 182 130 10 0 28 10 4 0

17 Dyrstaddalen -high lake 25 .7 88 81 55 9 2 11 3 1 0 18 Dalt jorna- 19 .9 88 157 122 7 0 14 11 3 0 19 Kraken lake 19 .9 88 159 109 10 4 22 10 4 0

x calculated from the ion balance

131 Tab. 2. Chemical composition of the river water.

Ions

№ Water from Date M нсо3 CI S04 Ca Mg Na К mg/1 Glacial basins: 20 Scottbreen 11 .9 88 103 61 8 4 17 9 3 1 21 Tjornbreen 24 .7 90 106 57 11 9 11 4 14х 22 Dyrstad 25 .7 88 103 67 9 0 13 4 10х 23 Lognebreen 24 7 88 116 73 9 5 9 6 14х 24 Dolterbreen 7 8 88 102 69 8 0 11 5 9х 25 Dunderbreen 15 8 88 82 46 5 7 15 5 3 1 26 Libreen 15 8 88 47 29 5 0 6 7 0х 27 Saksbreen 15 8 88 109 66 6 4 24 9 0х 28 Blunkebreen 31 7 90 96 57 10 4 12 3 10х Rivers from rock glaciers: 29 Beisdalen 24 7 88 135 85 11 5 14 7 13х 30 Hamardalen 24 7 88 116 79 7 1 11 5 13х 31 Dunderfjellet 27 7 90 202 107 13 26 25 6 25х 32 Beisknatten 27 7 90 124 76 11 4 18 4 11х 33 Grytdalen 27 7 90 139 87 13 4 19 7 9х 34 Konglomeratfiellet 15 8 88 93 61 6 0 19 7 0х Unglaciated basins: 35 Wydrzy.ca stream 18 7 88 166 119 12 0 23 9 3 0 36 Reinder stream 11 9 88 197 134 14 2 30 12 5 0 37 Dyrstrddalen stream 7 8 88 120 79 11 0 14 6 10х 38 Kolvebekken 7 8 88 192 137 10 0 27 10 8х 39 Dundrabeisen stream 19 9 88 176 121 11 5 24 10 5 0 40 Dunderelva 7 8 88 109 75 9 2 12 11 0х 41 Livdeggbekken 7 8 88 126 88 8 0 15 7 8х х 42 Trinutpasset 15 8 88 62 38 8 1 8 5 2 43 Chamberlinelva - estuary 25 7 88 137 95 9 0 25 6 2 0 44 Chamberlinelva - middle part 25 7 88 72 49 10 0 9 2 1 1 45 Chamberlinelva - ravine 25 7 88 100 70 10 0 13 5 2 0 х 46 Chamberlinpasset 15 8 88 41 23 9 0 4 5 0 47 Observatoriefjellet stream 20 7 88 122 76 8 7 24 4 2 1 х 48 Reinsletta stream 11 7. 90 232 160 15 0 32 10 15 49 Jarnbekken stream 18 7, 89 100 57 10 7 9 6 11* 50 Kapp Toscana stream 18 7 89 333 214 23 12 65 io 9х 51 Finsterwalderbreen stream 23 8 88 351 - outer outwash

calculated from the ion balance

132 Fig. 1. Chemical composition of waters in the northern part of Wedel Jarlsberg Land: 1 — glaciers, 2 — rivers, 3 — mountain ridges, 4 — sites of water sample taking, 5 — isoline 100 mg/1, 6 — ionic composition 133