Summary of the Overburden Studies of the Soil Pits OL-KK14 ... · Summary of the overburden studies...

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Anne -Ma j Lahdenperä

December 2009

Work ing Repor t 2009 -109

Summary of the Overburden Studies ofthe Soil Pits OL-KK14, OL-KK15, OL-KK16,

OL-KK17, OL-KK18 and OL-KK19at Olkiluoto, Eurajoki in 2008

December 2009

Base maps: ©National Land Survey, permission 41/MML/09

Working Reports contain information on work in progress

or pending completion.

The conclusions and viewpoints presented in the report

are those of author(s) and do not necessarily

coincide with those of Posiva.

Anne -Ma j Lahdenperä

Pöyry Env i ronment Oy

Work ing Repor t 2009 -109

Summary of the Overburden Studies ofthe Soil Pits OL-KK14, OL-KK15, OL-KK16,

OL-KK17, OL-KK18 and OL-KK19at Olkiluoto, Eurajoki in 2008

Summary of the overburden studies of the soil pits OL-KK14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 and OL-KK19 at Olkiluoto, Eurajoki in 2008.

ABSTRACT

The report summarises the geochemical and geotechnical properties of the soil pits

OL-KK14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 and OL-KK19 investigated at

the Olkiluoto Island in 2008. The aim was to get more information on the soil

stratigraphy and geochemistry in the geosphere-biosphere interface and for the

overburden modelling purposes.

The new soil pits OL-KK14…OL-KK16 situated in central, eastern and northern parts

of the Olkiluoto. The OL-KK17…OL-KK19 situated close to each other in the

infiltration experiment site near the ONKALO underground rock characterisation

facility and the Korvensuo reservoir.

Due to the Baltic Sea stages, the soils at Olkiluoto are young, and the soil horizons are

not well developed, thus the sampling horizons were mainly selected after visual

examination. At total, 25 samples were taken from the vertical profiles of soil pits, dug

by the excavator, from the humus and from two to five different mineral horizons.

Overburden of the investigated soil pits was fine-grained and sandy till. Sand and clay

layers were common, and some soil layers were stony. pH values varied in the humus

layers from 3.3 to 5.4. In the mineral soil layers pH increased as a function of depth,

which is typical for the Finnish soil profiles. The solubility of most analysed elements

(Al, Ba, Ca, Co, Cr, Fe, K, Mg, Mn, Na, Ni, P and Zn) was significantly higher in the

humus layers than in the mineral soil layers. Calcium and magnesium were the

dominating nutrients. The cation exchange capacity was the highest in the humus

horizons of OL-KK16 and OL-KK17, OL-KK19 was the most nutrient-poor of the

studied sites.

The geochemical and geotechnical properties of investigated soils were heterogeneous,

even in the three soil profiles (OL-KK17…OL-KK19) sampled close to each other.

The humus horizon properties, the amount of the clay and fine fraction contents in

different soil pits and within the soil layers affect geochemical and hydrological

properties and thus soil pedogenic processes.

Keywords: Overburden, geochemistry, grain size distribution, cation exchange capacity, element solubility

Yhteenveto tutkimuskuoppien OL-KK14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 ja OL-KK19 maaperätutkimuksista Olkiluodossa 2008.

TIIVISTELMÄ

Raporttiin on koottu yhteenveto Olkiluodossa 2008 tehtyjen tutkimuskuoppien OL-

KK-14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 ja OL-KK19 maaperän

geokemiallisista ja -fysikaalisista ominaisuuksista. Tutkimus antaa lisätietoa

Olkiluodon maaperän stratigrafiasta ja geokemiallisista ominaisuuksista geosfääri-

biosfääri rajapinnassa ja tuloksia käytetään maaperämallinnuksen tarpeisiin.

Tutkimuskuopat OL-KK14…OL-KK16 sijaitsivat saaren keski-, pohjois- ja itäosissa ja

OL-KK17…OL-KK19 maanalaisen loppusijoitustilan, ONKALOn ja Korvensuon

altaan läheisyyteen perustetulla suotaumakoealueella.

Itämeren vaiheista johtuen Olkiluodon maaperän maannoshorisontit ovat nuoria ja

siten heikosti kehittyneitä, joten maaperänäytteet valittiin maaperän eri ominaisuuksien

perusteella. Näytteet otettiin kaivinkonekuopista sekä humuskerroksesta että kahdesta

viiteen mineraalimaakerroksesta. Näytteitä otettiin yhteensä 25 kappaletta.

Tutkimuskuoppien maaperä oli hienoainesmoreenia tai hiekkamoreenia. Savi- ja

hiekkakerrokset olivat yleisiä ja paikoin esiintyi kivisiä maaperäkerroksia. Humus-

kerrosten pH vaihteli 3,3-5,4. Mineraalimaakerroksissa pH kasvoi maannoshorisontin

syvyyden mukaan, mikä on tyypillistä suomalaisille maannoksille. Useimpien alku-

aineiden (Al, Ba, Ca, Co, Cr, Fe, K, Mg, Mn, Na, Ni, P ja Zn) liukoisuus oli

huomattavasti suurempi humuskerroksissa kuin mineraalimaakerroksissa. Kalsium ja

magnesium olivat pääravinteet. Tutkimuskuoppien OL-KK16 ja OL-KK17 maaperä oli

ravinnerikkainta, OL-KK19 oli ravinneköyhin. Kationinvaihtokapasiteetti ja emäs-

kylläisyysaste vaihtelivat tutkimuskuopittain ja eri maaperäkerroksittain.

Suotaumakoealueella lähekkäin sijaitsevien tutkimuskuoppien (OL-KK17…OL-

KK19) geokemialliset ominaisuudet vaihtelivat huomattavasti. Tutkimuskuoppien geo-

kemiallisten ja -fysikaalisten ominaisuuksien vaihteluun ja maannostumisprosesseihin

vaikuttavat humuskerrosten ominaisuudet, savi- ja hienoainespitoisuuden määrät.

Avainsanat: Maaperä, geokemia, raekoostumus, kationinvaihtokapasiteetti, alku-aineiden liukoisuus

1

TABLE OF CONTENTS

ABSTRACT

TIIVISTELMÄ

1 INTRODUCTION ............................................................................................. 3

1.1 Soil pits OL-KK14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 and ........ 3

OL-KK19 ......................................................................................................... 3

1.2 Overburden properties at Olkiluoto ...................................................... 4

1.3 Earlier overburden studies at Olkiluoto Island ...................................... 7

2 MATERIALS AND METHODS ....................................................................... 11

2.1 Soil sampling and soil profile description ........................................... 11

2.2 Analysis of the samples ..................................................................... 22

3 RESULTS ..................................................................................................... 25

3.1 Geochemical and geotechnical analyses ........................................... 25

3.1.1 Basic properties ..................................................................... 25

3.1.2 Main exchangeable nutrients .................................................. 30

3.1.3 Easily leachable trace elements ............................................. 34

3.1.4 Main trace elements in total digestion .................................... 37

3.1.5 Easily leachable metal concentrations in partial digestion ...... 38

3.1.6 Other metal concentrations in total digestion .......................... 41

3.1.7 Iodine and selenium ............................................................... 43

3.2 Cation exchange capacity (CEC) and base saturation (BS) ............... 45

3.3 Solubility of the main elements .......................................................... 51

3.4 Grain size distribution and mineralogy ............................................... 54

4 CONCLUSIONS ............................................................................................ 55

5 SUMMARY .................................................................................................... 57

REFERENCES ......................................................................................................... 59

APPENDICES .......................................................................................................... 65

3

1 INTRODUCTION

Posiva Oy is responsible for implementing a final disposal repository programme for

spent nuclear fuel from Finnish nuclear power plants operated by Teollisuuden Voima

Oy and Fortum Power and Heat Oy. The spent nuclear fuel is planned to be disposed in

a KBS-3-type repository to be constructed at a depth between 400 and 600 meters in

crystalline bedrock at Olkiluoto. The suitability of Olkiluoto for the repository has

been investigated over a period of twenty years by means of different ground and

airborne methods (Posiva 2009).

Following the guidelines set forth by the Ministry of Trade and Industry (now Ministry

of Employment and Economy) Posiva Oy is preparing the next step of nuclear

licensing of the repository, which is to submit the construction license application for

spent fuel repository by the end of year 2012.

The overburden properties are of interest both for understanding of the site evolution

and for radionuclide transport analyses. The overburden changes the composition of

the infiltrating water and thus affects also the deeper groundwater. In the recent

radionuclide transport analysis (Hjerpe et al. 2009), radionuclide transport through the

geosphere-biosphere interface and further in the overburden has been explicitly

modelled (Karvonen 2009).

In the context of the transport of potential releases from the repository, the geosphere-

biosphere interface (GBI) is a zone where the changes from bedrock up to bioavailable

region takes place (without gaps in the top bedrock, overburden, and aquatic

sediments) (Lahdenperä 2006). As well, the opposite direction, infiltration from the

biosphere to the deep groundwater is important. The depth of the zone can vary greatly

depending on the media of the flow path and a wide variety of other reasons, such as

topography and contrasts in the hydraulic conductivity. The most important factor

determining the transport of radionuclides is the water balance of the system

(Haapanen et al. 2009).

1.1 Soil pits OL-KK14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 and OL-KK19 The report summarises the geochemical and geotechnical properties of the soil pits

OL-KK14, OL-KK15, OL-KK16, OL-KK17, OL-KK18 and OL-KK19 investigated at

the Olkiluoto Island in 2008 (Figure 1). The aim was to get more information on the

soil stratigraphy and geochemistry in the geosphere-biosphere interface and for the

overburden modelling purposes.

The new soil pits OL-KK14, OL-KK15 and OL-KK16 situated in the different parts of

the Olkiluoto. The OL-KK14 located near the main Olkiluoto road and the shallow

groundwater tube OL-PP39 (Pitkänen et al. 2008a), close to the Liiklansuo mire. The

gravitation plate lysimeters were installed in the pit OL-KK14 by the Finnish Forest

Research Institute. The OL-KK15 situated in the north of island, near the harbor. It

situated close to birch-dominated forest soil and vegetation sampling plot and to the

4

surface field survey line 2. This surface field survey included surficial study (< 1 m

depth) of the soil type and of vegetation mapping during the summer 2008 (Haapanen

& Lahdenperä 2009). The OL-KK16 situated in the north-eastern part of the island,

beside the Rumminperäntie road, near the spruce-dominated forest soil and vegetation

sampling plot and the surface field survey line 3. The supervisor of the pits OL-

KK14...OL-KK16 was PhD, hydrogeochemist Anne-Maj Lahdenperä from Pöyry

Environment Oy.

The three soil pits OL-KK17, OL-KK18 and OL-KK19 were dug in the infiltration

experiment site (Pitkänen et al. 2008b); near the ONKALO underground rock

chracterisation facility and the Korvensuo freshwater reservoir of the power plant

(Figure 1). The supervisor of the pits OL-KK17…OL-KK19 was MSc, geologist

Susanna Lindgren from Posiva Oy. The gravitation plate lysimeters were also installed

in these pits by the Finnish Forest Research Institute. The soil water results are not

presented in this report.

1.2 Overburden properties at Olkiluoto

Due to continuous land uplift at Olkiluoto, currently at the rate of 6–6.8 mm/y (Eronen

et al. 1995, Kahma et al. 2001), about thousand years ago many of the initially small

islands were interconnected into a bigger island and the Olkiluoto Island has begun to

get its present shape (Mäkiaho 2005). The effects of the land uplift are accentuated by

a rather flat topography and anthropogenic eutrophication of the coastal Baltic Sea,

which increases primary production, and consequently accumulation of organic matter

especially in shallow bays. The development of the shoreline will induce changes in

the local biosphere conditions, such as biosphere succession, sediment redistribution

and groundwater flow. These will in turn influence soil properties and again the

positions of the groundwater recharge and discharge areas (Haapanen et al. 2007,

2009).

The bedrock of Olkiluoto mostly comprises high-grade metamorphic supracrustal

rocks. According to the mineral composition, texture and migmatite structure, the

rocks of Olkiluoto have been divided into following rock types: i) the metamorphic

rocks including various migmatitic gneisses and homogenous, banded or weakly

migmatised gneisses, such as mica gneisses, quartz gneisses, mafic gneisses and

tonalitic-granodioritic-granite gneisses and ii) the igneous rocks comprising abundant

pegmatite granites and sprodadic narrow diabase dykes (Kärki & Paulamäki 2006).

The bedrock surface is variable, but the ground surface is quite smooth, even in the

places where the bedrock topography changes abruptly. As a result of last glaciation

the bedrock depressions are filled with thicker layers of overburden, mainly sandy till

and fine-textured till (Lahdenperä et al. 2005). The other terrestrial sediment types are,

in order of abundance, fine sand, sand, silt and clay. The thickness of the overburden is

usually 2-4 meters, although even up to 12-16 meter thick layers have been observed.

Some Litorina and Ancylus clay areas exist in addition to the areas of recent mud cover

especially at the northern and southern side of island (Haapanen et al. 2009).

5

Olkiluoto Island is relatively flat, with the average elevation of Olkiluoto being about 5

m above sea level. The bedrock highpoints, which are not covered by the late glacial

deposits, protrude through the soil layers. The highest points of Olkiluoto Island are

Liiklankallio (18 m), Selkänummenharju (13 m) and Ulkopäänniemi (12 m)

(Lahdenperä et al. 2005). Most of these exposed rock surfaces are facing west, which

has been the direction of most effective wave action during the shoreline phase

(Seppälä 2005).

The predominant soil-forming process in Finland is podzolization of mineral soils,

leading to leached and acidic soils with an organic layer overlying the mineral soil;

peat soils with a peat layer of varying thickness (Histosols); very shallow soils

(Leptosols); young soils (Arenosols or Regosols) and fine-textured soils (Cambisols).

Soil classification and detailed soil reflect the development of specific soil (Lilja et al.

2006, Tamminen et al. 2007).

Podzolisation, the natural acidification of soils, is a slow process that started on the surficial parts of supra-aquatic mineral soil after Weichselian glaciation, about 10 000–9000 years ago in Finland (Donner 1995). Owing the evolution of Baltic Sea, the oldest podzols are in supra-aquatic areas of northern and eastern Finland. The soils at Olkiluoto are poorly developed due to the short time span of land uplift and developed 0-3000 years ago (Mäkiaho 2005, Haapanen et al. 2009). According to Jauhiainen (1973) and Starr (1991) it takes 500 to 1500 years for a podzol to develop on sorted sands along the coast of Gulf of Bothnia.

Figure 2 illustrates the structure and horizons of a podzol profile and main processes. The high moisture content, high incidence of anaerobic conditions and poor decomposability of plant litter have resulted in gradual accumulation of organic layer comprising acidic, partially decomposed litter and humus in the surface layer (O). The composition of organic compounds varies widely, depending on the vegetation and soil properties (Brady 1984). Podzolic soils are characterized by light coloured eluvial surface soil (A), a horizon immediately below the organic layer, and a reddish subsoil (B), illuvial horizon below the A-horizon. The eluvial horizon has been leached by acid percolation water and is low in base cations. Iron and aluminium are removed as colloids incorporated by clay minerals or as organometallic complexes, mainly in illuvial horizon. Podzolized till soils are heterogeneous in chemical, mineralogical and physical properties (Kontio & Kähkönen 1991).

Figure 1. Soil investigation sites at the Olkiluoto Island described in this report. Soil test pits (OL-KK14…OL-KK19) are marked with red

dots (layout by Jani Helin/Posiva Oy).

6

7

Figure 2. Structure and horizons of a podzol profile: a) podzol profile and circulation of water, b) owing to electrolytes dissolved from the eluvial horizon, the pH of the runoff water increases in the illuvial horizon and transition zone, precipitating aluminium, iron and silicon compounds, c) cation exchange is most intense in the humus and eluvial horizons, and the chemical weathering of minerals in the transition zone and weakly altered parent material. Modified after Strahler (1970) and Jacks et al. (1984) by Teea Penttinen/Pöyry Environment Oy.

1.3 Earlier overburden studies at Olkiluoto Island

The current knowledge on overburden is based on several independent studies and no

systematic mapping covering the Olkiluoto area has been conducted. Direct point

observations are available from several sources, but they sites are mainly concentrated

on the central part of the island (Lintinen et al. 2003, Lintinen & Kahelin 2003, Posiva

2003, Lahdenperä et al. 2005, Huhta 2005, 2008, 2009). The following overburden

studies have been done since 1999 at Olkiluoto:

Data of overburden physical, mineralogical and chemical properties from the

deep soil pits OL-KK1…OL-KK13 (Figure 1), dug by excavator, and

investigated from different depths using standard procedures have been studied

by Hagros (1999), Lintinen et al. (2003), Lintinen & Kahelin (2003) and

summarised in Lahdenperä et al. (2005). The soils were sandy till, containing

some clay, sand, gravel and weathered layers. In some pits till was more stony

or compact, especially in deeper horizons. Two chemical digestions were used

for soil samples to evaluate different environmental conditions. In Table 1

8

some geochemical results digested by synthetic rainwater, organic matter and

water contents of the soil pits OL-KK6…OL-KK13 (Haapanen et al. 2009) are

presented. Synthetic rainwater used in Lintinen et al. (2003) and Lintinen &

Kahelin (2003) is weaker digestion than the ammonium acetate digestion used

for the analyses of OL-KK14-OL-KK19, thus the results are not fully

comparable.

Table 1. Geochemical and some geotechnical characteristics of mineral soil

samples from the surface horizons and C-horizons of the soil pits OL-KK6...OL-

KK13 extracted by synthetic rainwater at Olkiluoto. Median and in parentheses the

range of values (based on data from Lintinen et al. 2003, Lintinen & Kahelin

2003).

Variable Surface soil

horizons N C-horizon N

pH 6.5 (4.0-8.0) 19 7.5 (6.5-8.0) 8

Anions mg/kg

Cl <2-2.8 6 <2 2

F 1-2.0 6 <1-2.1 2

NO3 <2 6 <2 2

SO4 11.0 (1.7-19.0) 6 13.0-36.0 2

Cations mg/kg

Al 8.9 (0.6-24.4) 25 8.0 (0.6-15.2) 8

Ca 22.9 (6.4-79.6) 25 39.3 (18.5-118) 8

Cs <0.05 25 <0.05 8

Fe 9.0 (0.2-32.2) 25 7.2 (0.6-20.3) 8

K 10.9 (4.8-27.0) 25 22.2 (9.1-31.0) 8

Mg 4.8 (2.6-10.3) 25 5.8 (3.2-12.5) 8

Na 5.1 (2.8-14.0) 25 5.4 (4.1-9.4) 8

Sr 0.04 (0.001-1.4) 25 0.08 (0.02-0.2) 8

U 0.01 (<0.01-

0.08) 25

<0.01 (<0.01-

0.02) 8

Geotechnical

analyses

Water content

(weight-%) 9.5 (6.5-18.6) 25 10.9 (8.1-15.3) 8

Organic matter

% 1.1 (0.5-3.13) 25 1.0 (0.7-3.9) 8

The Laboratory of Radiochemistry of the University of Helsinki (HYRL)

carried out sorption studies for samples of the new soil pits OL-KK14-OL, OL-

KK15 KK16 in 2008 (Lusa et al. 2009). Supplementary samples were taken for

the separation of soil solution. The distribution coefficient, Kd, in addition of

the main elements and the main nuclides will be determined from these in situ

samples. In addition six profiles were taken for the 137

Cs determination. Also

mineralogical composition of the soil pits OL-KK14…OL-KK16 is reported in

Lusa et al. (2009).

Mainly for the bedrock charcterisation needs, the investigation trenches (OL-

TK1…OL-TK16) (Figure 1) have been mapped, but also the soil types and

groundwater level and essential overburden thickness have been studied in

9

some trenches (Huhta 2005, 2008, 2009, Lindberg & Paulamäki 2004,

Nordbäck 2007). Soil stratigraphy and soil types are investigated from the

trenches of OL-TK8, OL-TK9, OL-TK13, OL-TK14, OL-TK15 and OL-TK16.

Observations of disintegrated rock layers of rock debris between solid bedrock

and overburden were found along the investigation trenches e.g. OL-TK8, OL-

TK9 and OL-TK14. The depth of layers varied from some ten centimetres to 2-

3 meters. The layers were slightly chemically changed (so called

palarapakallio). The surface of broken bedrock was strongly weathered and

reddish brown in colour (Huhta 2005, 2008).

The comprehensive data set on estimated overburden thickness and interpreted

overburden type is collected with refraction seismic survey campaigns with

survey lines covering the whole Olkiluoto Island, and more detailed on a

central part of the island (Lehtimäki 2001, 2003).

A soil survey of 94 surface soil and vegetation plot sampling (Figure 1) was

carried out in 2005 (Tamminen et al. 2007). These plots were inventoried for

their humus, mineral soil (0–60 cm) and peat (0–30 cm) layers. According to

the survey, the most common soil types at Olkiluoto are weakly developed

(often at the beginning of podzolisation) coarse to medium coarse Arenosols or

fine-textured Regosols, shallow Leptosols and Gleysols characterised by

groundwater close to surface. Organic layer was classified in most cases as mor

or mull-like peat. In places, there was quite considerable amount of stones,

boulders, thin-covered soil with exposed bedrock.

On the basis of silvicultural inventory in 2003, the most common soil types at

the Olkiluoto Island area are fine-textured (53 %) and sandy (39 %) till. The

other types are gravelly till (4 %) and peat (3.4 %), in addition to one percent of

outcrops (Rautio et al. 2004).

In the summer 2008, a light surface field survey study (< 1 m depth) has been

carried out along five lines to verify the continuity/discontinuity between the

overburden and marine sediments at Olkiluoto (Figure 1). Each line was about

600 m in length with the soil survey being carried out every 25 m. Land

investigation included also the mapping of vegetation at the same sites.

According to the study, the soil types varied a lot; from stony shores to gyttja-

covered shores. Till was the main soil type, but in many places it was very

stony or thin. Rock outcrops were common. The results including a reed survey

at Olkiluoto inshore will be presented in Haapanen & Lahdenperä (2009).

Some Litorina and Ancylus clay areas exist in addition to the areas with mud

cover, mainly at the northern and southern side of the island (Rantataro 2001,

2002, Rantataro & Kaskela 2009). Mud/gyttja is stratified into the water and is

a mixture of decomposed plants, animals and fine-grained mineral soils. More

information on sea bed sediment distribution in the vicinity of the Olkiluoto

Island and the related sea area will be reported in (Rantataro & Kaskela 2009).

At Olkiluoto, the relative area of mires is less than the average for southwestern

Finland. The Olkiluodonjärvi mire is a typical young peatland, which is

10

initiated on an uplifted shore (current elevation is 1.5 m a.s.l, on average).

Primary mire formation was controlled by the shore displacement of the Baltic

Sea only some hundreds of years ago; the isolation occurred around 1491–1638

A.D. (Eronen et al. 1995, Vuorela et al. 2009). Geochemistry of four peat cores

has been investigated extending down to the upper part of till layer at the

Olkiluodonjärvi mire (Ikonen 2002, Lahdenperä et al. 2005). Ground-

penetrating radar probing was carried out on the Olkiluodonjärvi wetland area

in 2001 (Leino 2001). The aim was to map a thickness of peat layers and

overburden and to produce information on the degree of fracturing of the

bedrock’s surface part, if possible. However, the till was so conductive that

ground penetrating probing was not able to reach the bedrock surface.

In 2009, a project was launched to collect all available data on overburden

characteristics, especially thickness into a 3D model, and to be further interpreted

into a continuous stratigraphical volume model. The first version is planned to be

completed during the year 2009. In addition, this work will show the gaps in the

overburden data and advise the future overburden studies.

11

2 MATERIALS AND METHODS

2.1 Soil sampling and soil profile description

Altogether six soil pits were sampled in summer 2008: OL-KK14, OL-KK15, OL-

KK16, OL-KK17, OL-KK18 and OL-KK19, the three latter were located close to each

other in the infiltration experiment site (Pitkänen et al. 2008b). All the pits were dug by

excavator. The locations of the sampling sites are presented in Figure 1 and the site

descriptions are presented in Appendix 1. The coordinates of the soil pits are presented

in Table 2.

Table 2. Soil pit coordinates (in the KKJ system) sampled in 2008.

Soil pits Coordinates

Northing Easting

OL-KK14 6791912 1525631

OL-KK15 6793023 1526564

OL-KK16 6792149 1528049

OL-KK17 6792349 1525854

OL-KK18 6792383 1525796

OL-KK19 6792396 1525804

Samples were taken from vertical profiles of soil pits from humus and from two to five

different mineral horizons extending from soil surface down to bedrock, if possible.

Altogether 25 samples were analysed.

The bedrock was at the depth of 290-320 cm in OL-KK14…OL-KK16. The soil pits

(OL-KK17…OL-KK19) in the infiltration site were not dug down to bedrock. The

topography of the infiltration experiment site is very flat and only varies a few metres.

However, the topography of the bedrock surface seems to show a depression in NE-

SW direction (Pitkänen et al. 2008b). Earlier overburden surveys of the study site were

carried out in the autumn 2002 (Lintinen et al. 2003) and according to it, the

overburden thickness of the soil pits, OL-KK6 and OL-KK7, close to OL-KK17…OL-

KK19, varied from 2.0 m to 4.0 m.

The soil pit OL-KK14

The OL-KK14 situated near the Liiklansuo mire and the Olkiluoto main road. Also the

shallow groundwater drillhole (OL-PP39) (Pitkänen et al. 2008a) locates to the

northeastern side, close to pit. In the Figure 3 the soil profile of the OL-KK14 is

presented.

12

Figure 3. The soil profile of OL-KK14 (graphics Teea Penttinen/Pöyry Environment

Oy).

The soil was sandy till until 105 cm, and its bottom layer was very stony. Under these

layers was 135 cm thick homogenous, bluish clay layer. At the bottom 5-10 cm thick

weathered bedrock was found. The bedrock was pegmatitic granite. The groundwater

table was at around the depth of 240 cm and the yield of groundwater from the surface

of the bedrock was approximately 30 L/min. The gravitation plate lysimeters were

installed at the depths of 0-5 cm, 40 cm and 100 cm. The main tree species at the site

are pine, spruce and some birches and junipers. In the Figures 4 and 5 the soil profiles

of OL-KK14 are shown.

13

Figure 4. Soil profile of the excavator pit OL-KK14. Bluish homogenous clay layer is

seen at the bottom of the pit (photo by Anne-Maj Lahdenperä/Pöyry Environment Oy).

Figure 5. Excavator pit OL-KK14. The groundwater table was at the depth of 240 cm

(photo by Anne-Maj Lahdenperä/Pöyry Environment Oy).

14


The OL-KK15 situated in northern part of the island, in the end of the harbor road,

close to a birch-dominated soil and vegetation sampling plot and the light field survey

line 2 (Figure 1). In the Figure 6 the soil profile of the OL-KK15 is presented.


Oy).

The surface layer under the humus was sand (7-50 cm). At the bottom of this layer

there were some marks of carboniferous layers. Under that was a 30 cm thick fine-

grained silty-clayish till layer. After that soil type changed to somewhat stratified fine

sand with some stones, under which a brownish and quite loose clay layer (30 cm

thick) with some sand lenses in the surface was found. At the bottom there was coarse-

grained sandy till until a depth of 300 cm. Bedrock was veined gneiss. In Figure 7 soil

profile of the excavator pit OL-KK15 is shown. Groundwater table was in the contact

of the overburden and bedrock. The main tree species in the site are young birches, but

there is also on old dense spruce forest close by.

15

Figure 7. Soil profile of the excavator pit OL-KK15 (photo by Anne-Maj Lahdenperä/

Pöyry Environment Oy).


The OL-KK16 is situated in the eastern part of the island, next to the Rumminperä

road. The site locates very close to spruce-dominated soil and vegetation sampling plot

and the light field survey line 3 (Haapanen & Lahdenperä 2009) (Figure 1). The

mineral soil surface layers until 110 cm were coarse sand, sand and fine to coarse sand.

At the bottom there was a 190 cm thick layer of sandy till with some big boulders and

stones. Also some rounded Satakunta sandstones were found. The bottom soil was

loose and moist indicating closeness of groundwater table. The bedrock (at 300 cm)

was veined gneiss/stromatic gneiss. The main tree species at the site is spruce with

some birches. In the Figures 8 and 9 the soil profile is presented.

16


Oy).

Figure 9. Soil profile of the excavator pit OL-KK16 (photo by Anne-Maj Lahdenperä/

Pöyry Environment Oy.)

17

Soil pits OL-KK17, OL-KK18 and OL-KK19 at the infiltration experiment site

The soil pits OL-KK17, OL-KK18 and OL-KK19 were dug close to each other at the

infiltration experiment area (Pitkänen et al. 2008b), and near to the Korvensuo

freshwater reservoir, ONKALO underground rock chracterisation facility and the old

investigation trench OL-TK4 (Figure 1).

In the OL-KK17 the humus layer was thick (30 cm). The mineral surface layers were

sandy till. The sampled bottom soil layer was at the depth of 110 cm. Bedrock was not

reached. The gravitation plate lysimeters were installed into the depths of 10 cm, 40

cm and 100 cm by the Finnish Forest Research Institute. The vegetation is mixed

forest, with pine, spruce and birches. In the Figures 10 and 11 the soil profile is shown.


Oy).

18

Figure 11. The thick (30 cm) humus horizon of the excavator pit OL-KK17 (photo by

Susanna Lindgren/Posiva Oy).

In the pit OL-KK18 the humus layer was thick (20 cm). The mineral soil down to 200

cm was clayey till with stones up to 0.5-1 m in diameter. At the depth of 200-220 cm

there was a grey and tight clay layer. The bedrock was not reached. The gravitation

plate lysimeter was installed at the depth of 200 cm. The vegetation at the site is mixed

forest. The soil profile of the excavator pit OL-KK18 is presented in Figures 12 and 13.

19


Oy).

Figure 13. The soil profile of the excavator pit OL-KK18 and installation of lysimeters

by the Finnish Forest Research Institute (photo by Susanna Lindgren/Posiva Oy).

20

The soil pit OL-KK19 is situated about 10 m north from OL-KK18. The humus layer

was about as thick (20 cm). The mineral soil down to 200 cm was clayey till with

stones up to 0.5-1 m in diameter also here. At the depth of 200-235 cm there was grey

and tight clay layer. The gravitation plate lysimeters were installed at the depth of 220

cm. The bedrock was not reached. The soil profile of the excavator pit OL-KK19 is

presented in Figures 14 and 15. The vegetation is mixed forest.


Oy).

21

Figure 15. The soil profile of the excavator pit OL-KK19 (top) and a part of the profile

with a big stone at the depth of 185-200 cm (bottom) (photo by Susanna

Lindgren/Posiva Oy).

22

2.2 Analysis of the samples

Chemical analysis

The main chemical analyses (Table 3) were done in the laboratory of Labtium Ltd.

Total organic carbon (TOC) analyses for the humus layers of OL-KK14, OL-KK15

and OL-KK16 were done in the Nablab laboratory. The samples were cold-dried at

<40oC and sieved to a <2 mm fraction (ISO/DIS 11464). The results of the

geochemical analyses are presented in Appendix 2, and the detection limits for

analysed elements in Appendix 3.

The pH was determined by using CaCl2 extraction. Using a dilute CaCl2 solution will

probably give more consistent results than using rainwater or diluted water. When the

soil is diluted with water, most of the H+ ions tend to remain attracted to the soil

particles and are not released into the soil solution. The addition of small amounts of

calcium chloride provides Ca2+

ions to replace some of the H+ ions on the soil particles,

forcing the hydrogen ions into the solution and making their concentration in the bulk

solution closer to that found in the field. The pH measured in CaCl2 is almost always

lower than pH of the same soil measured in water due to the higher concentration of

H+. The procedure gives a value similar to that for natural soil solution because the soil

solution also contains dissolved Ca2+

and other ions (e.g. Derome 2003).

Carbon contents were analysed by carbon analyser and nitrogen contents by carbon-

nitrogen analyser (Appendix 2). Total organic carbon (TOC) from the humus layers of

OL-KK14, OL-KK15 and OL-KK16 was analysed by TOC-analyser. The analyser

determines TOC by subtracting the measured inorganic carbon (IC) from the measured

total carbon value (TC)

The concentrations of the main elements (multi-element analysis) of the easily

leachable/bioavailble fraction of humus and mineral soil samples were measured with

partial dissolution, buffered by 1.0 M NH4Ac (NH4Ac-CH4COO; ratio of solution

1:10) digested at pH 4.5, and measured using ICP-MS/CP-OES. The cation exchange

capacity (CEC) was determined as a sum of concentrations of base cations

(Ca+Mg+Na+K), aluminium and iron. CEC is given in mmol/kg. The corresponding

buffer capacity was determined as a base saturation (BS %), i.e. the percentage of base

cations in the CEC.

The total concentrations of the humus and mineral soil layers were measured by

hydrofluoric acid-perchloric acid digestion (ratio of solution 5:1) using the ICP-

MS/ICP-OES-technique.

The analyses of Se and I were carried out by ALS Laboratory Group in Luleå, Sweden.

The samples were dried at 105 oC according to the Swedish standard SS028113.

Digestion was performed on non-dried samples in closed Teflon vessels in microwave

oven with HNO3 + H2O. Determination of iodine (I) was performed after digestion

using ICP-SFMS. Determination of selenium (Se) was performed after digestion,

reduction with HCl and hydride generation with ICP-SFMS.

23

Table 3. Analysed parameters, methods and used standards.

Parameter Unit Method Standard Number of

samples

pH CaCl2 extraction

ISO10390

SFS ISO 10390 25

Loss on ignition (LOI) mass-% Gravimetrically

at 550oC

CEN 15407 25

Moisture and dry

matter content

mass-% Gravimetrically

at 105oC

ISO 11465 25

Carbon mass-%dw Carbon analyser CEN 15104 25

Nitrogen mass-%dw Carbon-nitrogen

analyser

ISO 13878, CEN

15104

25

Total organic carbon mass-% TOC- analyser.

SFS-EN 13137 3

Iodine mg/kgdw ICP-SFMS 25

Selenium mg/kgdw ICP-SFMS 25

1) Multi-element

analysis with

ammonium acetate

(NH4 Ac) extraction,

pH 4.5)

mg/kgdw ICP-MS/ICP-

OES-technique

SFS-EN-

ISO17294-2 and

SFS-EN-ISO

11885

25

2) Multi-element

analysis with

hydrofluoric acid -

perchloric acid

extraction

mg/kgdw ICP-MS/ICP-

OES-technique

SFS-EN-ISO

17294-2 and SFS-

EN-ISO 11885

25

Grain size distribution % Dry-sieving and

sedigraph-

analysis

ISO 3310/1 19

Mineralogy X-ray diffraction

analyser

13

1) Analysed elements: Al, As, B, Ba, Ca, Cd, Co, Cr, Cu, Fe, K, Li, Mg, Mn, Mo, Na, Ni, P, Pb, S, Sb,

Sr, Ti, V, Zn

2) Analysed elements: Al, As, Ba, Be, Bi, Ca, Cd, Co, Cr, Cu, Fe, K, Li, Mg, Mn, Mo, Na, Ni, P, Pb,

Rb, S, Sb, Sr, Ti, V, Zn, Zr

Grain-size distribution and mineralogy

Grain-size analyses of >0.063 mm particles were carried out by dry sieving the

samples by mechanical sieve shaker (ISO3310/1). The sieve apertures used were 20

mm, 2 mm, 0.63 mm, 0.2 mm and 0.063 mm. Grain size analyses of <0.063-mm

particles was carried out by using Sedigraph 5100 instrument. Results of sieving and

sedigraph analyses were combined at 0.063 mm for grain-size distribution graphs. The

grain size distribution for the OL-KK14…OL-KK19 was done at the Geological

Survey of Finland and at the Labtium Ltd. laboratory.

The mineralogical composition was determined by X-ray diffraction analyser (Philips X´Pert MPD) in Labtium Ltd. laboratory. The results of soil samples OL-KK14…OL-KK16 are reported in Lusa et al. 2009. Mineralogical analyses of the soil pits OL-KK17…OL-KK19 were not available.

25

3 RESULTS

3.1 Geochemical and geotechnical analyses

3.1.1 Basic properties

As a result of weathering and buffering processes, the pH of the percolating water

gradually increases as it passes through deeper horizons. The greatest deviations in soil

pH are due to variation in humus and clay contents (e.g. Räisänen 1989, Kähkönen

1996). In addition, soil pH values are also affected by the organic and inorganic humic

and fulvic acids produced by biological activity (Nuotio et al. 1990, Räisänen 1989).

pH-values varied in the humus layers from 3.3 to 5.4. The pH was <4 in OL-KK14, OL-KK15, OL-KK18 and OL-KK19. In the humus layers of OL-KK16 pH was 4.8 and in OL-KK17 5.4. In the humus horizon pH variation was large (2.1 pH units). In the mineral soil layers pH ranged from 4.7 to 7.7, and increased as a function of depth (Figure 16 and Appendix 2.1).

Humus

MS1

MS2

MS3

MS4

MS5

3.0 3.5 4.0 4.5 5.0 5.5 6.0 6.5 7.0 7.5 8.0 8.5

pH

So

il L

ay

er

OL-KK14OL-KK15OL-KK16OL-KK17OL-KK18OL-KK19

Figure 16. pH of soil pits OL-KK14…OL-KK19 from different soil layers analysed by

CaCl2.

When comparing the pH values obtained within different methods; pH measured in

water and saline solution (CaCl2), the pH measured in water solution is typically 0.5-

1.0 units higher than pH measured in saline solution (Westman 1991). This is also seen

when comparing the same samples of OL-KK14…OL-KK16, where the pH in

Laboratory of Radiochemistry (HYRL) was analysed using water solution (Lusa et al.

2009) and in saline CaCl2 solution presented in this report (Table 4). pH of the humus

horizons of the studied soils was, in general, similar to humus horizons of the top soil

and vegetation plots digested both by water and CaCl2 solutions (Tamminen et al.

26

2007). The pH of studied mineral soil layers was not comparable because soil samples

were taken from different and deeper depths than top soil plot layers.

Table 4. pH-value comparison of the soil sample results analysed by CaCl2 reported

here and by H2O reported by Lusa et al. (2009).

Sample OL-KK14

OL-KK14

(Lusa et

al. 2009)

OL-KK15

OL-KK15

(Lusa et al.

2009)

OL-KK16

OL-KK16

(Lusa et

al. 2009)

Humus 3.6 4.4 3.9 4.2 4.8 5.0

MS1 5.2 5.2 4.7 5.9 5.4 6.5

MS2 5.7 6.5 6.4 6.5 6.3 7.1

MS3 5.8 6.7 7.0 7.7 7.3 7.7

MS4 7.6 8.1 7.5 8.0 7.5 8.6

MS5 - - 7.7 8.6 - -

- Not sampled

The dry matter content increased as a function of depth, varying in the humus horizons

from 49.8 mass-% to 69.1 mass-% and in the bottom soil layers from 88.8 mass-% to

99.6 mass-% (Figure 17). The organic matter and moisture contents decreased as a

function of depth. The organic matter, measured by loss on ignition (LOI), varied quite

a lot in the humus layers, from 15.8 mass-% (OL-KK19) to 58.5 mass-% (OL-KK16)

(Figure 18). Also the moisture content varied in the humus horizons, being lowest

(30.9 mass-%) in OL-KK19 and highest (50.2 mass-%) in OL-KK18 (Figure 19). In

the mineral soil layers LOI was mainly <1 mass-%. Total organic carbon (TOC)

concentrations of the humus horizons OL-KK14…OL-KK16 varied from 22 % to 32

%. The TOC analyses of OL-KK17…OL-KK19 were not available. The pH, dry and

organic matter, TOC, LOI and moisture content are presented in Appendix 2.1.

The carbon content in the humus layers ranged from 9.9 % (OL-KK19) to 31.9 % (OL-KK18). Although these sites situated close to each other there was a three fold difference in the carbon content. In the humus horizon of the OL-KK17, carbon content was 26.3 %. In the mineral soils layers C content was <1 % (Figure 20). The nitrogen content in the humus horizons ranged from 0.29 % (OL-KK19) to 2.02 % (OL-KK16). In the mineral soil layers nitrogen content was low or under the detection limits (Figure 21). C/N ratio in the humus horizon varied from 15.7 % (OL-KK16) to 34.1 % (OL-KK19) (Table 5). Generally the values correspond to the results reported in Tamminen et al. (2007).

27

Humus

MS1

MS2

MS3

MS4

MS5

40 45 50 55 60 65 70 75 80 85 90 95 100

Dry Matter Content %

So

il L

ayer

OL-KK14

OL-KK15

OL-KK16

OL-KK17

OL-KK18

OL-KK19

Figure 17. Dry matter content (mass-%) of soil pits OL-KK14…OL-KK19 from

different soil layers.

Humus

MS1

MS2

MS3

MS4

MS5

0 5 10 15 20 25 30 35 40 45 50 55 60

Organic Matter %

So

il L

ay

er


Figure 18. Organic matter content (mass-%dw) of soil pits OL-KK14…OL-KK19 from


28

MS5

MS4

MS3

MS2

MS1

Humus

0 5 10 15 20 25 30 35 40 45 50 55

Moisture %

So

il L

ay

er


Figure 19. Moisture content (mass-%) of soil OL-KK14…OL-KK19 from different soil

layers.

Humus

MS1

MS2

MS3

MS4

MS5

0 5 10 15 20 25 30 35

Carbon %

So

il L

ayer

OL-KK14

OL-KK15

OL-KK16

OL-KK17

OL-KK18

OL-KK19

Figure 20. Carbon content (%dw) of soil pits OL-KK14…OL-KK19 from different soil

layers.

29

Humus

MS1

MS2

MS3

MS4

MS5

0 0.2 0.4 0.6 0.8 1 1.2 1.4 1.6 1.8 2 2.2

Nitrogen %

So

il L

ay

er


Figure 21. Nitrogen content (-%dw) of soil pits OL-KK14…OL-KK19 from different

soil layers.

Table 5. Carbon, nitrogen and ratio of C and N in soil pits OL-KK14…OL-KK19 in

different depths.

Sample Sample

layer

Sampling

depth (cm)

Carbon

mass- %dw

Nitrogen

mass-%dw C/N

OL-KK14

Humus 0-5 30.5 1.42 21.5

MS1 5-20 0.20 <0.03 -

MS2 20-60 0.27 0.04 6.75

MS3 60-105 0.13 <0.03 -

MS4 105-240 0.18 <0.03 -

OL-KK15

Humus 0-7 21.9 1.18 18.6

MS1 7-50 0.22 0.04 5.50

MS2 50-80 0.33 0.04 8.25

MS3 80-110 0.18 <0.03 -

MS4 110-160 0.23 0.03 7.67

MS5 160-300 0.14 <0.03 -

OL-KK16

Humus 0-10 31.8 2.02 15.7

MS1 10-30 0.64 0.07 9.14

MS2 30-50 0.14 <0.03 -

MS3 50-110 0.13 <0.03 -

MS4 110-300 0.13 <0.03 -

OL-KK17

Humus 0-30 26.3 0.98 26.8

MS1 30-46 0.41 0.05 8.20

MS2 46-82 0.12 <0.03 -

OL-KK18

Humus 0-20 31.9 1.17 27.3

MS1 20-200 0.07 <0.03 -

MS2 200-220 0.18 <0.03 -

OL-KK19

Humus 0-20 9.89 0.29 34.1

MS1 20-200 0.11 <0.03 -

MS2 200-235 0.14 <0.03 -

- Not determined; nitrogen concentration under the detection limit

30

3.1.2 Main exchangeable nutrients

The ammonium acetate digested main nutrient concentrations are presented in Table 6.

Easily leachable and bioavailable main nutrient (Ca, Mg, K, P and S) contents were

distinctly higher in the humus horizon than in the mineral soil layers. Calcium was the

dominating nutrient, varying from 616 mg/kg (OL-KK19) to 13800 mg/kg (OL-KK17)

in the humus horizon. Calcium concentration in the humus horizons of OL-KK16 and

OL-KK17 were 4-5 times higher than in other humus horizons. In the mineral soil,

calcium concentrations increased according to soil depth (Figure 22). Calcium minerals

weather easily and are essential nutrients (Koljonen 1992).

Table 6. Easily leachable (NH4 Ac-digestion, pH 4.5) of main nutrients in soil pits of

OL-KK14…OL-KK19 in different soil layers.

Soil sample Soil layer

Sampling

depth

(cm)

Ca

(mg/kg)

K

(mg/kg)

Mg

(mg/kg)

P

(mg/kg)

S

(mg/kg)

OL-KK14

Humus 0-5 1560 341 285 36.5 91.9

MS1 5-20 391 38.5 98.3 4.80 4.93

MS2 20-60 620 51.0 110 16.7 5.21

MS3 60-105 365 39.4 60.5 21.3 17.5

MS4 105-240 1370 56.1 81.8 14.8 58.5

OL-KK15

Humus 0-7 3580 195 347 23.9 91.1

MS1 7-50 124 16.2 32.6 6.61 7.89

MS2 50-80 676 135 204 8.81 36.4

MS3 80-110 1090 61.0 110 10.0 19.6

MS4 110-160 1860 143 198 18.8 68.2

MS5 160-300 1340 59.7 104 16.1 35.1

OL-KK16

Humus 0-10 10700 237 1120 18.2 83.1

MS1 10-30 650 26.2 62.5 4.71 14.2

MS2 30-50 364 31.9 47.5 12.3 12.5

MS3 50-110 1350 30.3 69.9 12.4 26.9

MS4 110-300 1560 37.8 77.8 13.4 32.0

OL-KK17 Humus 0-30 13800 253 866 16.5 56.0

MS1 30-46 682 17.2 29.7 9.26 11.1

MS2 46-82 518 28.5 31.6 19.8 7.87

OL-KK18 Humus 0-20 2880 583 472 73.0 68.2

MS1 20-200 403 26.5 23.6 28.5 3.31

MS2 200-220 2060 48.0 90.9 12.3 36.9

OL-KK19 Humus 0-20 616 81.2 146 25.7 17.5

MS1 20-200 1510 27.6 26.2 11.2 <2

MS2 200-235 1610 36.7 53.4 10.7 31.9

31

Humus

MS1

MS2

MS3

MS4

MS5

0 2000 4000 6000 8000 10000 12000 14000 16000

Ca (mg/kg)

So

il L

ay

er


Figure 22. Easily leachable calcium concentrations of OL-KK14…OL-KK19 in


Magnesium concentrations varied from 146 mg/kg (OL-KK19) to 1120 mg/kg (OL-

KK16) in the humus horizons and in the mineral soil layers from 23.6 mg/kg to 204

mg/kg (Figure 23). The Mg concentration was highest in the humus horizons of OL-

KK16 and OL-KK17, following the pattern of calcium. Magnesium minerals weather

quite easily, with dissolved magnesium being removed from solution, mostly into clay

minerals. Potassium concentrations varied from 81.2 mg/kg (OL-KK19) to 583 mg/kg

(OL-KK18) in the humus horizons, although these soil pits situated close to each other

in the infiltration experiment site. In the mineral soil potassium concentrations varied

from 16.2 mg/kg (OL-KK15) to 143 mg/kg (OL-KK15) (Figure 24). Dissolved

potassium is adsorbed from solutions onto colloids and is enriched in clays.

32

Humus

MS1

MS2

MS3

MS4

MS5

0 100 200 300 400 500 600 700 800 900 1000 1100 1200

Mg (mg/kg)

So

il L

ay

er


Figure 23. Easily leachable magnesium concentrations of OL-KK14…OL-KK19 in


Humus

MS1

MS2

MS3

MS4

MS5

0 50 100 150 200 250 300 350 400 450 500 550 600 650

K (mg/kg)

So

il L

ay

er


Figure 24. Easily leachable potassium concentrations of OL-KK14…OL-KK19 in


33

Sulphur is a non-metalic element, which in nature occurs in oxidation states -2 (+3), +4

(+5) and +6, and thus it is distributed in a highly heterogeneous manner (Koljonen

1992). Sulphur is also an essential non-toxic nutrient, in some extent. Sulphur

concentrations are highest at the Finnish coast, where sulphide and sulphur bearing

clays are common (Erviö 1975, Ojala et al. 2007, Palko 1994).

Sulphur concentrations were enriched in the humus horizons. Concentration varied

from 17.5 mg/kg (OL-KK19) to 91.9 - 91.1 mg/kg (OL-KK15 and OL-KK14) in the

humus horizons and in the mineral soil layers from <2 mg/kg to 68.2 mg/kg (Figure

25). In OL-KK16…OL-KK19 sulphur concentrations increased according to the depth.

In OL-KK14 and OL-KK-15 sulphur was enriched in the mineral soil layers MS4,

where the heavy metal concentrations of arsenic, cobalt, copper and lead

concentrations were high. Sulphur occurs mainly as sulphides (FeS2, FeS, CuFeS2,

PbS, FeAsS). The most of the sulphides are the main sources for the sulphur in the

overburden.

Phosphorus occurs in several minerals as diluted calcium, aluminum and iron

phosphates and organic compounds. Natural phosphorus in soils only appears in small

amounts and in a diluted state they are washed away gradually from the soil (Kabata-

Pendias & Pendias 1992). Phosphorus concentrations varied from 16.5 mg/kg (OL-

KK17) to 73 mg/kg (OL-KK18) in the humus horizons, and in the mineral soil layers

from 4.7 mg/kg to 28.5 mg/kg (Figure 26). In the mineral soil layers of OL-

KK14…OL-KK16 phosphorus concentrations increased according to the depth.

Humus

MS1

MS2

MS3

MS4

MS5

0 10 20 30 40 50 60 70 80 90 100

S (mg/kg)

So

il L

ay

er


Figure 25. Easily leachable sulphur concentrations of OL-KK14…OL-KK19 in


34

Humus

MS1

MS2

MS3

MS4

MS5

0 10 20 30 40 50 60 70 80

P (mg/kg)

So

il L

ay

er


Figure 26. Easily leachable phosphorus concentrations of OL-KK14…OL-KK19 in


3.1.3 Easily leachable trace elements

The concentrations of easily leachable main trace elements are presented in Table 7. Copper (Cu) is an essential trace-element and nutrient, but toxic in excess. Copper concentrations varied from 0.37 mg/kg (OL-KK18) to 1.57 mg/kg (OL-KK15) in the humus horizons. In the mineral soil layers the variation was from 0.37 mg/kg to 2.72 mg/kg, being highest in the deepest soils layers, in general.

Molybdenum (Mo) is an essential nutrient, moderately toxic, which participates in

redox reactions. Molybdenite (MoS2) is highly resistant to weathering and is poorly

soluble in acid environment. In dissolved form it rapidly removes from solutions and is

adsorbed into clays, and especially into sediments rich in organic matter (Kabata-

Pendias & Pendias 1992). Molybdenum concentrations were in most cases under the

detection limit (<0.03 mg/kg).

The geochemistry of iron (Fe) is complex in the terrestrial system. The reactions of Fe

in processes of weathering are dependent largely on the Eh-pH system of the

environment and on the stage of oxidation of the Fe compounds involved. In oxidizing

and alkaline conditions the mobilization and fixation of Fe promote the precipitation of

Fe, whereas acid and reducing conditions promote the solution of Fe compounds. Both

mineral and organic compounds of Fe are easily transformed in soils, and organic

matter appears to have significant influence on the formation of Fe oxides. Like Mn

compounds in soils, Fe compounds are greatly involved in the behavior of some

macronutrients and many of trace elements. The degree to which Fe is responsible for

trace metal solubility and availability is strongly governed by several soil factors

35

(Kabata-Pendias & Pendias 1992). The Fe content of soils is both inherited from parent

rock material and the result of soil formation processes. Both Fe uptake and transport

between plant organs are highly affected by several environmental factors, of which

soil pH, concentration of Ca and P, and ratios of several heavy metals are most

pronounced (Kabata-Pendias & Pendias 1992). Easily leachable iron concentrations

were the highest in the humus horizons and varied from 345 mg/kg (OL-KK19) to

2230 mg/kg (OL-KK15), except in the OL-KK17 and OL-KK18, where the Fe

concentration was enriched in subsoil layers. In the mineral soil layers Fe

concentration varied from 9.4 mg/kg to 249 mg/kg. The generally highest iron

concentrations were in OL-KK14 and OL-KK15 (Figure 27).

Table 7. Easily leachable/plant available (NH4 Ac-digestion, pH 4.5) of main trace

elements in soil pits of OL-KK14…OL-KK19 in different soil depths.

Soil

sample

Soil

layer

Sampling

depth

(cm)

Cu

(mg/kg)

Mo

(mg/kg)

Fe

(mg/kg)

Mn

(mg/kg)

Na

(mg/kg)

Zn

(mg/kg)

OL-

KK14

Humus 0-5 1.04 <0.03 1030 27.4 49.0 22.6

MS1 5-20 0.64 <0.03 106 1.83 8.76 0.31

MS2 20-60 0.91 <0.03 80.0 2.12 9.25 0.30

MS3 60-105 1.18 <0.03 83.4 3.61 4.43 0.45

MS4 105-240 2.07 0.03 147 44.3 4.16 0.96

OL-

KK15

Humus 0-7 1.57 0.04 2230 7.47 32.0 2.81

MS1 7-50 0.60 0.06 90.4 2.87 3.07 0.36

MS2 50-80 2.72 <0.03 189 14.0 24.9 1.07

MS3 80-110 0.94 <0.03 128 16.9 12.3 0.53

MS4 110-160 2.33 0.07 224 62.4 19.1 1.16

MS5 160-300 1.40 0.05 85.7 29.2 9.79 0.81

OL-

KK16

Humus 0-10 1.02 <0.03 427 7.89 84.6 9.73

MS1 10-30 0.64 0.03 249 0.46 6.27 0.16

MS2 30-50 1.36 <0.03 112 2.02 3.88 0.87

MS3 50-110 1.11 <0.03 62.3 22.0 4.34 0.60

MS4 110-300 2.36 0.05 91.5 33.5 5.35 0.66

OL-

KK17

Humus 0-30 0.51 <0.03 19.7 61.6 46.6 12.2

MS1 30-46 0.37 <0.03 9.36 1.70 <3 0.13

MS2 46-82 1.16 <0.03 52.7 2.56 6.01 0.21

OL-

KK18

Humus 0-20 0.37 <0.03 18.7 153 19.1 43.0

MS1 20-200 0.53 <0.03 40.2 2.99 3.44 0.38

MS2 200-220 2.02 0.03 123 43.3 4.33 0.76

OL-

KK19

Humus 0-20 0.53 <0.03 345 7.51 10.8 8.00

MS1 20-200 0.71 <0.03 44.7 14.5 <3 0.79

MS2 200-235 1.69 0.03 52.8 23.8 <3 0.38

36

Humus

MS1

MS2

MS3

MS4

MS5

0 500 1000 1500 2000 2500

Fe (mg/kg)

S

oil L

ayer


Figure 27. Easily leachable iron concentrations of OL-KK14…OL-KK19 in different

soil layers.

Manganese (Mn) is one of the most abundant trace elements. The highest

concentrations are associated with mafic rocks. The behavior of Mn in surfical deposits

is complex and is governed by different environmental factors, of which Eh-pH

conditions are the most important. All Mn compounds are important soil constituents

because this element is essential in plant nutrition and controls the behavior of several

other micronutrients. Mn-rich precipitates occur as crusts and layers in soils.

Manganese is a non-toxic nutrient, which participates in redox reactions in organisms

(Kabata-Pendias & Pendias 1992). Manganese concentrations are low (< 500 mg/kg) in

areas of eastern and southern Finland were granites and gneisses are predominant

(Koljonen 1992). At Olkiluoto the manganese concentrations were low. In the humus

horizons Mn concentrations varied from 7.47 mg/kg (OL-KK15) to 153 mg/kg (OL-

KK18) and in the mineral soil layers from 0.46 mg/kg to (OL-KK16) 62.4 mg/kg (OL-

KK15). Generally, manganese concentrations increased with the function of depth.

Owing to high reactivity, sodium (Na) is found in nature only as a compound and not

as a free element. With aluminum, sodium forms silicates and in bedrock it is mostly

incorporated in feldspars. Dissolved sodium remains in solution in ion form and is

removed to the seas, where it adds to the salinity. The distribution of sodium is similar

to that of calcium, showing that these elements occur together, in plagioclases

(Koljonen 1992). Na concentrations were highest in the humus horizons, varying from

10.8 mg/kg (OL-KK19) to 84.6 mg/kg (OL-KK16). The OL-KK16 located closest to

the sea in the northern part of the island. In the mineral soil layers Na concentrations

varied from <3 mg/kg to 24.9 mg/kg.

37

The solubilisation of zinc (Zn) minerals during weathering produces mobiles Zn2+

,

especially in acid, oxidizing environments. Zn is, however, also adsorbed by organic

components and thus, its accumulation in the surface horizons is observed. Soil organic

matter is known to be capable of bonding Zn into stabile forms, therefore,

accumulation of Zn in organic soil horizon and peat is usually observed. Zn is

considered to be readily soluble relative to the other heavy metals in soils. Soluble

forms of Zn are readily available to plants. The composition of the nutrient solution,

particularly the presence of Ca is a great importance (Kabata-Pendias & Pendias 1992,

Koljonen 1992). The Zn concentration was clearly higher in the humus horizons than

in mineral soil layers, and varied from 2.81 mg/kg (OL-KK15) to 43 mg/kg (OL-

KK18). In the mineral soil layers variation was from 0.13 mg/kg to 1.16 mg/kg (Figure

28).

MS5

MS4

MS3

MS2

MS1

Humus

0 10 20 30 40 50

Zn (mg/kg)

S

oil

La

ye

r


Figure 28. Easily leachable zinc concentrations of OL-KK14…OL-KK19 in different

soil layers.

3.1.4 Main trace elements in total digestion

The main trace metal concentrations analysed after total dissolution in strong mineral

acids (hydrofluoric acid – perchloric acid digestion) are presented in Table 8. The

method digests into solution most of the elements incorporated in silicates, oxides,

carbonates, sulphates and phosphates. The copper (Cu) was enriched in humus, ranging

from 16.0 mg/kg (OL-KK19) to 71.3 mg/kg (OL-KK17). In the mineral soil layers the

Cu concentrations varied from 7.5 mg/kg to 29.8 mg/kg. Molybdenum (Mo)

concentrations were low; the highest (4.15 mg/kg) was in the humus horizon of OL-

KK15. In most cases Mo concentrations were under the detection limit.

38

The iron (Fe) concentration varied from 5970 mg/kg (OL-KK18) to 31800 mg/kg (OL-

KK14). The highest concentrations were found in the mineral soil layers of MS1 and

MS2 in all soil pits. In the soil profiles manganese (Mn) concentrations varied from 89

mg/kg to 604 mg/kg and Mn concentration pattern followed that of iron. Sodium (Na)

concentration varied from 3840 mg/kg to 15800 mg/kg, being lowest in the humus

horizons. Zinc (Zn) concentrations varied from 25.6 mg/kg to 112 mg/kg in soil layers.

In OL-KK14…OL-KK16 and OL-KK19 Zn concentrations followed the pattern of Fe

and Mn.

Table 8. Total concentrations (hydrofluoric acid-perchloric acid digestion) of main

trace elements in soil pits OL-KK14…OL-KK19 in different soil layers.

Soil

sample

Soil

layer

Sampling

depth

(cm)

Cu

(mg/kg)

Mo

(mg/kg)

Fe

(mg/kg)

Mn

(mg/kg)

Na

(mg/kg)

Zn

(mg/kg)

OL-KK14

Humus 0-5 65.0 1.2 10900 103 4730 60.9

MS1 5-20 19.2 0.72 24900 510 13900 58.7

MS2 20-60 27.4 0.95 31800 604 14700 73.9

MS3 60-105 16.7 <0.5 20000 343 12500 53.8

MS4 105-240 13.8 <0.5 18500 334 13400 48.4

OL-KK15

Humus 0-7 34.2 4.2 22300 164 6730 25.6

MS1 7-50 29.8 <0.5 11300 183 15000 32.5

MS2 50-80 25.9 1.5 30200 518 15800 82.6

MS3 80-110 19.2 0.58 20400 391 13200 56.2

MS4 110-160 17.8 0.55 22000 405 12900 55.4

MS5 160-300 14.9 <0.5 15300 271 12700 48.3

OL-KK16

Humus 0-10 52.2 2.4 16900 89.1 3840 34.4

MS1 10-30 9.02 1.4 17600 209 12400 72.8

MS2 30-50 15.3 <0.5 17500 243 12900 53.6

MS3 50-110 9.99 <0.5 13800 256 12900 39.8

MS4 110-300 11.6 <0.5 14000 268 13600 45.2

OL-KK17

Humus 0-30 71.3 0.99 12600 228 4730 79.3

MS1 30-46 7.49 <0.5 14400 191 11600 40.9

MS2 46-82 17.4 <0.5 17800 293 12700 46.7

OL-KK18

Humus 0-20 25.9 0.96 5970 421 4460 112

MS1 20-200 16.1 <0.5 17600 311 12400 50.4

MS2 200-220 11.6 <0.5 16000 315 13400 44.9

OL-KK19

Humus 0-20 16.0 0.52 12300 126 9490 43.5

MS1 20-200 15.8 1.1 16000 266 12500 47.5

MS2 200-235 11.4 <0.5 15600 275 12600 44.3

3.1.5 Easily leachable metal concentrations in partial digestion

In addition to the total digestion, metals were analysed by a partial digestion with

ammonium acetate digestion, (pH 4.5) as summarized in Table 9 and discussed below.

In general, the solubility of aluminum (Al) hydroxides is low, especially at the pH

range from 5 to 9. The total Al content of soils is inherited from parent rocks; however,

only that fraction of Al which is easily mobile and exchangeable plays an important

role in soil fertility. In acid soils with pH below 5.5, the mobility of Al increases

39

sharply and very actively competes with other cations for exchangeable sites. The

mobile Al toxicity is also frequently associated with increased levels of Fe and Mn,

and possibly other heavy metals, which are readily available in acid soils. The Ca and

Mg in soil greatly reduce Al toxicity. Al toxicity is one of the major growth limiting

factors in many acid soils (Kabata-Pendias & Pendias 1992, Koljonen 1992). Easily

leachable aluminum concentrations were highest in the humus horizons: Al varied

from 55.5 mg/kg (OL-KK18) to 740 mg/kg (OL-KK14) and in the mineral soil layers

from 11.9 mg/kg to 88.6 mg/kg. The highest concentrations were in OL-KK14 and

OL-KK15 (Figure 29).

MS5

MS4

MS3

MS2

MS1

Humus

0 200 400 600 800

Al (mg/kg)

S

oil

La

ye

r


Figure 29. Easily leachable aluminum concentrations of OL-KK14…OL-KK19 in


Although arsenic (As) minerals and compounds are readily soluble, As migration is

greatly limited due to the strong sorption by clays, hydroxides and organic matter. The

lowest As levels are found in sandy soils, in particular, in those derived from granites,

whereas higher As concentrations are related to most often to soils with rich in organic

matter. Acid sulphate clay soils are also reported to accumulate a high proportion of

As. Arsenic is a constituent of most plants, but little is known about its biochemical

role (Kabata-Pendias & Pendias 1992, Koljonen 1992). Arsenic concentrations were

low, being highest in the humus horizons (0.09-0.44 mg/kg). The highest arsenic

concentration in humus horizon was in OL-KK15.

During weathering, cadmium (Cd) goes readily into solution and, though it is known to

occur as Cd2+

, it may also form several complex ions. The most important factors

which control the Cd mobility are pH and oxidation potential. Soil microbial activity

plays a significant role in the Cd behavior in soils. Cd is most mobile in acidic soils

within the range of pH 4.5 to 5.5, whereas in alkaline soil Cd is rather immobile

40

(Kabata-Pendias & Pendias 1992, Koljonen 1992). Cadmium concentrations varied

from 0.16 mg/kg (OL-KK19) to 0.73 mg/kg (OL-KK17) in the humus horizons, in the

mineral soil layers concentrations were under the detection limit.

Soil organic matter and clay content in addition of manganese oxides and pH are most

important factors that govern the cobalt (Co) distribution and behavior. The mobility of

Co is strongly related to organic matter in soils. The cobalt concentrations were low;

the highest values were in the humus horizon (0.36-1.42 mg/kg). The highest cobalt

concentration in the humus horizon was in OL-KK14.

In surface soil horizon nickel (Ni) appears to occur mainly in organically bound forms.

Ni distribution in soil profiles is related to organic matter and clay fractions, depending

on soil type. The Ni status in soil is highly dependent on the Ni content of parent rocks.

However, the concentration of Ni in surface soils also reflects soil-forming processes

and pollution (Koljonen 1992). In the humus horizons nickel concentrations varied

from 0.97 mg/kg (OL-KK17) to 2.27 mg/kg (OL-KK14), in the mineral soil layers

concentrations were in most cases under the detection limit.

The natural lead (Pb) content of soil is inherited from parent rocks and Pb is the least

mobile among the other heavy metals. However, due to Pb pollution and radon

emanation (Pb is the last daughter in the decay chain); most soils are enriched by Pb,

especially in the topsoil. However, the characteristic localisation of Pb near the soil

surface in most soil profiles is primarily related to the surficial accumulation of organic

matter (Kabata-Pendias & Pendias 1992, Koljonen 1992). Lead concentrations were

clearly higher in the humus horizons, varying from 3.2 mg/kg (OL-KK17) to 17.5

mg/kg (OL-KK18). In the mineral soil layers lead concentrations were lower (Figure

30).

Figure 30. Easily leachable lead concentrations of OL-KK14…OL-KK19 in different

soil layers.

Humus

MS1

MS2

MS3

MS4

MS5

0 5 10 15 20

Pb (mg/kg)

S

oil

La

ye

r


41

Vanadium-bearing mafic minerals weather easily and the dissolved element is removed

from solution mainly into sediments rich in organic matter. Vanadium (V) is a micro-

nutrient, but some of its compounds are known to be toxic. Vanadium concentrations

were low. The highest concentration was in OL-KK15 in the humus horizon.

Table 9. Easily leachable, harmful metals concentrations in partial digestion (NH4 Ac-

digestion, pH 4.5) in soil pits OL-KK14…OL-KK19 in different sampling soil layers.

Soil

sample

Soil

layer

Sampling

depth

(cm)

Al

(mg/kg)

As

(mg/kg)

Cd

(mg/kg)

Co

(mg/kg)

Ni

(mg/kg)

Pb

(mg/kg)

V

(mg/kg)

OL-

KK14

Humus 0-5 740 0.26 0.38 1.42 2.27 16.5 0.26

MS1 5-20 46.3 0.05 <0.1 <0.1 <0.5 0.44 <0.1

MS2 20-60 40.0 0.06 <0.1 <0.1 <0.5 0.36 <0.1

MS3 60-105 21.4 0.09 <0.1 <0.1 <0.5 4.87 <0.1

MS4 105-240 34.3 0.15 <0.1 0.46 0.71 0.86 0.31

OL-

KK15

Humus 0-7 369 0.44 0.24 0.85 2.02 5.49 0.74

MS1 7-50 69.1 0.06 <0.1 0.37 <0.5 0.20 0.11

MS2 50-80 88.6 0.15 <0.1 0.16 0.67 1.02 <0.1

MS3 80-110 42.4 0.10 <0.1 0.12 <0.5 0.59 <0.1

MS4 110-160 59.0 0.43 <0.1 0.71 1.27 1.97 0.66

MS5 160-300 18.5 0.12 <0.1 0.28 0.51 4.82 0.23

OL-

KK16

Humus 0-10 241 0.27 0.41 0.48 1.54 7.25 0.37

MS1 10-30 52.8 0.08 <0.1 <0.1 <0.5 0.37 0.21

MS2 30-50 35.4 0.08 <0.1 0.14 <0.5 0.39 <0.1

MS3 50-110 11.9 0.09 <0.1 0.14 <0.5 0.50 <0.1

MS4 110-300 15.3 0.09 <0.1 0.23 <0.5 0.54 0.21

OL-

KK17

Humus 0-30 108 0.09 0.73 1.07 0.97 3.20 0.10

MS1 30-46 32.2 <0.03 <0.1 <0.1 <0.5 <0.1 <0.1

MS2 46-82 20.3 0.09 <0.1 <0.1 <0.5 0.25 <0.1

OL-

KK18

Humus 0-20 55.5 0.09 0.50 0.36 1.01 17.5 0.19

MS1 20-200 19.4 0.06 <0.1 <0.1 <0.5 0.32 <0.1

MS2 200-220 31.9 0.13 <0.1 0.44 0.59 0.78 0.38

OL-

KK19

Humus 0-20 250 0.12 0.16 0.39 1.17 5.68 0.23

MS1 20-200 20.0 0.05 <0.1 0.11 <0.5 0.48 <0.1

MS2 200-235 17.3 0.03 <0.1 0.21 <0.5 0.36 0.10

3.1.6 Other metal concentrations in total digestion

Aluminum (Al) concentrations varied from 18.1 g/kg (OL-KK18) to 38.1 g/kg (OL-

KK19) in humus horizon. In mineral soil layers aluminum concentrations were highest

in OL-KK15 (62.8 g/kg) and in OL-KK14 (61.3 g/kg), indicating aluminum

enrichment (Figure 31). In well developed podzol profiles Al is precipitated in illuvial

horizons. Arsenic (As), cadmium (Cd), copper (Cu) and lead (Pb) concentrations were

highest in the humus horizons (Table 10). Cd concentrations varied from 0.17 mg/kg

(OL-KK19) to 1.58 mg/kg (OL-KK17). Cu concentrations varied from 16.0 mg/kg

(OL-KK19) to 71.3 mg/kg (OL-KK17) and Pb concentrations from 23.8 mg/kg (OL-

KK15) to 69.2 mg/kg (OL-KK18) in the humus horizons. Co and V concentrations

varied along the profile depths (Table 10). Co varied from 2.3 mg/kg to 15.7 mg/kg

and V concentration from 14.8 mg/kg to 76.6 mg/kg. Cu and Pb concentrations were

highest in the humus horizons. In general, Al, As, Co, Cu, Ni and V concentrations

were enriched in MS2 mineral soil layers, except in OL-KK17, where concentrations

were highest in the humus horizon.

42

MS5

MS4

MS3

MS2

MS1

Humus

0 10000 20000 30000 40000 50000 60000 70000

Al (mg/kg)

S

oil

La

ye

r


Figure 31. Total aluminum concentrations of OL-KK14…OL-KK19 in different soil

layers.

43

Table 10. Metal concentrations in total digestion (hydrofluoric acid-perchloric acid

digestion) in soil pits OL-KK14…OL-KK19 in different soil layers.

Soil

sample

Soil

layer

Sampling

depth

(cm)

Al

(mg/kg)

As

(mg/kg)

Cd

(mg/kg)

Co

(mg/kg)

Cu

(mg/kg)

Ni

(mg/kg)

Pb

(mg/kg)

V

(mg/kg)

OL-

KK14

Humus 0-5 21400 2.54 0.77 5.03 65.0 16.1 52.8 14.8

MS1 5-20 52800 4.12 <0.1 10.8 19.2 25.1 16.3 57.8

MS2 20-60 61300 5.77 0.22 15.7 27.4 37.1 21.1 76.6

MS3 60-105 49500 2.18 <0.1 7.71 16.7 21.1 20.3 44.8

MS4 105-240 47600 1.82 <0.1 7.74 13.8 17.2 15.0 42.2

OL-

KK15

Humus 0-7 23300 5.57 0.38 5.14 34.2 12.9 23.8 36.8

MS1 7-50 46300 0.54 <0.1 3.88 29.8 9.17 15.9 23.7

MS2 50-80 62800 6.56 0.12 14.8 25.9 32.6 23.2 73.4

MS3 80-110 47600 3.93 0.21 10.9 19.2 24.1 20.1 47.0

MS4 110-160 49500 2.49 <0.1 9.58 17.8 20.2 15.9 51.2

MS5 160-300 43900 1.44 <0.1 5.48 14.9 13.2 16.0 33.3

OL-

KK16

Humus 0-10 20200 6.25 0.74 4.05 52.2 17.7 29.6 30.7

MS1 10-30 44100 2.90 0.21 4.18 9.02 11.2 16.6 35.4

MS2 30-50 45000 2.46 <0.1 6.76 15.3 16.6 15.7 37.9

MS3 50-110 42300 1.61 <0.1 5.36 9.99 11.2 16.1 28.3

MS4 110-300 43000 1.09 <0.1 5.71 11.6 12.6 14.5 31.8

OL-

KK17

Humus 0-30 23400 7.19 1.58 9.28 71.3 30.9 26.9 24.9

MS1 30-46 43700 <0.5 <0.1 3.80 7.49 12.5 14.3 25.0

MS2 46-82 46400 1.65 <0.1 6.60 17.4 16.5 14.9 40.6

OL-

KK18

Humus 0-20 18100 1.90 0.64 2.29 25.9 10.9 69.2 18.1

MS1 20-200 46300 1.56 <0.1 7.23 16.1 17.7 15.7 40.4

MS2 200-220 44000 1.72 <0.1 6.44 11.6 13.2 15.0 36.0

OL-

KK19

Humus 0-20 38100 1.18 0.17 3.07 16.0 10.9 25.5 25.8

MS1 20-200 44500 1.49 <0.1 6.37 15.8 14.8 16.0 33.1

MS2 200-235 44400 1.47 <0.1 6.22 11.4 13.9 15.8 33.9

3.1.7 Iodine and selenium

Geochemical and biochemical behaviour of selenium (Se) is complex. In soils, selenium can be present in a number of different forms depending upon the soil redox conditions. The chemical form will influence selenium behaviour, including partitioning between liquid and solid phases and bioavailability. Microbial activity also has an influence on the form of selenium in soils. However, microbial activity is dependent on a number of factors, including nutrient availability, thus nutrient deficient soils may have a slower rate of microbial-induced speciation than nutrient-rich soils (Kabata-Pendias & Pendias 1992).

In both clay and sand soils, the majority of selenium has been found to be associated

with organic matter, with subsequently decreasing amounts of metal selenides and

elemental selenium. The binding of selenium to organic matter renders selenium less

bioavailable than that retained in solution. In sandy soils lower concentrations of each

Se forms have been found than in clay soils. It is concluded that to understand

selenium behavior in soils, speciation of selenium needs to be understood – different

forms can be available within the same soils (Kabata-Pendias & Pendias 1992).

Selenium concentrations were 5-10 higher in the humus horizons, ranging from 0.158

44

(OL-KK19) to 0.794 mg/kg (OL-KK16). In the mineral soil layers the range was 0.03

mg/kg to 0.197 mg/kg.

All iodine (I) compounds are readily soluble, therefore, weathering of rocks results in

the release of much of their content. Although iodine is known to be easily transported

by waters, its great sorption by carbon, organic matter and clays greatly influences

iodine cycling. The geochemistry of iodine is strongly connected to its involvement in

biological processes. The high iodine content of sediments and soils is mostly due to

uptake of iodine by plankton or is due to fixation of iodine by organic matter. The

association between iodine and organic matter, hydrous oxides of Fe and Al, and clay

of the chlorite-illite group has been noted. However, as Selezniev & Tiuriukanov

(1971) and Whitehead (1975) have reported, organic matter is most responsible for

iodine sorption in soil and therefore iodine is accumulated mainly in topsoil horizons.

The oxidation of iodine to iodate and further alteration to elemental iodine may occur

in soils and also exchange of volatile iodine compounds between soil and atmosphere.

Several ionic forms (I-, IO3) may occur in the aquatic phase of soil (Kabata-Pendias &

Pendias 1992).

Iodine concentrations were significantly higher in the humus horizons than in the

mineral soil layer. Iodine concentrations varied from 2.86 mg/kg (OL-KK19) to 29.7

mg/kg (OL-KK16) in the humus horizons. In the mineral soil layers iodine

concentrations were low, or under the detection limit (<0.05 mg/kg). The lowest values

were in OL-KK18 and OL-KK19. The results of iodine and selenium analysis are

presented in Table 11.

Table 11. A concentration of selenium and iodine in soil pits of OL-KK14…OL-KK19

in different soil layers.

Soil sample Soil layer Sampling

depth (cm)

Se

(mg/kg)

I

(mg/kg)

OL-KK14

Humus 0-5 0.696 12.6

MS1 5-20 0.113 0.967

MS2 20-60 0.135 0.69

MS3 60-105 0.087 0.203

MS4 105-240 0.080 0.14

OL-KK15

Humus 0-7 0.677 21.9

MS1 7-50 0.030 0.616

MS2 50-80 0.197 0.373

MS3 80-110 0.077 0.2

MS4 110-160 0.078 0.284

MS5 160-300 0.106 <0.05

OL-KK16

Humus 0-10 0.794 29.7

MS1 10-30 0.089 2.04

MS2 30-50 0.096 0.281

MS3 50-110 0.039 <0.05

MS4 110-300 0.052 <0.05

OL-KK17

Humus 0-30 0.742 20.1

MS1 30-46 0.100 0.491

MS2 46-82 0.068 0.475

OL-KK18

Humus 0-20 0.401 5.91

MS1 20-200 0.050 0.11

MS2 200-220 0.074 0.19

OL-KK19

Humus 0-20 0.158 2.86

MS1 20-200 0.047 0.17

MS2 200-235 0.101 0.08

45

3.2 Cation exchange capacity (CEC) and base saturation (BS)

Cations are positively charged ions such as calcium (Ca2+

), magnesium (Mg2+

),

potassium (K+), sodium (Na

+) hydrogen (H

+), aluminum (Al

3+), iron (Fe

2+), manganese

(Mn+), zinc (Zn

2+) and copper (Cu

2+). The capacity of the soil to hold on to these

cations is called the cation exchange capacity (CEC). These cations are held by the

negatively charged clay and organic matter particles in the soil through electrostatic

forces (negative soil particles attract the positive cations). Cation exchange on the

surfaces of soil particles is the most important buffering process in the humus horizons

(Evans 1980, Brady 1984). The cations on the CEC of the soil particles are easily

exchangeable with other cations and as a result, they are available to plants.

The cation exchange capacity of soil can be determined by two different methods:

potential and effective. In the potential CEC measurement the pH is adjusted to certain

value, as is used in this report (buffered (pH 4.5) ammonium acetate digestion). The

effective CEC is measured by unbuffered saline solution. The effective and potential

cation exchange can differ a lot (Westman 1991).

The cation exchange capacity was calculated by counting the alkaline and alkaline

earth metals of Ca2+

, Mg2+

, K+, Na

+ and acid ions (Al

3+, Fe

2+), and expressed in

mmol/kg. It should be noticed that the acid ions are not real acids but release hydrogen

ions from the soil solution (Westman 1991).

The cation exchange capacities of humus and mineral soil differ, depending on the

chemical and mineralogical composition of the soils, the decomposability of plant

residues in the soils, and microbiological activity. In mineral soils, cation exchange

takes place primarily in the fine fraction because of its large, negatively charged

surface area (Birkeland 1974). The clay and humus are essential cation reservoirs of

the soil and are very important because they improve the nutrient and water holding

capacity of the soil. However, CEC vary with the type of clay (Kabata-Pendias &

Pendias 1992).

The cation exchange capacity varied notably in different soil profiles (Table 12). In the

humus horizons CEC was significantly higher than in the mineral soil layers, the

variation was from 39.4 mmol/kg (OL-KK19) to 393 mmol/kg (OL-KK17). In the

mineral soil layers the CEC was highest in the parent material. The highest CEC-

values were found in the humus horizons of OL-KK16 and OL-KK17 (Figure 32). The

CEC values in OL-KK19 were notably lower (Table 12). Calcium was evidently the

predominant cation in all soil layers. In the humus horizons calcium contents varied

from 15.4 mmol/kg (OL-KK19) to 344 mmol/kg (OL-KK17).

Base saturation (BS %) refers to the fraction of the CEC that is occupied by the basic

cations (Ca2+

, Mg 2+

, K + and Na

+). Base saturation (BS) varied from 57.3 % (OL-

KK14) to 98.9 % (OL-KK17) in the humus horizons. In OL-KK14 and OL-KK15

aluminium (27.4 mmol/kg, 13.7 mmol/kg) and iron concentrations (18.5 mmol/kg,

40.0 mmol/kg) were high decreasing the amount of buffering base cations (Table 12).

In Figures 33-38 the cation exchange capacity and contribution of cations in different

soil pits are presented.

Table 12. Al, Ca, Mg, K, Na and Fe concentration (mmol/kg), cation exchange capacity (CEC mmol/kg) and base saturation (BS %) of OL-KK14…OL-KK19 in different soil layers.

Sample Sample

layer

Sampling

depth (cm)

Elements (mmol/kg) CEC

(Ca+Mg+K+Na+Al+

Fe)

(mmol/kg)

(Ca+Mg+K+Na)

(mmol/kg)

BS (%)

((Ca+Mg+K+Na)/

(Ca+Mg+K+Na+Al+

Fe))x 100 Al Ca Fe K Mg Na

OL-KK14

Humus 0-5 27.43 38.92 18.46 8.72 11.73 2.1 107.4 61.5 57.3

MS1 5-20 1.72 9.76 1.90 0.98 4.05 0.4 18.8 15.2 80.8

MS2 20-60 1.48 15.47 1.43 1.30 4.53 0.4 24.6 21.7 88.2

MS3 60-105 0.79 9.11 1.49 1.01 2.49 0.2 15.1 12.8 84.9

MS4 105-240 1.27 34.18 2.63 1.43 3.37 0.18 43.1 39.2 90.9

OL-KK15

Humus 0-7 13.68 89.32 39.96 4.99 8.66 1.39 158.0 104.4 66.1

MS1 7-50 2.56 3.09 1.62 0.41 0.81 0.13 8.6 4.4 51.5

MS2 50-80 3.28 16.87 3.39 3.45 5.09 1.08 33.2 26.5 79.9

MS3 80-110 1.57 27.20 2.29 1.56 2.74 0.54 35.9 32.0 89.2

MS4 110-160 2.19 46.41 4.01 3.66 4.94 0.83 62.0 55.8 90.0

MS5 160-300 0.69 33.43 1.54 1.53 2.59 0.43 40.2 38.0 94.5

OL-KK16

Humus 0-10 8.93 266.97 7.65 6.06 46.09 3.68 339.4 322.8 95.1

MS1 10-30 1.96 16.22 4.46 0.67 2.57 0.27 26.2 19.7 75.4

MS2 30-50 1.31 9.08 2.01 0.82 1.95 0.17 15.3 12.0 78.4

MS3 50-110 0.44 33.68 1.64 0.77 2.88 0.19 39.6 37.5 94.7

MS4 110-300 0.57 38.92 1.64 0.97 3.20 0.23 45.5 43.3 95.1

OL-KK17

Humus 0-30 4.00 344.31 0.35 6.47 35.64 2.03 392.8 388.5 98.9

MS1 30-46 1.19 17.02 0.17 0.44 1.22 - 20.0 18.7 93.2

MS2 46-82 0.75 12.92 0.94 0.73 1.30 0.26 16.9 15.2 90.0

OL-KK18

Humus 0-20 2.06 71.86 0.34 14.91 19.42 0.83 109.4 107.0 97.8

MS1 20-200 0.72 10.05 0.72 0.68 0.97 0.15 13.3 11.9 89.2

MS2 200-220 1.18 51.40 2.20 1.23 3.74 0.19 59.9 56.6 94.4

OL-KK19

Humus 0-20 9.27 15.37 6.18 2.08 6.01 0.47 39.4 23.9 60.8

MS1 20-200 0.74 37.67 0.80 0.71 1.08 - 41.0 39.5 96.2

MS2 200-235 0.64 40.17 0.95 0.94 2.20 - 44.9 43.3 96.5

- = under detection limit

46

47

Humus

MS1

MS2

MS3

MS4

MS5

0 100 200 300 400

CEC (mmol/kg)

S

oil L

ayer


Figure 32. Cation exchange capacity (CEC) of OL-KK14…OL-KK19 in different soil

layers.

OL-KK14

0 20 40 60 80 100 120 140 160 180 200 220 240 260 280 300 320 340 360 380 400

Humus

MS1

MS2

MS3

MS4

CEC (mmol/kg)

Ca

Mg

K

Na

Al

Fe

mmol/kg

Figure 33. Cation exchange capacity (CEC) mmol/kg in the soil pit OL-KK14 in different soil layers. The proportion of Ca, Mg, K, Na, Al and Fe are expressed separately.

48

OL-KK15

0 20 40 60 80 100 120 140 160 180 200 220 240 260 280 300 320 340 360 380 400

Humus

MS1

MS2

MS3

MS4

MS5

CEC (mmol/kg)

Ca

Mg

K

Na

Al

Fe

mmol/kg


OL-KK16

0 20 40 60 80 100 120 140 160 180 200 220 240 260 280 300 320 340 360 380 400

Humus

MS1

MS2

MS3

MS4

CEC (mmol/kg)

Ca

Mg

K

Na

Al

Fe

mmol/kg


49

OL-KK17

0 20 40 60 80 100 120 140 160 180 200 220 240 260 280 300 320 340 360 380 400

Humus

MS1

MS2

CEC (mmol/kg)

Ca

Mg

K

Na

Al

Fe

mmol/kg


OL-KK18

0 20 40 60 80 100 120 140 160 180 200 220 240 260 280 300 320 340 360 380 400

Humus

MS1

MS2

CEC (mmol/kg)

Ca

Mg

K

Na

Al

Fe

mmol/kg


50

OL-KK19

0 10 20 30 40 50

Humus

MS1

MS2

CEC (mmol/kg)

Ca

Mg

K

Na

Al

Fe

mmol/kg

Figure 38. Cation exchange capacity (CEC) mmol/kg in the soil pit OL-KK19 in different soil layers. The proportion of Ca, Mg, K, Na, Al and Fe are expressed separately (note the different scale).

51

3.3 Solubility of the main elements

The migration of elements and substances in soils takes place mainly through advection, dispersion, diffusion and evaporation and can be enhanced by complexation and colloidal sorption. The most effective sorptive compounds are organic matter, the oxyhydroxides of iron, aluminium and manganese and clay minerals. Sorption also increases with an increase in the specific surface area. The retention capacity of soil is limited and can be exceeded by excessive loading and lowered due to a change in chemical conditions. The soil mechanisms are mainly governed by the water content and structure of soil, by temperature and by the amount of complexing and colloidal compounds in soil. Migration is most effective when the water content and permeability of soil are high (Heikkinen 2001).

The solubility of elements in soil has great significance in their bioavailability and migration. Knowledge of the total composition of the soil solution and easily leachable fraction is essential; the uptake of a given ion depends on not only its activity in the solution but also on upon the activities of other ions and the relation that exists between solution ions and exchangeable or solid-phase ions. Soluble major ions greatly influence the quantities of soluble trace elements. Solutions of most soils contain an excess of calcium, which in many soils constitutes more than 80-90 % of the total cation concentration. Ca is, therefore, the most important cation in governing the soluble stage of trace elements in soil (Kabata-Pendias & Pendias 1992).

Methods used for obtaining solutions from soils differ widely; therefore it is difficult to adequately determine mean concentrations of trace elements. Rainfall, evaporation and plant transpiration can change trace element concentrations in soil solution more than tenfold, whereas the observed variation for major ions (Ca, Mg, K, Na, NO3, PO4) is much less. The acidification increases the intensity by which trace metals are mobilised in soil. The anionic composition of soil solution is also of importance in controlling the trace element status (Kabata-Pendias & Pendias 1992).

The bioavailable fraction (%) of the main elements soluble on ammonium acetate and total digestions was estimated by using the ratio of these digestions and expressed as percents (Table 13). The solubility of most analysed elements (Al, Ba, Ca, Co, Cr, Fe, K, Mg, Mn, Na, Ni, P and Zn) was significantly higher in the humus than in the mineral soil layers. In the mineral soil layers, exceptions were found in the solubility of copper, manganese and sulphur; solubility was generally higher in the mineral soil layers than in the humus horizons. In the OL-KK14 Al solubility-% (3.5 %) was threefold compared to the lowest value in OL-KK18 (0.31%). Calcium solubility varied from 14.2% (OL-KK19) to 58.0% (OL-KK17) in the humus horizons, in the mineral soil layers Ca solubility increased with depth. Magnesium solubility followed the pattern of calcium. Iron solubility was the highest in the humus horizons of OL-KK14 and OL-KK15. Sulphur solubility was the highest in the mineral soil layers of MS2, in general.

52

Table 13. Bioavailable fraction (%), (ammonium acetate concentrations mg/kg / total

concentrations mg/kg) *100.

- Not determined, value < the detection limit

Soil

sample

Soil layer Sampling

depth

(cm)

Bioavailable fraction (%)

Al As Ba Ca Co Cr Cu Fe K

OL-

KK14

Humus 0-5 3.5 10.2 10.3 38.2 28.4 3.3 1.6 9.4 3.8

MS1 5-20 0.09 1.2 2.5 3.8 - 0.20 3.3 0.43 0.18

MS2 20-60 0.07 1.0 2.0 5.0 - 0.12 3.3 0.3 0.2

MS3 60-105 0.04 4.13 1.2 4.4 - - 7.1 0.42 0.17

MS4 105-240 0.07 8.2 1.4 13.0 5.9 - 15.0 0.79 0.26

OL-

KK15

Humus 0-7 1.6 7.9 2.1 41.4 16.5 4.3 4.6 10.0 2.0

MS1 7-50 0.15 11.1 0.42 1.53 9.5 1.1 2.0 0.80 0.08

MS2 50-80 0.14 2.3 2.3 5.9 1.1 0.28 10.5 0.63 0.52

MS3 80-110 0.09 2.5 1.5 10.7 1.1 0.22 4.9 0.63 0.29

MS4 110-160 0.12 17.3 2.2 17.1 7.4 0.41 13.1 1.0 0.66

MS5 160-300 0.04 8.3 1.3 13.9 5.1 9.4 0.56 0.29

OL-

KK16

Humus 0-10 1.19 4.3 3.3 54.9 11.8 1.35 1.9 2.5 3.3

MS1 10-30 0.12 2.8 0.83 8.4 - 0.88 7.1 1.4 0.13

MS2 30-50 0.08 3.2 1.2 4.3 2.1 - 8.9 0.64 0.15

MS3 50-110 0.03 5.6 0.88 14.1 2.6 - 11.1 0.45 0.15

MS4 110-300 0.04 8.3 1.1 15.3 4.0 - 20.3 0.65 0.19

OL-

KK17

Humus 0-30 0.46 1.3 3.3 58.0 11.5 0.48 0.72 0.16 2.5

MS1 30-46 0.07 - 0.48 10.8 - - 4.9 0.07 0.07

MS2 46-82 0.04 - 0.95 6.1 - - 6.7 0.30 0.13

OL-

KK18

Humus 0-20 0.31 4.7 12.5 46.2 15.7 1.2 1.4 0.31 7.0

MS1 20-200 0.04 3.9 1.1 5.0 - - 3.3 0.23 0.12

MS2 200-220 0.07 7.6 1.1 19.4 6.8 - 17.4 0.77 0.24

OL-

KK19

Humus 0-20 0.66 10.2 2.4 14.2 12.7 2.1 3.3 2.8 0.43

MS1 20-200 0.04 3.4 0.91 16.6 1.7 - 4.5 0.28 0.13

MS2 200-235 0.04 2.0 0.87 16.6 3.4 - 14.8 0.34 0.17

53

Table 13. (cont´d.) Bioavailable fraction (%), (ammonium acetate concentrations

mg/kg / total concentrations mg/kg) *100.

Soil

sample

Soil layer Sampling

depth

(cm)

Bioavailable fraction (%)

Mg Mn Na Ni P S Sr Zn

OL-

KK14

Humus 0-5 20.7 26.6 1.0 14.1 3.8 9.6 16.5 37.1

MS1 5-20 1.3 0.36 0.06 - 0.92 - 1.4 0.53

MS2 20-60 1.1 0.35 0.06 - 2.4 7.4 1.5 0.41

MS3 60-105 1.0 1.1 0.04 - 4.1 10.6 0.93 0.84

MS4 105-240 1.4 13.3 0.03 4.1 3.0 9.7 1.0 2.0

OL-

KK15

Humus 0-7 16.7 4.6 0.48 15.7 3.6 8.6 20.1 11.0

MS1 7-50 0.91 1.6 0.02 - 1.7 10.2 0.69 1.1

MS2 50-80 2.0 2.7 0.16 2.1 1.4 21.7 2.5 1.3

MS3 80-110 1.8 4.3 0.09 - 1.9 9.4 1.6 0.94

MS4 110-160 2.8 15.4 0.15 6.3 3.9 10.6 2.5 2.1

MS5 160-300 2.3 10.8 0.08 3.9 3.7 5.6 1.4 1.7

OL-

KK16

Humus 0-10 32.8 8.9 2.2 8.7 2.2 4.5 21.7 28.3

MS1 10-30 1.4 0.22 0.05 - 1.1 6.7 1.0 0.22

MS2 30-50 1.0 0.83 0.03 - 2.5 11.8 0.85 1.6

MS3 50-110 1.8 8,6 0.03 - 2.9 5.8 1.2 1.5

MS4 110-300 1.9 12.5 0.04 - 3.2 5.9 1.2 1.5

OL-

KK17

Humus 0-30 22.9 27.0 0.99 3.1 2.4 4.0 24.5 15.4

MS1 30-46 0.72 0.89 - - 1.9 7.4 0.99 0.32

MS2 46-82 0.62 0.87 0.05 - 4.1 12.5 0.78 0.45

OL-

KK18

Humus 0-20 29.0 36.3 0.43 9.3 10.1 7.2 15.7 38.4

MS1 20-200 0.47 0.96 0.03 - 6.2 5.2 0.60 0.75

MS2 200-220 2.0 13.7 0.03 4.5 2.6 5.7 1.2 1.7

OL-

KK19

Humus 0-20 5.2 6.0 0.11 10.7 6.1 7.4 3.6 18.4

MS1 20-200 0.57 5.4 - - 2.4 - 0.91 1.7

MS2 200-235 1.2 8.6 - - 2.3 6.1 1.1 0.9

- Not determined, value < the detection limit

54

3.4 Grain size distribution and mineralogy

The grain size distribution of mineral soil samples and cumulative weight percent from

OL-KK14, OL-KK15 and OL-KK16 are presented in Appendices 4.1 and 4.2 (Lusa et

al. 2009). The soils were mainly fine-textured or sandy till. The proportion of fine

fraction (Ø <0.063 mm) increased after the uppermost mineral layer (MS1) and was

highest in MS2-layers of OL-KK14 and OL-KK15, being 37 % and 38 %, respectively.

In OL-KK16 the proportion of fine fraction was highest in MS3 (28 %). The amount of

clay (Ø <0.002 mm) varied from 0 to 12 % in OL-KK14…OL-KK16. The highest clay

contents were found in OL-KK14 and OL-KK15 in MS2 layers.

The grain size distribution of mineral soil samples and cumulative weight percent from

OL-KK17, OL-KK18 and OL-KK19 are presented in Appendices 4.3 and 4.4. The soil

type of OL-KK17 was sandy till. The clay content in MS1-layer was 1.8 % and

increased in the MS2-layer to (46-82 cm) to 8.3 %. In OL-KK18 and OL-KK19 soil

type was fine-textured till. In OL-KK18 clay content in MS1-layer (20-200 cm) was

9.3 % and increased to 12.8 % in MS2-layer (200-220 cm). In OL-KK19 clay content

was in MS1 (20-200 cm) 8.8 % and in MS2-layer (200-235 cm) 8.4 %. The stone

content varied in mineral soil layers from 2.4 % to 21.6 % being highest in MS2-layers

(19.8 - 21.6 %).

The mineral soils constituted mainly of quartz, potassium feldspar and plagioclase in OL-KK14…OL-KK16. The average quartz content in the mineral layers was 66 % and varied from 55 to 70 %. The average potassium feldspar proportion was 12 % and for plagioclase 19 % for all grain sizes. The small amounts (<5 %) of mica, chlorite and amphibole were found. The results corresponded to mineralogy of OL-KK6-OL-KK11 (Lintinen et al. 2003.) In addition, in some samples minor amounts of hematite and talc were found. The detailed description of mineralogy in OL-KK14, OL-KK15 and OL-KK16 is reported in Lusa et al. (2009). Mineralogical analyses of OL-KK17, OL-KK18 and OL-KK19 were not available.

55

4 CONCLUSIONS

The soils at Olkiluoto are young, thus the soil horizons are not yet well developed. Soil type is mainly sandy till or fine-textured till, containing some clay, sand, gravel and weathered layers. There was quite a large variation in acidity and elemental solubility of the investigated soil profiles, even in the three soil profiles (OL-KK17…OL-KK19) located only about ten meters from each other.

The surface soils were acid, but pH increased to neutral or alkaline as a function of depth, which is typical for the Finnish podzolised soil profiles. The base cation concentration and cation exchange capacity of the surface overburden have been found quite high compared to soils in inlands. The solubility of most analysed elements (Al, Ba, Ca, Co, Cr, Fe, K, Mg, Mn, Na, Ni, P and Zn) correlated positively with the organic matter content. However, base cations and other elements are expected to decrease in the future due to pedogenic processes, e.g. surface soil weathering, leaching and nutrient uptake and anthropogenic factors.

The soil mechanisms are mainly governed by the water content and structure of soil, by temperature and by the amount of complexing and colloidal compounds in soil. Migration is most effective when the water content and permeability of soil are high. The main reasons for the heterogeneous geochemistry Ol-KK14…OL-KK19 were mainly quite large variation in the humus properties and in the amount of clay and fine fraction contents between the soil pits and within different soil profile layers. Humus, clay and silt layers are the most active fraction in soils, e.g. due to their large reactive surface area.

Also the thickness of the sampling layers varied in the different soil pits, thus representing larger geochemical variation in some soil layers than in others. Also some anthropogenic factors could have affected natural stage of overburden; e.g. the OL-KK17…OL-KK19 located in the central part of island, which is the most extensively investigated area in the island. The soil pits OL-KK15 and OL-KK16 were selected from more natural areas (baseline areas), in the northern and eastern parts of the island. However, it is difficult to distinguish impacts of anthropogenic and natural factors.

When comparing results to earlier overburden investigations at Olkiluoto, the main

differences have been the investigation approaches; e.g. the sampling and analysing

methods used for obtaining geochemical and physical characteristics of the overburden

have been somewhat different. Although, there are still gaps in overburden data, all

overburden and related (e.g. soil water, groundwater, geophysics) investigations

broaden the scope and understanding of the site evolution, prevailing processes,

radionuclide transport and support modellining requirements.

The new overburden investigation locations should be selected based on relevance to surface and near-surface hydrological modelling, both formation of groundwater and possible routes of releases; and for the overburden modelling purposes, e.g. spatially lack of or low density data areas. The surface environments will evolve significantly on a timescale comparable to that of variations in the radionuclide release from the geosphere, for example areas currently sea bottom sediments will develop into terrestrial and limnic areas.

57

5 SUMMARY

The detailed soil investigations at Olkiluoto continued in the summer 2008. The six new soil pits were dug by excavator at the different parts of the island. The pit OL-KK14 is situated near the Liiklansuo mire and the main road; OL-KK15 in the northern part of the island, near the harbor road, and OL-KK16 in the north-eastern part, beside the Rumminperäntie road. The pits OL-KK17…OL-KK19 are located at the infiltration experiment site (Pitkänen et al. 2008b); west of the ONKALO underground rock characterisation facility and the Korvensuo freshwater reservoir.

Samples were taken from the vertical overburden profiles of the humus and two to five

mineral soil layers down to bedrock, if possible. The soils at Olkiluoto are very young

and thus soil profiles and horizons are not well developed, the sampling layers were

mainly selected after visual examination, e.g. according soil stratigraphy and type,

stoniness and color. The pH, moisture, dry and organic matter contents, carbon and

nitrogen were determined in the humus and mineral soil layers. Total organic carbon

was determined from the humus horizons of OL-KK14…OL-KK16.

The concentrations of the multi-element analysis of the easily leachable fraction were

measured with the buffered (pH 4.5) ammonium acetate and the total concentrations by

hydrofluoric acid-perchloric acid digestions using ICP-MS/ICP-OES-technique by

Labtium Ltd. The total cation exchange capacity (CEC) and base saturation (BS) were

calculated by using the exchangeable cations digested by the ammonium acetate. Also

selenium and iodine were measured. The grain size distribution was analysed from the

mineral soil layers. Mineralogy of OL-KK14…OL-KK16 is reported in (Lusa et al.

2009). Mineralogical analyses of OL-KK17…OL-KK19 were not available.

Overburden in the investigated soil pits was fine-grained and sandy till. However, sand and clay layers were common in the soil profiles. The clay content (Ø <0.002 mm) varied from 0 % to 12.8 % and was highest in OL-KK14 and OL-KK15. The fine fraction content (Ø <0.063 mm) varied from 1 % to 56.5 %. Observations of slightly chemically changed disintegrated rock layer (5-10 cm) were found in the contact of overburden and bedrock of OL-KK14. In the soil pits OL-KK14…OL-KK16 bedrock was at the depth of 290-320 cm. In OL-KK17…OL-KK19 the pits were not dug down to bedrock.

pH values varied in the humus layers from 3.3 to 5.4. In the different mineral soil layers pH ranged from 4.7 to 7.7 and increased as a function of depth, which is typical for the Finnish soil profiles. The pH variation between the soil pits was large; 2.1 pH units in the humus horizons and 3.0 units in the mineral soil layers. The dry-matter content increased as a function of depth, being in the humus horizons 49.8-69.1 % and in the subsoil layers 88.8-99.6 %. The organic matter and moisture contents decreased as a function of depth. The organic matter had a large variation in the humus layers, from 15.8 % (OL-KK19) to 58.5 % (OL-KK16).

The carbon content in the humus layers ranged from 9.9% (OL-KK19) to 31.9 % (OL-KK18), although these sites situated close to each other in the infiltration site. In the mineral soils layers the carbon content was <1 %. The nitrogen content ranged in the humus horizons from 0.29 (OL-KK19) to 2.02 % (OL-KK16), and in the mineral soil layers nitrogen content was low or under the detection limit. C/N ratio in the humus horizon varied from 15.7 % (OL-KK16) to 34.1 % (OL-KK19). In general, C and N

58

concentrations were in the range of studied top soil forest sampling plots at Olkiluoto (Tamminen et al. 2007).

The most nutrient rich soils were OL-KK16 and OL-KK17, while the soil of OL-KK19 was the most nutrient-poor of the studied sites. Easily leachable main nutrient contents were highest in the humus horizons. Calcium and magnesium were the dominating nutrients. Calcium was around 20 times and magnesium around 5 times higher in OL-KK16 and OL-KK17 than in OL-KK19. Also iodine and selenium concentrations were around seven times higher in OL-KK16 and OL-KK17 than in OL-KK19.

Cation exchange capacity and base saturation values varied by different soil profiles. The CEC was highest in the humus horizon of OL-KK16 and OL-KK17, calcium and magnesium being the dominating cations indicating the good buffering capacity of these soils. In OL-KK14 and OL-KK15 aluminium and iron concentrations were higher compared to base cation concentrations than in other studied soil pits. In OL-KK19 CEC and BS were low.

Sulphur, phosphorus, iron, zinc and sodium were enriched in the humus horizons. In the mineral soil layers aluminum and iron were enriched in MS1 and MS2 (the topmost mineral soil layers). Aluminium and iron concentrations were highest in OL-KK14 and OL-KK15, where the clay content was also the highest. Phosphorus, potassium, lead and zinc concentrations were highest in OL-KK14 and OL-KK18. The total concentrations of main trace elements showed an opposite pattern compared to ammonium acetate digested concentrations; iron, manganese, sodium and zinc concentration were not highest in the humus horizon, but in the mineral soil layers, mainly in MS1 and MS2 layers. The highest values were found in OL-KK14 and OL-KK15. The easily leachable metal concentrations showed a similar patter in Al, As, Cd, Co, Ni, Pb and V, being clearly higher in the humus horizons, especially aluminium, nickel and lead concentrations. The highest contents were in OL-KK14 and OL-KK15, and also lead in OL-KK18.

The bioavailable fraction (%) of the main elements soluble on ammonium acetate and total digestions was estimated by using the ratio of these digestions and expressed as percents. The solubility of most analysed elements (Al, Ba, Ca, Co, Cr, Fe, K, Mg, Mn, Na, Ni, P and Zn) was significantly higher in the humus layers than in the mineral soil layers. The main reasons for the heterogeneous geochemistry were mainly quite large variation in the thickness and quality of the humus horizons and in the amount of the clay and fine fraction contents between the soil pits and within different soil profile layers.

59

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65

APPENDICES

APPENDIX 1. Description of soil sampling sites and layers.

APPENDIX 2. Geochemical analysis results of the soil samples OL-KK14…OL-KK19 Appendix 2.1. pH, Carbon, nitrogen, moisture, dry matter, LOI, Se and I contents

Appendix 2.2. Element concentrations analysed by ammonium acetate (pH 4.5)

digestion

Appendix 2.3. Element concentrations analysed by hydrofluoric acid – perchloric acid

digestion

APPENDIX 3. Detection limits of ammonium acetate (pH 4.5) and hydrofluoric acid -

perchloric acid digestions

APPENDIX 4. Grain size distribution of OL-KK14…OL-KK19 Appendix 4.1. Grain size distribution of OL-KK14, OL-KK15 and OL-KK16

Appendix 4.2. Cumulative weight percent of different grain sizes of OL-KK14, OL-

KK15 and OL-KK16

Appendix 4.3. Grain size distribution of OL-KK17, OL-KK18 and OL-KK19

Appendix 4.4. Cumulative weight percent of different grain sizes of OL-KK17, OL-

KK18 and OL-KK19

- Cumulative grain size distribution of OL-KK17 in the mineral soil layer (30-46

cm) by sedigraph analysis and dry sieving.

- Cumulative grain size distribution of OL-KK17 in the mineral soil layer (46-82

cm) by sedigraph analysis and dry sieving.

- Cumulative gain size distribution of OL-KK18 in the mineral soil layer 20-200

cm by sedigraph analysis and dry sieving.

- Cumulative grain size distribution of OL-KK18 in the mineral soil layer (200-

220 cm) by sedigraph analysis and dry sieving.





Appendix 1. Description of soil sampling sites and layers. Soil pit Sampling layer Thickness of

sampling soil layer (cm)

Sampling depth (cm)

Soil type Description of sampling layer

OL-KK14 Humus 5 0-5

Location at Olkiluoto

MS1 15 5-20 Sandy till Brownish grey, undeveloped horizon

Between the Olkiluoto main road and Forest Intensive Plot (FIP4)

MS2 38 20-60 Sandy till Brownish grey, some stones

Description of vegetation

MS3 48 60-105 Sandy till Brownish, very stony

Pine, spruce, some birches, junipers. Undergrowth: bilberry, lingonberry, moss, grass, wood anemone

MS4 110-130 105-240 Clay Bluish, tight, groundwater level on the bottom

Bedrock at the depth of 240 cm

OL-KK15 Humus 7 0-7 Location at Olkiluoto

MS1 40 7-50 Sand Sandy lenses, stony

Beside of the end of the Harbour road

MS2 32 50-80 Fine-grained silty/clayish till

Sandy lenses, stones, some stratification


MS3 30 80-110 Fine sand Some sandy lenses on the top of the layer

Quite young birch forest, next to it dense old spruce forest. Undergrowth: mainly grass, lingonberry, moss and may lily

MS4 53 110-160 Clay Brownish, big stones, loose, moist

MS5 140 160-300 Coarse-grained sandy till

Sandy lenses, stony

Bedrock at the depth of 300-320 cm

OL-KK16 Humus 10 0-10 Location at Olkiluoto

MS1 22 10-30 Coarse sand Brownish, some stones

Beside the Rumminperäntie road

MS2 15-20 30-50 Sand Greenish brown, some stones


MS3 60 50-110 Fine to coarse sand

Stones including some reddish Satakunta sandstones

Spruce, some birches. Undergrowth: moss, grass, lingonberry

MS4 170-190 110-300 Sandy till Greyish, some big stones, bottom layer more loose and moist

Bedrock at the depth of 300 cm

67

Appendix 1. (cont´d) Description of soil sampling sites and layers. Soil pit Sampling layer Thickness of

sampling soil layer (cm)

Sampling depth (cm)

Soil type Description of sampling layer

OL-KK17 Humus 30 0-30


MS1 16 30-46 Sandy till No information

In the Infiltration Experiment area

MS2 36 46-82 Sandy till No information


Bedrock was not reached

Mixed forest: pine, spruce, birch



MS1 180 20-200 Fine-grained/clayey till

Stones (ø 0.5-1.0 m)


MS2 20 200-220 Clay Grey and tight






MS1 180 20-200 Fine-grained/clayey till

Stones (ø 0.5-1.0 m)


MS2 35 200-235 Clay Grey and tight




68

Appendix 2.1. pH, carbon, nitrogen, moisture, dry matter, loss on ignition (LOI, organic matter content), selenium (Se) and iodine(I) contents.

Soil sample

Soil layer

Sampling depth (cm)

pH Carbon

mass-%dw Moisture mass-%

Dry matter mass- %dw

LOI mass-%dw

Nitrogen mass-%dw

TOC %

Sedw (mg/kg)

Idw (mg/kg)

Humus 0-5 3.64 30.5 31.4 68.6 50.7 1.41 28 0.696 12.6

MS1 5-20 5.18 0.20 7.50 92.5 0.92 <0.03 - 0.113 0.967

MS2 20-60 5.70 0.27 11.2 88.8 0.16 0.04 - 0.135 0.69

MS3 60-105 5.81 0.13 5.30 94.7 0.61 <0.03 - 0.087 0.203

OL-KK14

MS4 105-240 7.59 0.18 7.30 92.7 0.55 <0.03 - 0.080 0.14

Humus 0-7 3.88 21.9 33.8 66.2 39.1 1.18 22 0.677 21.9

MS1 7-50 4.66 0.22 0.40 99.6 0.66 0.04 - 0.030 0.616

MS2 50-80 6.45 0.33 2.60 97.4 1.32 0.04 - 0.197 0.373

MS3 80-110 6.96 0.18 0.80 99.2 0.75 <0.03 - 0.077 0.2

MS4 110-160 7.48 0.23 2.00 98.0 0.76 0.03 - 0.078 0.284

OL-KK15

MS5 160-300 7.66 0.14 0.70 99.3 0.41 <0.03 - 0.106 <0.05

Humus 0-10 4.83 31.8 48.1 51.9 58.5 2.02 32 0.794 29.7

MS1 10-30 5.44 0.64 8.50 91.5 1.83 0.07 - 0.089 2.04

MS2 30-50 6.29 0.14 2.60 97.4 0.60 <0.03 - 0.096 0.281

MS3 50-110 7.32 0.13 1.30 98.7 0.36 <0.03 - 0.039 <0.05

OL-KK16

MS4 110-300 7.52 0.13 3.90 96.1 0.36 <0.03 - 0.052 <0.05

Humus 0-30 5.40 26.3 49.2 50.8 45.7 0.98 - 0.742 20.1

MS1 30-46 5.90 0.41 3.80 96.2 1.16 0.05 - 0.100 0.491

OL-KK17

MS2 46-82 6.56 0.12 5.60 94.4 0.68 <0.03 - 0.068 0.475

Humus 0-20 3.47 31.9 50.2 49.8 49.7 1.17 - 0.401 5.91

MS1 20-200 6.03 0.07 8.10 91.9 0.54 <0.03 - 0.050 0.11

OL-KK18

MS2 200-220 7.22 0.18 9.50 90.5 0.45 <0.03 - 0.074 0.19

Humus 0-20 3.33 9.89 30.9 69.1 15.8 0.29 - 0.158 2.86

MS1 20-200 7.42 0.11 7.80 92.2 0.42 <0.03 - 0.047 0.17

OL-KK19

MS2 200-235 7.67 0.14 8.40 91.6 0.43 <0.03 - 0.101 0.08

69

Appendix 2.2. Bioavailble element concentrations (dry weight) analysed by ammonium acetate (pH 4.5) digestion.

NH4Ac digestion, pH 4.5 (mg/kg) Soil sample

Soil layer

Sampling depth (cm)

Al As B Ba Ca Cd Co Cr Cu Fe K Li Mg

Humus 0-5 740 0.26 <0.5 21.3 1560 0.38 1.42 0.73 1.04 1030 341 <0.05 285

MS1 5-20 46.3 0.05 <0.5 11.5 391 <0.1 <0.1 0.11 0.64 106 38.5 0.15 98.3

MS2 20-60 40.0 0.06 <0.5 10.4 620 <0.1 <0.1 0.10 0.91 80.0 51.0 0.19 110

MS3 60-105 21.4 0.09 <0.5 5.10 365 <0.1 <0.1 <0.1 1.18 83.4 39.4 0.11 60.5

OL-KK14

MS4 105-240 34.3 0.15 <0.5 5.63 1370 <0.1 0.46 <0.1 2.07 147 56.1 0.09 81.8

Humus 0-7 369 0.44 <0.5 4.15 3580 0.24 0.85 1.08 1.57 2230 195 0.06 347

MS1 7-50 69.1 0.06 <0.5 1.73 124 <0.1 0.37 0.25 0.60 90.4 16.2 <0.05 32.6

MS2 50-80 88.6 0.15 <0.5 12.4 676 <0.1 0.16 0.19 2.72 189 135 0.22 204

MS3 80-110 42.4 0.10 <0.5 6.26 1090 <0.1 0.12 0.11 0.94 128 61.0 0.12 110

MS4 110-160 59.0 0.43 <0.5 9.61 1860 <0.1 0.71 0.19 2.33 224 143 0.22 198

OL-KK15

MS5 160-300 18.5 0.12 <0.5 4.93 1340 <0.1 0.28 <0.1 1.40 85.7 59.7 0.07 104

Humus 0-10 241 0.27 <0.5 5.05 10700 0.41 0.48 0.44 1.02 427 237 0.1 1120

MS1 10-30 52.8 0.08 <0.5 3.30 650 <0.1 <0.1 0.30 0.64 249 26.2 0.08 62.5

MS2 30-50 35.4 0.08 <0.5 4.63 364 <0.1 0.14 <0.1 1.36 112 31.9 0.11 47.5

MS3 50-110 11.9 0.09 <0.5 3.43 1350 <0.1 0.14 <0.1 1.11 62.3 30.3 <0.05 69.9

OL-KK16

MS4 110-300 15.3 0.09 <0.5 4.26 1560 <0.1 0.23 <0.1 2.36 91.5 37.8 0.05 77.8

Humus 0-30 108 0.09 0.82 5.38 13800 0.73 1.07 0.16 0.51 19.7 253 0.16 866

MS1 30-46 32.2 <0.03 <0.5 1.77 682 <0.1 <0.1 <0.1 0.37 9.36 17.2 0.10 29.7

OL-KK17

MS2 46-82 20.3 0.09 <0.5 3.79 518 <0.1 <0.1 <0.1 1.16 52.7 28.5 0.12 31.6

Humus 0-20 55.5 0.09 <0.5 23.8 2880 0.50 0.36 0.19 0.37 18.7 583 0.06 472

MS1 20-200 19.4 0.06 <0.5 4.07 403 <0.1 <0.1 <0.1 0.53 40.2 26.5 0.08 23.6

OL-KK18

MS2 200-220 31.9 0.13 <0.5 4.34 2060 <0.1 0.44 <0.1 2.02 123 48.0 0.09 90.9

Humus 0-20 250 0.12 <0.5 7.59 616 0.16 0.39 0.66 0.53 345 81.2 0.06 146

MS1 20-200 20.0 0.05 <0.5 3.46 1510 <0.1 0.11 <0.1 0.71 44.7 27.6 0.06 26.2

OL-KK19

MS2 200-235 17.3 0.03 <0.5 3.29 1610 <0.1 0.21 <0.1 1.69 52.8 36.7 0.06 53.4

70

Appendix 2.2. (cont`d) Bioavailble element concentrations (dry weight) analysed by ammonium acetate (pH 4.5) digestion.

NH4Ac digestion, pH 4.5 (mg/kg) Soil sample

Soil layer

Sampling depth (cm)

Mn Mo Na Ni P Pb S Sb Sr Ti V Zn

Humus 0-5 27.4 <0.03 49.0 2.27 36.5 16.5 91.9 0.01 9.82 2.39 0.26 22.6

MS1 5-20 1.83 <0.03 8.76 <0.5 4.80 0.44 4.93 <0.01 1.98 0.25 <0.1 0.31

MS2 20-60 2.12 <0.03 9.25 <0.5 16.7 0.36 5.21 <0.01 2.22 0.25 <0.1 0.30

MS3 60-105 3.61 <0.03 4.43 <0.5 21.3 4.87 17.5 <0.01 1.12 0.20 <0.1 0.45

OL-KK14

MS4 105-240 44.3 0.03 4.16 0.71 14.8 0.86 58.5 0.01 1.34 0.24 0.31 0.96

Humus 0-7 7.47 0.04 32.0 2.02 23.9 5.49 91.1 0.01 19.6 3.61 0.74 2.81

MS1 7-50 2.87 0.06 3.07 <0.5 6.61 0.20 7.89 <0.01 0.91 0.49 0.11 0.36

MS2 50-80 14.0 <0.03 24.9 0.67 8.81 1.02 36.4 0.01 3.57 0.24 <0.1 1.07

MS3 80-110 16.9 <0.03 12.3 <0.5 10.0 0.59 19.6 <0.01 2.12 0.20 <0.1 0.53

MS4 110-160 62.4 0.07 19.1 1.27 18.8 1.97 68.2 0.02 3.30 0.30 0.66 1.16

OL-KK15

MS5 160-300 29.2 0.05 9.79 0.51 16.1 4.82 35.1 <0.01 1.68 0.22 0.23 0.81

Humus 0-10 7.89 <0.03 84.6 1.54 18.2 7.25 83.1 0.01 15.4 0.75 0.37 9.73

MS1 10-30 0.46 0.03 6.27 <0.5 4.71 0.37 14.2 <0.01 1.24 0.46 0.21 0.16

MS2 30-50 2.02 <0.03 3.88 <0.5 12.3 0.39 12.5 <0.01 1.07 0.16 <0.1 0.87

MS3 50-110 22.0 <0.03 4.34 <0.5 12.4 0.50 26.9 <0.01 1.54 0.25 <0.1 0.60

OL-KK16

MS4 110-300 33.5 0.05 5.35 <0.5 13.4 0.54 32.0 <0.01 1.53 0.20 0.21 0.66

Humus 0-30 61.6 <0.03 46.6 0.97 16.5 3.20 56.0 0.01 20.5 <0.1 0.10 12.20

MS1 30-46 1.70 <0.03 <3 <0.5 9.26 <0.1 11.1 <0.01 1.02 0.18 <0.1 0.13

OL-KK17

MS2 46-82 2.56 <0.03 6.01 <0.5 19.8 0.25 7.87 <0.01 0.95 0.21 <0.1 0.21

Humus 0-20 153 <0.03 19.1 1.01 73.0 17.5 68.2 0.01 8.57 1.00 0.19 43.0

MS1 20-200 2.99 <0.03 3.44 <0.5 28.5 0.32 3.31 <0.01 0.71 0.24 <0.1 0.38

OL-KK18

MS2 200-220 43.3 0.03 4.33 0.59 12.3 0.78 36.9 <0.01 1.59 0.23 0.38 0.76

Humus 0-20 7.51 <0.03 10.8 1.17 25.7 5.68 17.5 <0.01 3.10 2.18 0.23 8.00

MS1 20-200 14.5 <0.03 <3 <0.5 11.2 0.48 <2 <0.01 1.09 0.31 <0.1 0.79

OL-KK19

MS2 200-235 23.8 0.03 <3 <0.5 10.7 0.36 31.9 <0.01 1.37 0.25 0.10 0.38

71

Appendix 2.3. Total element concentrations (dry weight) analysed by hydrofluoric acid-perchloric acid digestion.

Hydrofluoric acid-perchloric acid digestion (mg/kg) Soil sample

Soil layer Sampling depth (cm) Al As Ba Be Bi Ca Cd Co Cr Cu

Humus 0-5 21400 2.54 207 <0.5 0.43 4080 0.77 5.03 21.8 65.0

MS1 5-20 52800 4.12 464 1.88 0.16 10400 <0.1 10.8 53.8 19.2

MS2 20-60 61300 5.77 518 2.64 0.20 12300 0.22 15.7 84.7 27.4

MS3 60-105 49500 2.18 416 1.24 0.38 8370 <0.1 7.71 45.9 16.7

OL-KK14

MS4 105-240 47600 1.82 404 1.42 0.28 10500 <0.1 7.74 41.9 13.8

Humus 0-7 23300 5.57 198 1.08 0.43 8650 0.38 5.14 24.8 34.2

MS1 7-50 46300 0.54 416 0.57 0.15 8120 <0.1 3.88 23.7 29.8

MS2 50-80 62800 6.56 536 2.10 0.43 11500 0.12 14.8 66.9 25.9

MS3 80-110 47600 3.93 430 1.61 0.25 10200 0.21 10.9 49.0 19.2

MS4 110-160 49500 2.49 443 0.71 0.15 10900 <0.1 9.58 46.2 17.8

OL-KK15

MS5 160-300 43900 1.44 383 1.16 0.26 9670 <0.1 5.48 30.7 14.9

Humus 0-10 20200 6.25 152 <0.5 0.32 19500 0.74 4.05 32.7 52.2

MS1 10-30 44100 2.90 400 1.44 0.23 7700 0.21 4.18 34.1 9.02

MS2 30-50 45000 2.46 398 1.30 0.15 8390 <0.1 6.76 35.3 15.3

MS3 50-110 42300 1.61 391 0.60 0.13 9610 <0.1 5.36 26.0 9.99

OL-KK16

MS4 110-300 43000 1.09 397 0.65 0.13 10200 <0.1 5.71 28.0 11.6

Humus 0-30 23400 7.19 161 <0.5 0.62 23800 1.58 9.28 33.2 71.3

MS1 30-46 43700 <0.5 367 0.76 0.11 6310 <0.1 3.80 33.5 7.49

OL-KK17

MS2 46-82 46400 1.65 398 0.72 0.30 8440 <0.1 6.60 36.6 17.4

Humus 0-20 18100 1.90 191 <0.5 0.97 6230 0.64 2.29 16.1 25.9

MS1 20-200 46300 1.56 384 0.59 0.28 8050 <0.1 7.23 39.6 16.1

OL-KK18

MS2 200-220 44000 1.72 393 1.14 0.14 10600 <0.1 6.44 36.4 11.6

Humus 0-20 38100 1.18 315 0.94 0.24 4330 0.17 3.07 31.4 16.0

MS1 20-200 44500 1.49 381 1.08 0.25 9070 <0.1 6.37 34.5 15.8

OL-KK19

MS2 200-235 44400 1.47 380 0.93 0.28 9680 <0.1 6.22 33.1 11.4

72

Appendix 2.3. (cont`d) Total element concentrations (dry weight) analysed by hydrofluoric acid-perchloric acid digestion.


Soil layer Sampling depth (cm) Fe K Li Mg Mn Mo Na Ni P Pb

Humus 0-5 10900 9040 <5 1380 103 1.22 4730 16.1 965 52.8

MS1 5-20 24900 21900 23.8 7430 510 0.72 13900 25.1 524 16.3

MS2 20-60 31800 24600 31.2 9870 604 0.95 14700 37.1 706 21.1

MS3 60-105 20000 23400 23.6 6040 343 <0.5 12500 21.1 514 20.3

OL-KK14

MS4 105-240 18500 21500 19.8 5660 334 <0.5 13400 17.2 499 15.0

Humus 0-7 22300 9680 5.83 2080 164 4.15 6730 12.9 668 23.8

MS1 7-50 11300 21600 16.7 3590 183 <0.5 15000 9.17 380 15.9

MS2 50-80 30200 26100 40.2 9980 518 1.45 15800 32.6 630 23.2

MS3 80-110 20400 21000 19.7 6050 391 0.58 13200 24.1 514 20.1

MS4 110-160 22000 21700 22.2 6940 405 0.55 12900 20.2 479 15.9

OL-KK15

MS5 160-300 15300 20800 15.4 4500 271 <0.5 12700 13.2 429 16.0

Humus 0-10 16900 7090 9.18 3410 89.1 2.36 3840 17.7 837 29.6

MS1 10-30 17600 20600 16.9 4380 209 1.42 12400 11.2 421 16.6

MS2 30-50 17500 20900 17.7 4710 243 <0.5 12900 16.6 500 15.7

MS3 50-110 13800 19700 12.7 3930 256 <0.5 12900 11.2 422 16.1

OL-KK16

MS4 110-300 14000 20100 13.8 4060 268 <0.5 13600 12.6 416 14.5

Humus 0-30 12600 10100 12.7 3780 228 0.99 4730 30.9 679 26.9

MS1 30-46 14400 23400 18.1 4130 191 <0.5 11600 12.5 489 14.3

OL-KK17

MS2 46-82 17800 21600 17.7 5120 293 <0.5 12700 16.5 482 14.9

Humus 0-20 5970 8350 5.93 1630 421 0.96 4460 10.9 724 69.2

MS1 20-200 17600 22200 17.3 5010 311 <0.5 12400 17.7 459 15.7

OL-KK18

MS2 200-220 16000 20200 13.9 4610 315 <0.5 13400 13.2 475 15.0

Humus 0-20 12300 19100 10.2 2820 126 0.52 9490 10.9 419 25.5

MS1 20-200 16000 21600 16.5 4600 266 1.07 12500 14.8 461 16.0

OL-KK19

MS2 200-235 15600 21400 18.0 4600 275 <0.5 12600 13.9 457 15.8

73

Appendix 2.3. (cont´d) Total element concentrations (dry weight) analysed by hydrofluoric acid- perchloric acid digestion.


Soil layer Sampling depth (cm) Rb S Sb Sn Sr Ti Tl V Zn Zr

Humus 0-5 41.6 957 0.74 <2 59.5 752 0.43 14.8 60.9 47.7

MS1 5-20 106 <50 0.20 2.20 139 3250 0.69 57.8 58.7 132

MS2 20-60 138 70.2 0.45 3.07 149 4370 0.80 76.6 73.9 144

MS3 60-105 114 165 0.21 <2 121 2350 0.54 44.8 53.8 120

OL-KK14

MS4 105-240 97.2 600 0.25 <2 132 2310 0.46 42.2 48.4 127

Humus 0-7 50.2 1060 0.27 <2 97.4 1060 0.54 36.8 25.6 74.6

MS1 7-50 106 77.6 0.11 <2 131 1270 0.53 23.7 32.5 70.1

MS2 50-80 147 168 0.36 2.63 144 3160 0.78 73.4 82.6 120

MS3 80-110 116 209 0.35 2.59 131 2300 0.69 47.0 56.2 122

MS4 110-160 102 643 0.28 2.00 131 2530 0.44 51.2 55.4 110

OL-KK15

MS5 160-300 95.7 623 0.11 <2 123 1840 0.39 33.3 48.3 116

Humus 0-10 45.6 1860 0.46 <2 71.0 1170 0.52 30.7 34.4 47.3

MS1 10-30 102 212 0.14 <2 123 1760 0.48 35.4 72.8 80.7

MS2 30-50 102 106 0.21 <2 126 2030 0.57 37.9 53.6 116

MS3 50-110 86.3 460 0.14 <2 126 1800 0.35 28.3 39.8 111

OL-KK16

MS4 110-300 90.3 544 0.14 <2 132 1880 0.44 31.8 45.2 113

Humus 0-30 69.5 1400 0.71 <2 83.8 853 0.44 24.9 79.3 55.4

MS1 30-46 115 149 0.13 <2 103 1350 0.50 25.0 40.9 79.1

OL-KK17

MS2 46-82 101 63.1 <0.1 <2 122 2010 0.44 40.6 46.7 109

Humus 0-20 37.3 942 1.08 <2 54.5 901 0.19 18.1 112 43.9

MS1 20-200 107 63.4 0.15 <2 119 2060 0.57 40.4 50.4 114

OL-KK18

MS2 200-220 86.8 649 <0.1 <2 132 2150 0.37 36.0 44.9 123

Humus 0-20 99.7 237 0.17 2.07 85.3 1230 0.54 25.8 43.5 58.6

MS1 20-200 99.5 94.4 0.12 <2 120 1910 0.46 33.1 47.5 109

OL-KK19

MS2 200-235 99.7 520 0.15 2.04 122 1940 0.55 33.9 44.3 121

74

Appendix 3. Detection limits (mg/kg) of ammonium acetate (pH 4.5) and hydrofluoric acid-perchloric acid digestion.

Detection limit (mg/kg)

Element NH4Ac digestion

(bioavailble)

Hydrofluoric acid-perchloric acid

digestion (total concentration)

Al 2 100 As 0.03 0.5 B 0.5 - Ba 0.1 0.5 Be - 0.5 Bi - 0.1 Ca 5 200 Cd 0.1 0.1 Co 0.1 0.2 Cr 0.1 4 Cu 0.1 2 Fe 5 100 I 0.05 - K 10 200 Li 0.05 5 Mg 5 50 Mn 0.05 5 Mo 0.03 0.5 Na 3 200 Ni 0.5 4 P 2 100 Pb 0.1 1 Rb - 0.2 S 2 50 Sb 0.01 0.1 Se 0.01 - Sn - 2 Sr 0.05 3 Ti 0.1 10 Tl - 0.1 V 0.1 5 Zn 0.1 20 Zr - 10

- Not analysed

75

Appendix 4.1. The grain size distribution of OL-KK14, OL-KK15 and OL-KK16 in different mineral soil layers (Lusa et al. 2009).

Sampling site Layer <0.002 mm %

0.002-0.006 mm %

0.063-0.125 mm %

0.125-0.25 mm

%

02.5 -0.5 mm %

0.5-1.0 mm %

1.0-2.0 mm %

>2.0 mm %

OL-KK14 MS1 5-20 cm 1 4 15 15 20 14 7 24

OL-KK14 MS2 20-60 cm 11 26 7 12 16 13 9 6

OL-KK14 MS3 60-105 cm 6 20 12 12 15 12 10 13

OL-KK14 MS4 105-240 cm 5 25 15 13 13 11 11 7

OL-KK15 MS1 7-50 cm 0 1 3 9 15 10 20 42

OL-KK15 MS2 50-80 cm 12 26 2 12 15 13 11 9

OL-KK15 MS3 80-110 cm 5 22 15 14 13 12 8 11

OL-KK15 MS4 110-160 cm 8 15 11 12 19 16 13 6

OL-KK15 MS5 160-300 cm 4 15 15 15 13 9 9 20

OL-KK16 MS1 10-30 cm 2 8 8 9 13 12 20 28

OL-KK16 MS2 30-50 cm 6 19 12 11 15 11 11 15

OL-KK16 MS3 50-110 cm 5 23 17 16 14 8 6 11

OL-KK16 MS4 110-300 cm 4 23 18 16 15 6 7 11

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Appendix 4.2. The cumulative weight percent of different grain sizes of OL-KK14, OL-KK15 and OL-KK16 in different mineral soil layer (Lusa et al. 2009).


<0.006 mm %

<0.125 mm %

<0.25 mm %

<0.5 mm %

<1.0 mm %

<2.0 mm %

>2.0 mm %

OL-KK14 MS1 5-20 cm 1 5 20 35 55 69 76 100

OL-KK14 MS2 20-60 cm 11 37 44 56 72 85 94 100

OL-KK14 MS3 60-105 cm 6 26 38 50 65 77 87 100

OL-KK14 MS4 105-240 cm 5 30 45 58 71 82 93 100

OL-KK15 MS1 7-50 cm 0 1 4 13 28 38 58 100

OL-KK15 MS2 50-80 cm 12 38 40 52 67 80 91 100

OL-KK15 MS3 80-110 cm 5 27 42 56 69 81 89 100

OL-KK15 MS4 110-160 cm 8 23 34 46 65 81 94 100

OL-KK15 MS5 160-300 cm 4 19 34 49 62 71 80 100

OL-KK16 MS1 10-30 cm 2 10 18 27 40 52 72 100

OL-KK16 MS2 30-50 cm 6 25 37 48 63 74 85 100

OL-KK16 MS3 50-110 cm 5 28 45 61 75 83 89 100

OL-KK16 MS4 110-300 cm 4 27 45 61 76 82 89 100

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Appendix 4.2. The cumulative weight percent of different grain sizes of OL-KK14 (above) and OL-KK15 (below) (Lusa et al. 2009).

79

Appendix 4.2. The cumulative weight percent of different grain sizes of OL-KK16 (Lusa et al. 2009).

80

Appendix 4.3. The grain size distribution of OL-KK17, OL-KK18 and OL-KK19 in different mineral soil layers and stone content.


0.0006- 0.001 mm

%

0.001-0.002 mm %

0.002-0.004 mm

%

0.004-0.006 mm

%

0.006-0.01 mm

%

0.01-0.016 mm

%

0.016-0.02 mm

%

0.02-0.03 mm %

OL-KK17 MS1 20-46 cm 3.9 1.4 4.0 5.4 2.9 3.7 3.9 2.2 4.6

OL-KK17 MS2 46-82 cm 1.2 0.2 0.4 0.8 0.3 0.6 0.7 0.3 0.9

OL-KK18 MS1 20-200 cm 3.7 1.8 4.0 5.0 2.8 3.6 3.8 2.1 4.3

OL-KK18 MS2 200-220 cm 6.7 1.6 4.5 7.0 4.4 6.8 7.0 3.5 6.1

OL-KK19 MS1 20-200 cm 4.1 1.3 3.4 4.8 2.8 4.1 4.3 2.3 5.2

OL-KK19 MS2 200-235 cm 3.8 1.0 3.6 4.6 2.8 4.0 4.5 2.5 5.2

Sampling site Layer 0.03-0.04 mm %

0.04-0.05 mm %

0.05-0.06 mm %

0.063-0.06 mm

%

0.06-0.02 mm %

0.02-0.63 mm %

0.63-2.0 mm %

>2.0 mm %

Stones %

OL-KK17 MS1 20-46 cm 0.7 0.4 0.2 0.2 26.3 24.5 28.4 13.9 2.44

OL-KK17 MS2 46-82 cm 3.5 2.1 0.8 0.4 21.2 19.2 12.3 8.9 21.6

OL-KK18 MS1 20-200 cm 3.2 1.9 0.8 0.5 20.5 18.4 13.2 10.4 19.9

OL-KK18 MS2 200-220 cm 4.4 2.4 0.9 1.2 21.2 13.3 5.6 3.4 2.88

OL-KK19 MS1 20-200 cm 3.7 2.0 0.8 1.0 22.2 18.6 12.0 6.4 18.9

OL-KK19 MS2 200-235 cm 3.8 2.4 0.9 0.9 24.3 19.2 11.2 5.3 7.8

81

Appendix 4.4. The cumulative weight percent of different grain sizes of OL-KK17, OL-KK18 and OL-KK19 in different mineral soil layers.


<0.001 mm %

<0.002 mm %

<0.004 mm %

<0.006 mm %

<0.01 mm %

<0.016 mm %

<0.02 mm %

<0.03 mm %

OL-KK17 MS1 20-46 cm 1.2 1.4 1.8 2.6 2.9 3.5 4.2 4.5 5.4

OL-KK17 MS2 46-82 cm 3.6 5.0 8.3 12.8 15.4 18.8 22.4 24.4 28.5

OL-KK18 MS1 20-200 cm 3.9 5.3 9.3 14.7 17.6 21.3 25.2 27.4 32.0

OL-KK18 MS2 200-220 cm 6.7 8.3 12.8 19.8 24.2 31.0 38.0 41.5 47.6

OL-KK19 MS1 20-200 cm 4.1 5.4 8.8 13.6 16.4 20.5 24.8 27.1 32.3

OL-KK19 MS2 200-235 cm 3.8 4.8 8.4 13 15.8 19.8 24.3 26.8 32.0


<0.05 mm %

<0.06 mm %

<0.063mm %

<0.02 mm %

<0.63 mm %

<2.0 mm %

>6.3 mm

OL-KK17 MS1 20-46 cm 6.1 6.5 6.7 6.9 33.2 57.7 86.1 100

OL-KK17 MS2 46-82 cm 31.5 33.3 34.0 34.8 55.0 74.8 87.6 100

OL-KK18 MS1 20-200 cm 35.5 37.6 38.4 38.8 60.0 79.2 91.5 100

OL-KK18 MS2 200-220 cm 52.0 54.4 55.3 56.5 77.7 91.0 86.6 100

OL-KK19 MS1 20-200 cm 36.0 38.0 38.8 39.8 62.0 81.6 93.6 100

OL-KK19 MS2 200-235 cm 35.8 38.2 39.1 40.0 64.3 83.5 94.7 100

82

Labtium OyPL 1500Neulaniementie 570211 KUOPIOPuh: 010 653 8000Fax: 010 653 8489

Laboratorion näytetunnus : L08161711Tilausnumero : 213971Tilaajan näytetunnus : OL-KK17 30-46 cmTilaaja : Posiva Oy Susanna Lindgren

16.3.2009

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Näytteestä poistettu >6 mm aines.

667C Humuspitoisuuden määritys spektrofotometrisesti (%) 0.61650G Karkean fraktion määritys ja poisto (%) 2.44651 Pesuseulonta OK

Sedigraph-analyysi (658)Kuivaseulonta seulasarjalla ISO 3310/1 (652)

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Savi Hiesu Hieta Hiekka Sora Kiviä

D (mm) % D (mm) % D (mm) % D (mm) % D (mm) %20.0000 100.0 0.0630 6.9 0.0200 4.5 0.0020 1.86.3000 100.0 0.0600 6.7 0.0160 4.2 0.0010 1.42.0000 86.1 0.0500 6.5 0.0100 3.5 0.0006 1.20.6300 57.7 0.0400 6.1 0.0060 2.90.2000 33.2 0.0300 5.4 0.0040 2.6

83


Laboratorion näytetunnus : L08161710Tilausnumero : 213971Tilaajan näytetunnus : OL-KK17 46-(82) cmTilaaja : Posiva Oy Susanna Lindgren

16.3.2009

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650G Karkean fraktion määritys ja poisto (%) 21.63651 Pesuseulonta OK


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Summary of the Overburden Studies of the Soil Pits OL-KK14 ... · Summary of the overburden studies...

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