# Ranges of B, Cd, Cr, Cu, Fe, Pb, Sr, Tl, and Zn Concentrations and Isotope Ratios in Environmental Matrices from an Urban Area

Authors: Nicola Pallavicini; Emma Engström; Douglas C. Baxter; Björn Öhlander; Johan Ingri; Scott Hawley; Catherine Hirst; Katerina Rodushkina; Ilia Rodushkin
Journal: Journal of Spectroscopy
 (2018)

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## Abstract

Isotopic information may provide powerful insight into the elemental cycling processes which occur in natural compartments. Further implementation of isotopic techniques in natural sciences requires a better understanding of the range of elemental and isotopic compositional variability in environmental matrices. This study assesses the local-scale concentration and isotopic composition variability of nine elements: boron (B), cadmium (Cd), chromium (Cr), copper (Cu), iron (Fe), lead (Pb), strontium (Sr), thallium (Tl), and zinc (Zn) in lysimetric waters, mushrooms, litter, needles, leaves, and lichens. Sequential extractions were also performed on soil samples from 6 depth profiles providing more detailed information on the variability of elemental concentrations and isotope ratios between the elemental pools present in soil. For most of the sample types studied the range of isotopic variability between samples spans almost the entire ranges reported in the literature for natural samples. These results represent a starting point for discussing the role of natural variability in isotopic studies (for example, as a limiting factor in the use of isotopic mixing models) and a baseline for future in-depth studies examining the controls on isotope fraction in natural systems.


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## Body

## 1. Introduction

The development of isotope-based techniques in environmental science has grown exponentially in the last few decades [1–6]. Recent studies in the field are increasingly adopting multielemental approaches to determine sample provenance [7–9], fingerprint pollution sources [10–14] and identify biochemical processes [15, 16]. Ultimately, the usefulness of all such single and multielemental isotope methods in biological and environmental sciences is limited by the uncertainties of interpreting the isotope ratio data [17].Historically, analytical (im)precision was a significant barrier to unambiguous data interpretation for stable [18, 19] and even radiogenic isotopic systems [20]. The advent and continued development of multiple collector inductively coupled plasma mass spectrometry (MC-ICP-MS) has greatly improved analytic precision attainable. Nowadays, the ability to unambiguously interpret high-quality MC-ICP-MS data is increasingly limited by a lack of data on the isotopic variability of environmental samples, i.e., is the identified difference in isotopic compositions between two samples within a range to be expected for the sample type given natural variability or not?The severity of the issue was highlighted in a previous study whereof the total concentrations and isotope ratios of a number of elements in leaves, needles, and mushrooms from northern Sweden were determined [2]. Even after removing some known sources of variation such as sampling height (for leaves and needles) and sampling period, very broad ranges in isotopic compositions of many elements were found across samples collected over a confined geographic area. The variability was attributed to a combination of differences in accumulation pathways, soil type, subsoil geology, proximity to local contamination sources, sampling period, and weather preceding sampling occasion [21–23]. Given such a large number of confounding factors may contribute to the isotopic composition of environments samples, it was concluded that while foliage samples may provide highly spatially and temporally resolved snapshots of elemental and isotopic interactions, a better understanding of the individual variables within the system is needed to understand the observed isotopic variability in bioindicators.Therefore, the aim of this work is to build on the previous work [2] and extend a comprehensive dataset of concentrations and isotopic compositions to nine elements in a variety of environmental samples (topsoil, lysimetric waters, mushrooms, litter, wood ash, needles, leaves, and lichens). As the fate and behaviour of an element in soil is dependent on the physical/chemical form of that element in soils, i.e., dissolved, exchangeable, included in the mineral lattice, or insoluble [24], distinguishing the subpools is an important complement to bulk concentration and isotope ratio measurements. The sequential extraction procedure (SEP) used by this study allowed the determination of 6 functionally defined elemental pools from 6 soil profiles from urban and suburban locations.The elements measured in this study are currently broadly used across many environmental fields (disciplines) to study a wide range of processes. Several of the elements (Zn, Fe, Cu, and B) are essential for plant growth and can be important cofactors in other biological processes. Moreover, the elements included in the study can be of environmental concern (Cd, Pb, Cr, Cu, Zn, and Tl) and/or are commonly used tracers in provenance studies (Sr, B, and Pb). Overall, both radiogenic (Sr and Pb) and stable isotopic systems (B, Cd, Cr, Cu, Fe, Sr, Tl, and Zn) are included and a single multielement/multi-isotopic analytical procedure [2] can be used to measure them all.The local-scale variability in isotopic composition was compared with the published assessments of global isotopic variability. For elements like Tl, where there is limited published data on the isotopic compositions of environmental samples, the information thus obtained aids gaining knowledge needed for better understanding of Tl systematics. For other elements, such as Fe, the information offers a framework for considering the relationship between carefully controlled fractionation experiments and real-world samples. In order to illustrate the significance of such variability assessments, a case study is presented using multi-isotope data for two landfills contaminated by tailings from Fe production, Fe and Cu slag, and fly ash.


## 2. Materials and Methods

### 2.1. Study Site

All samples in this project were collected in and around the city of Luleå, a medium-sized town situated in northern Sweden in the province of Norrbotten (Figure1). The original village of Luleå dates back to 1649 [25] and has more recently become industrialized including a major steelworks. Samples collected within approximately 5 km direct distance from local steelworks and harbours will, for the remainder of this study, be referred to as “city” samples. Samples from a broader area, approximately 10 km from the major local industries, are referred to as “suburb” samples. The suburban locality was relatively recently a seabed (the study area, as well as entire northern part of the Nordic region is rising due to postglacial up-lift almost 9 mm a year, due to isostatic glacial readjustment [26]) and has been involved in the urbanization process only from the late 1980s.Figure 1
Map of the sampling locations. Filled circles represent the sampling point where biological samples have been collected (leaves, needles, and mushrooms); filled stars represent the locations where soil samples have been collected.The local soil consists mainly of clay and silt loam overlying 1.9 Ga granitic bedrock with minor metasedimentary constituents. The suburban location is specifically characterized by a rather homogeneous sandy and well sorted soil with little variations in grain size. The sampling locations in the urban (city) area are till soils characterized by coarse and heterogeneous grain sizes which were formed at the time the land emerged from a sea some 400 years ago.


### 2.2. Sample Collection and Preparation

The sampling procedures for bioindicator organisms (mushrooms,n > 60; one pooled litter sample; leaves, n > 200; needles, n > 40; lichens, n > 30) are reported in Pallavicini et al. [21] and in Rodushkin et al. [2]. Wood ash (originated mainly from local birch wood) was collected from several dedicated recreational fireplaces in Luleå vicinity and pooled into a single sample. Individual soil samples were collected at the end of July 2015 following the same scheme (n > 150, approximately 10 g of soil from upper, predominantly organic, 2-3 cm layer sampled by acid-washed plastic spoon). To supplement the individual soils, samples six soil profiles, two from the city centre and four from the suburban area hereafter referred to as “city” and “suburb” respectively, were also collected. The profiles were collected using a vertical soil core sampler to a maximum sampling depth of 60 cm (consistent with typical rooting depth for tree species sampled [27]. Once collected, each soil core was divided into four equal 15 cm horizontal subsamples and stored in 50 mL polypropylene screw-capped tubes. The soil subsamples does not directly correspond to different soil horizons. In order to compliment the soil samples, pore-water solutions (approximately 250 mL) were collected from nine locations in the town using drain-gauge passive-capillary lysimeters (n = 15) installed at 20 cm depth. Two heavily contaminated soil samples (landfills) from the same region were also added to this study.Details on sample preparation procedure including chemicals and reagents used, sample digestion and sequential extraction procedure (SEP), analyte/matrix separation, element concentration, and isotopic analyses are fully reported in the ESI. The SEP followed a method involving six extractions [28] and has been summarized in Table 1.Table 1
Sequential extraction scheme.
Code
Extracted phase
Solution
Volume (mL)
F1
Exchangeable
Distilled water
40
F2
Carbonates
0.11 M·CH3COOH (acetic acid)
40
F3
Reducible
0.1 M·NH2OH·HCl (hydroxylamine hydrochloride)
40
F4
Oxidizable
8.8 M·H2O2 (hydrogen peroxide)
10 + 10
1 M·CH3COONH4 (ammonium acetate) pH 2
50
F5
Residual I
Aqua regia
20
F6
Residual II
HF
10


### 2.3. Analytic Performance

Information on operating parameters and measurement conditions for MC-ICP-MS can be found in Table2 (see ESI for more detailed description). All stable isotopic systems are reported in standard delta (δ) notation while radiogenic systems are reported as ratios in accordance with standard practices. Stable isotopic differences between samples are reported as capital delta (Δ) notation denoting the difference between two δ values.Table 2
MC-ICP-MS operating parameters and measurement conditions for isotope ratio measurementsb. Table modified from Rodushkin et al. [2].
Elementsa
Configuration of introduction system
Resolution mode
Integration time (s)
Sample uptake rate (mL·min−1)
Dynamic mode configuration
Cup configuration
“δ-zero” reference standards
Reported ratios
L4
L3
L2
L1
C
H1
H2
H3
H4
B
Pumped micromist nebulizer, minicyclonic spray chamber, X-type skimmer cone
Low
0.524
0.40–0.50
—
—
10B
—
—
—
11B
—
—
NIST SRM 951a boric acid
δ
11B
Cd
Aridus/Apex desolvating systems, self-aspirating microconcentric PFA nebulizer, X-type skimmer cone
Low
0.524
0.04–0.06
107Ag
108Cd
109Ag
110Cd
111Cd
112Cd
114Cd
116Cd
117Sn
NIST SRM 3108 Cd solution Lot 130116
δ
114Cd
108Pd
110Pd
112Sn
114Sn
116Sn
Zn/Cu
Pumped micromist nebulizer, double spray chamber, H-type skimmer cone
Medium
0.262
0.20–0.25
—
63Cu
64Zn
65Cu
66Zn
67Zn
68Zn
70Zn
—
NIST SRM 976 Cu standard solution
δ
56Cu
(64Ni)
IRMM-3702 Zn solution
δ
66Zn
Cr/Ni
Pumped micromist nebulizer, double spray chamber, H-type skimmer cone/Apex desolvating systems, self-aspirating microconcentric PFA nebulizer, X-type skimmer cone
High
1.262
0.05–0.25
Main
—
52Cr
53Cr
54Cr
—
56Fe
—
—
—
NBS SRM 979 Cr standard
δ
53Cr
54Fe
Sub configuration
—
—
—
—
—
60Ni
61Ni
62Ni
—
Fe/Ni
Pumped micromist nebulizer, double spray chamber, H-type skimmer cone
Medium
0.262
0.20–0.25
54Fe
—
56Fe
57Fe
—
60Ni
61Ni
62Ni
—
IRMM-014 Fe metal
δ
56Fe
54Cr
Pb/Tl
Aridus/Apex desolvating systems, self-aspirating microconcentric PFA nebulizer, X-type skimmer cone
Low
0.524
0.04–0.06
—
202Hg
203Tl
204Pb
205Tl
206Pb
207Pb
208Pb
—
NIST SRM 981 common Pb
206Pb/207Pb;208Pb/207Pb
Tl: 1000 mg·L−1 elemental standard. Ultra scientific, North Kingstown, RI, USA; Lot L00709
δ
205Tl
204Hg
Sr
Pumped micromist  nebulizer, double spray chamber, H-type skimmer cone
Low
0.262
0.20–0.25
82Kr
83Kr
84Sr
85Rb
86Sr
87Sr
88Sr
—
—
Sr carbonate NIST SRM 987 (NBS-987) Sr carbonate
87Sr/86Sr
84Kr
86Kr
87Rb
aOne element is used as the internal standard for the second element, except for Ni and Ag which were only used as the internal standards. bRF power: 1400–1450 W. Coolant gas flow: 15 L·min−1. Auxiliary gas flow: 1.4·L min−1. Sample gas flow: 0.9–1.25 L·min−1. Additional gas flow (N2, Aridus and Apex) 0.01–0.02 L·min−1. Ion lens settings: adjusted daily to obtain maximum sensitivity and signal stability. Zoom optic settings: adjusted daily to obtain maximum resolution. Number of blocks: 9. Number of cycles per block: 5. Number of integrations: 3–5. Amplifier rotation: left.All solutions were analyzed in duplicate. Signal intensities were transferred to commercially available spreadsheet software for further off-line calculations, including blank, isobaric interference(s) as well as instrumental mass bias corrections. The latter was corrected by the revised exponential correction model [29] using the internal standard (for all isotopic systems but B), and the corrected ratios or δ-values were calculated against bracketing standard solutions. Results from the two measurements were used to calculate mean ratios or δ-values and in-run repeatability for each sample.For the stable isotopic systems, many of the individual isotopes were measured as possible (Table2) to validate the mass dependent nature of the measurements, but for easy of reporting, only a single δ value will be used consistently for each system (Table 2).The analytical results for reference standards (QC Loam Soil (VIK) (soil powder) (Eurofins A/S Denmark, Vallensbæk Strand, Denmark), GBW 07410 (soil) (National Research Centre of Geoanalysis, Beijing, China), and IRMM ERM-CC141 (soil powder)) along with typical repeatability and intermediate precision figures for soils, mushrooms, and leaves are reported in Table3. All reference standards were processed and analyzed in parallel with the samples. It should be noted that results for GBW 07410 and ERM-CC141 are calculated using concentrations and isotope ratios for individual sequential extraction fractions and therefore more uncertain. A full list of certified materials used to assess performance of the method for bioindicators is available in the ESI.Table 3
Concentrations and isotope information for CRMs.
Element
BCR-146R, Aqua regia
CRM052, Aqua regia
BCR-146R
CRM052
Found ±σ, µg·g−1
Certified ± 95% CI
Found ±σ, µg·g−1
Certified ± 95% CI
Found ± 2σ
Found ± 2σ
(n = 8)
(µg·g−1)
(n = 6)
(µg·g−1)
(n = 8)
n = 6
B
17.3 ± 1.6
NA
177 ± 11
NA
δ11B. ‰
−3.40 ± 1.53
7.21 ± 1.09
Cd
17.7 ± 0.4
18.4 ± 0.4
263 ± 9
256 ± 6
δ114Cd. ‰
0.11 ± 0.09
−0.01 ± 0.09
Cr
175 ± 10
174 ± 7
346 ± 19
332 ± 5
δ53Cr. ‰
0.04 ± 0.09
0.14 ± 0.07
Cu
798 ± 25
831 ± 16
130 ± 7
130 ± 3
δ65Cu. ‰
0.22 ± 0.06
0.84 ± 0.14
Fe
13600 ± 800
NA
4610 ± 320
4280 ± 208
δ56Fe. ‰
0.18 ± 0.05
0.80 ± 0.07
Pb
548 ± 43
583 ± 17
115 ± 11
108 ± 3
206Pb/207Pb
1.1496 ± 0.0002
1.2078 ± 0.0004
208Pb/207Pb
2.4288 ± 0.0003
2.4650 ± 0.0004
Sr
1070 ± 99
NA
243 ± 13
113 ± 11
87Sr/86Sr
0.70805 ± 0.00003
0.70914 ± 0.00004
Tl
0.469 ± 0.033
NA
75.5 ± 6.2
71.6 ± 2.7
δ205 Tl. ‰
−0.50 ± 0.04
−0.41 ± 0.09
Zn
3050 ± 170
3040 ± 60
512 ± 34
516 ± 12
δ66Zn. ‰
−0.12 ± 0.05
−0.18 ± 0.05
Element
GBW 07410
ERM-CC141, Aqua regia
ERM-CC141, total
Found,µg·g−1
Certified ± 95% CI
Recovery, %
Found,µg·g−1
Certified ± 95% CI
Recovery, %
Found,µg·g−1
Certified ± 95% CI
Recovery, %
B
42.1
38.3 ± 4, 8
110
NA
NA
16
NA
NA
Cd
0.117
0.086 ± 0,015
136
0.28
0.25 ± 0.04
112
0.31
0.35 ± 0.05
89
Cr
57
66 ± 4, 5
86
30
31 ± 4
97
66
86 ± 8
77
Cu
23.7
23.2 ± 2, 2
102
13
12.4 ± 0.9
105
14.4
14.4 ± 1.4
100
Fe
32200
32200
100
19800
NA
NA
24800
NA
NA
Pb
29.9
29.2 ± 3, 2
102
34.4
32.2 ± 1.4
107
42.1
41 ± 4
103
Sr
175
188 ± 9
93
12
NA
NA
68
NA
NA
Tl
0.66
0.62 ± 0, 16
106
0,14
NA
NA
0.52
NA
NA
Zn
71.7
69.1 ± 2, 7
104
52
50 ± 4
104
60
57 ± 4
105
GBW 07410
ERM-CC141
Repeatability, 2σ
Intermediate precision, 2σ
Found
Found
Mushrooms,n = 8
Leaves,n = 12
Soil,n = 10
Mushrooms,n = 16
Leaves,n = 24
Soil,n = 20
δ
11B, ‰
−6.0
4.5
3.2
0.7
1.6
5.4
1.2
2.4
δ
114Cd, ‰
−0.07
−0.11
0.022
0.032
0.074
0.041
0.072
0.116
δ
53Cr, ‰
0.11
0.06
NA
NA
0.078
NA
NA
0.107
δ
65Cu, ‰
0.34
0.28
0.074
0.078
0.052
0.097
0.086
0.073
δ
56Fe, ‰
0.16
0.06
0.077
0.056
0.034
0.086
0.081
0.059
208Pb/207Pb
2.4452
2.4431
0.0037
0.0053
0.0021
0.0040
0.0058
0.0024
206Pb/207Pb
1.1781
1.1913
0.0022
0.0034
0.0011
0.0028
0.0041
0.0016
87Sr/86Sr
0.7122
0.7291
0.0014
0.0001
0.0002
0.0018
0.0002
0.0002
δ
205Tl, ‰
−0.53
−0.67
0.089
0.106
0.031
0.112
0.122
0.059
δ
66Zn, ‰
0.02
0.18
0.048
0.062
0.034
0.088
0.095
0.061Though mass balances for both concentrations (%-recovery of sum of extracts) and stable isotope ratios (comparison of measured and calculated bulk sample delta values) for all soil samples subject to SEP may aid to accuracy evaluation, this would require thorough homogenization (e.g., by fine grinding) of soils before taking subsample for bulk analyses with accompanying risk of introducing contamination and affecting distribution between phases.


#### 2.3.1. Precision

The intermediate precision for concentration data, defined as the reproducibility of an analytic technique from digestion to measurements on multiple occasions by different analysts, for the reference standards BCR-146R and CRM052 is <7% for most elements (Table3). For isotopic ratios, attainable precision varies significantly between isotope systems and matrices studied. It should be stressed that intermediate precision is about two times greater than repeatability (Table 3) due to varying element concentrations, slight variations in column yield, efficiency of matrix separation and contamination during column chemistry, instrumental optimization, etc. Intermediate precision, defined in this manner, is therefore considered to provide a valid assessment of the overall method uncertainty or the analytical “resolution” of the procedure. For example, due in large part to low absolute B concentrations, B isotope ratio measurements in mushrooms have a mean uncertainty of approximately 5‰ if performed on different occasions, and natural variations in isotopic composition below this level cannot be discerned.


#### 2.3.2. Accuracy

Elemental concentrations in the aqua regia digests were within the 90%–110% range of the certified values for the CRMs except for Sr in CRM052 (Table3). Reanalysis of the digests by an alternative technique (ICP-optical emission spectrometry) confirmed the double-focusing sector field ICP-MS (ICP-SFMS) results and the reason for our high reported Sr concentrations remains unclear. The overall accuracy of the SEP was calculated by summing the elemental concentrations in all the fractions in GBW 07410 and ERM-CC141. The majority of elements were within 10% of the certified values, but Cr concentrations samples are around 80% of the certified values.The reference materials utilized in this study are not certified for isotopic composition, and, to the authors’ knowledge, there is no other published isotope data for the measured CRMs. Therefore, the accuracy of the presented isotope ratio data cannot be directly evaluated. Isotopic information for CRMs presented in Table3 can aid future interlaboratory calibrations of new reference standards for such matrices.


## 2.1. Study Site

All samples in this project were collected in and around the city of Luleå, a medium-sized town situated in northern Sweden in the province of Norrbotten (Figure1). The original village of Luleå dates back to 1649 [25] and has more recently become industrialized including a major steelworks. Samples collected within approximately 5 km direct distance from local steelworks and harbours will, for the remainder of this study, be referred to as “city” samples. Samples from a broader area, approximately 10 km from the major local industries, are referred to as “suburb” samples. The suburban locality was relatively recently a seabed (the study area, as well as entire northern part of the Nordic region is rising due to postglacial up-lift almost 9 mm a year, due to isostatic glacial readjustment [26]) and has been involved in the urbanization process only from the late 1980s.Figure 1
Map of the sampling locations. Filled circles represent the sampling point where biological samples have been collected (leaves, needles, and mushrooms); filled stars represent the locations where soil samples have been collected.The local soil consists mainly of clay and silt loam overlying 1.9 Ga granitic bedrock with minor metasedimentary constituents. The suburban location is specifically characterized by a rather homogeneous sandy and well sorted soil with little variations in grain size. The sampling locations in the urban (city) area are till soils characterized by coarse and heterogeneous grain sizes which were formed at the time the land emerged from a sea some 400 years ago.


## 2.2. Sample Collection and Preparation

The sampling procedures for bioindicator organisms (mushrooms,n > 60; one pooled litter sample; leaves, n > 200; needles, n > 40; lichens, n > 30) are reported in Pallavicini et al. [21] and in Rodushkin et al. [2]. Wood ash (originated mainly from local birch wood) was collected from several dedicated recreational fireplaces in Luleå vicinity and pooled into a single sample. Individual soil samples were collected at the end of July 2015 following the same scheme (n > 150, approximately 10 g of soil from upper, predominantly organic, 2-3 cm layer sampled by acid-washed plastic spoon). To supplement the individual soils, samples six soil profiles, two from the city centre and four from the suburban area hereafter referred to as “city” and “suburb” respectively, were also collected. The profiles were collected using a vertical soil core sampler to a maximum sampling depth of 60 cm (consistent with typical rooting depth for tree species sampled [27]. Once collected, each soil core was divided into four equal 15 cm horizontal subsamples and stored in 50 mL polypropylene screw-capped tubes. The soil subsamples does not directly correspond to different soil horizons. In order to compliment the soil samples, pore-water solutions (approximately 250 mL) were collected from nine locations in the town using drain-gauge passive-capillary lysimeters (n = 15) installed at 20 cm depth. Two heavily contaminated soil samples (landfills) from the same region were also added to this study.Details on sample preparation procedure including chemicals and reagents used, sample digestion and sequential extraction procedure (SEP), analyte/matrix separation, element concentration, and isotopic analyses are fully reported in the ESI. The SEP followed a method involving six extractions [28] and has been summarized in Table 1.Table 1
Sequential extraction scheme.
Code
Extracted phase
Solution
Volume (mL)
F1
Exchangeable
Distilled water
40
F2
Carbonates
0.11 M·CH3COOH (acetic acid)
40
F3
Reducible
0.1 M·NH2OH·HCl (hydroxylamine hydrochloride)
40
F4
Oxidizable
8.8 M·H2O2 (hydrogen peroxide)
10 + 10
1 M·CH3COONH4 (ammonium acetate) pH 2
50
F5
Residual I
Aqua regia
20
F6
Residual II
HF
10


## 2.3. Analytic Performance

Information on operating parameters and measurement conditions for MC-ICP-MS can be found in Table2 (see ESI for more detailed description). All stable isotopic systems are reported in standard delta (δ) notation while radiogenic systems are reported as ratios in accordance with standard practices. Stable isotopic differences between samples are reported as capital delta (Δ) notation denoting the difference between two δ values.Table 2
MC-ICP-MS operating parameters and measurement conditions for isotope ratio measurementsb. Table modified from Rodushkin et al. [2].
Elementsa
Configuration of introduction system
Resolution mode
Integration time (s)
Sample uptake rate (mL·min−1)
Dynamic mode configuration
Cup configuration
“δ-zero” reference standards
Reported ratios
L4
L3
L2
L1
C
H1
H2
H3
H4
B
Pumped micromist nebulizer, minicyclonic spray chamber, X-type skimmer cone
Low
0.524
0.40–0.50
—
—
10B
—
—
—
11B
—
—
NIST SRM 951a boric acid
δ
11B
Cd
Aridus/Apex desolvating systems, self-aspirating microconcentric PFA nebulizer, X-type skimmer cone
Low
0.524
0.04–0.06
107Ag
108Cd
109Ag
110Cd
111Cd
112Cd
114Cd
116Cd
117Sn
NIST SRM 3108 Cd solution Lot 130116
δ
114Cd
108Pd
110Pd
112Sn
114Sn
116Sn
Zn/Cu
Pumped micromist nebulizer, double spray chamber, H-type skimmer cone
Medium
0.262
0.20–0.25
—
63Cu
64Zn
65Cu
66Zn
67Zn
68Zn
70Zn
—
NIST SRM 976 Cu standard solution
δ
56Cu
(64Ni)
IRMM-3702 Zn solution
δ
66Zn
Cr/Ni
Pumped micromist nebulizer, double spray chamber, H-type skimmer cone/Apex desolvating systems, self-aspirating microconcentric PFA nebulizer, X-type skimmer cone
High
1.262
0.05–0.25
Main
—
52Cr
53Cr
54Cr
—
56Fe
—
—
—
NBS SRM 979 Cr standard
δ
53Cr
54Fe
Sub configuration
—
—
—
—
—
60Ni
61Ni
62Ni
—
Fe/Ni
Pumped micromist nebulizer, double spray chamber, H-type skimmer cone
Medium
0.262
0.20–0.25
54Fe
—
56Fe
57Fe
—
60Ni
61Ni
62Ni
—
IRMM-014 Fe metal
δ
56Fe
54Cr
Pb/Tl
Aridus/Apex desolvating systems, self-aspirating microconcentric PFA nebulizer, X-type skimmer cone
Low
0.524
0.04–0.06
—
202Hg
203Tl
204Pb
205Tl
206Pb
207Pb
208Pb
—
NIST SRM 981 common Pb
206Pb/207Pb;208Pb/207Pb
Tl: 1000 mg·L−1 elemental standard. Ultra scientific, North Kingstown, RI, USA; Lot L00709
δ
205Tl
204Hg
Sr
Pumped micromist  nebulizer, double spray chamber, H-type skimmer cone
Low
0.262
0.20–0.25
82Kr
83Kr
84Sr
85Rb
86Sr
87Sr
88Sr
—
—
Sr carbonate NIST SRM 987 (NBS-987) Sr carbonate
87Sr/86Sr
84Kr
86Kr
87Rb
aOne element is used as the internal standard for the second element, except for Ni and Ag which were only used as the internal standards. bRF power: 1400–1450 W. Coolant gas flow: 15 L·min−1. Auxiliary gas flow: 1.4·L min−1. Sample gas flow: 0.9–1.25 L·min−1. Additional gas flow (N2, Aridus and Apex) 0.01–0.02 L·min−1. Ion lens settings: adjusted daily to obtain maximum sensitivity and signal stability. Zoom optic settings: adjusted daily to obtain maximum resolution. Number of blocks: 9. Number of cycles per block: 5. Number of integrations: 3–5. Amplifier rotation: left.All solutions were analyzed in duplicate. Signal intensities were transferred to commercially available spreadsheet software for further off-line calculations, including blank, isobaric interference(s) as well as instrumental mass bias corrections. The latter was corrected by the revised exponential correction model [29] using the internal standard (for all isotopic systems but B), and the corrected ratios or δ-values were calculated against bracketing standard solutions. Results from the two measurements were used to calculate mean ratios or δ-values and in-run repeatability for each sample.For the stable isotopic systems, many of the individual isotopes were measured as possible (Table2) to validate the mass dependent nature of the measurements, but for easy of reporting, only a single δ value will be used consistently for each system (Table 2).The analytical results for reference standards (QC Loam Soil (VIK) (soil powder) (Eurofins A/S Denmark, Vallensbæk Strand, Denmark), GBW 07410 (soil) (National Research Centre of Geoanalysis, Beijing, China), and IRMM ERM-CC141 (soil powder)) along with typical repeatability and intermediate precision figures for soils, mushrooms, and leaves are reported in Table3. All reference standards were processed and analyzed in parallel with the samples. It should be noted that results for GBW 07410 and ERM-CC141 are calculated using concentrations and isotope ratios for individual sequential extraction fractions and therefore more uncertain. A full list of certified materials used to assess performance of the method for bioindicators is available in the ESI.Table 3
Concentrations and isotope information for CRMs.
Element
BCR-146R, Aqua regia
CRM052, Aqua regia
BCR-146R
CRM052
Found ±σ, µg·g−1
Certified ± 95% CI
Found ±σ, µg·g−1
Certified ± 95% CI
Found ± 2σ
Found ± 2σ
(n = 8)
(µg·g−1)
(n = 6)
(µg·g−1)
(n = 8)
n = 6
B
17.3 ± 1.6
NA
177 ± 11
NA
δ11B. ‰
−3.40 ± 1.53
7.21 ± 1.09
Cd
17.7 ± 0.4
18.4 ± 0.4
263 ± 9
256 ± 6
δ114Cd. ‰
0.11 ± 0.09
−0.01 ± 0.09
Cr
175 ± 10
174 ± 7
346 ± 19
332 ± 5
δ53Cr. ‰
0.04 ± 0.09
0.14 ± 0.07
Cu
798 ± 25
831 ± 16
130 ± 7
130 ± 3
δ65Cu. ‰
0.22 ± 0.06
0.84 ± 0.14
Fe
13600 ± 800
NA
4610 ± 320
4280 ± 208
δ56Fe. ‰
0.18 ± 0.05
0.80 ± 0.07
Pb
548 ± 43
583 ± 17
115 ± 11
108 ± 3
206Pb/207Pb
1.1496 ± 0.0002
1.2078 ± 0.0004
208Pb/207Pb
2.4288 ± 0.0003
2.4650 ± 0.0004
Sr
1070 ± 99
NA
243 ± 13
113 ± 11
87Sr/86Sr
0.70805 ± 0.00003
0.70914 ± 0.00004
Tl
0.469 ± 0.033
NA
75.5 ± 6.2
71.6 ± 2.7
δ205 Tl. ‰
−0.50 ± 0.04
−0.41 ± 0.09
Zn
3050 ± 170
3040 ± 60
512 ± 34
516 ± 12
δ66Zn. ‰
−0.12 ± 0.05
−0.18 ± 0.05
Element
GBW 07410
ERM-CC141, Aqua regia
ERM-CC141, total
Found,µg·g−1
Certified ± 95% CI
Recovery, %
Found,µg·g−1
Certified ± 95% CI
Recovery, %
Found,µg·g−1
Certified ± 95% CI
Recovery, %
B
42.1
38.3 ± 4, 8
110
NA
NA
16
NA
NA
Cd
0.117
0.086 ± 0,015
136
0.28
0.25 ± 0.04
112
0.31
0.35 ± 0.05
89
Cr
57
66 ± 4, 5
86
30
31 ± 4
97
66
86 ± 8
77
Cu
23.7
23.2 ± 2, 2
102
13
12.4 ± 0.9
105
14.4
14.4 ± 1.4
100
Fe
32200
32200
100
19800
NA
NA
24800
NA
NA
Pb
29.9
29.2 ± 3, 2
102
34.4
32.2 ± 1.4
107
42.1
41 ± 4
103
Sr
175
188 ± 9
93
12
NA
NA
68
NA
NA
Tl
0.66
0.62 ± 0, 16
106
0,14
NA
NA
0.52
NA
NA
Zn
71.7
69.1 ± 2, 7
104
52
50 ± 4
104
60
57 ± 4
105
GBW 07410
ERM-CC141
Repeatability, 2σ
Intermediate precision, 2σ
Found
Found
Mushrooms,n = 8
Leaves,n = 12
Soil,n = 10
Mushrooms,n = 16
Leaves,n = 24
Soil,n = 20
δ
11B, ‰
−6.0
4.5
3.2
0.7
1.6
5.4
1.2
2.4
δ
114Cd, ‰
−0.07
−0.11
0.022
0.032
0.074
0.041
0.072
0.116
δ
53Cr, ‰
0.11
0.06
NA
NA
0.078
NA
NA
0.107
δ
65Cu, ‰
0.34
0.28
0.074
0.078
0.052
0.097
0.086
0.073
δ
56Fe, ‰
0.16
0.06
0.077
0.056
0.034
0.086
0.081
0.059
208Pb/207Pb
2.4452
2.4431
0.0037
0.0053
0.0021
0.0040
0.0058
0.0024
206Pb/207Pb
1.1781
1.1913
0.0022
0.0034
0.0011
0.0028
0.0041
0.0016
87Sr/86Sr
0.7122
0.7291
0.0014
0.0001
0.0002
0.0018
0.0002
0.0002
δ
205Tl, ‰
−0.53
−0.67
0.089
0.106
0.031
0.112
0.122
0.059
δ
66Zn, ‰
0.02
0.18
0.048
0.062
0.034
0.088
0.095
0.061Though mass balances for both concentrations (%-recovery of sum of extracts) and stable isotope ratios (comparison of measured and calculated bulk sample delta values) for all soil samples subject to SEP may aid to accuracy evaluation, this would require thorough homogenization (e.g., by fine grinding) of soils before taking subsample for bulk analyses with accompanying risk of introducing contamination and affecting distribution between phases.


### 2.3.1. Precision

The intermediate precision for concentration data, defined as the reproducibility of an analytic technique from digestion to measurements on multiple occasions by different analysts, for the reference standards BCR-146R and CRM052 is <7% for most elements (Table3). For isotopic ratios, attainable precision varies significantly between isotope systems and matrices studied. It should be stressed that intermediate precision is about two times greater than repeatability (Table 3) due to varying element concentrations, slight variations in column yield, efficiency of matrix separation and contamination during column chemistry, instrumental optimization, etc. Intermediate precision, defined in this manner, is therefore considered to provide a valid assessment of the overall method uncertainty or the analytical “resolution” of the procedure. For example, due in large part to low absolute B concentrations, B isotope ratio measurements in mushrooms have a mean uncertainty of approximately 5‰ if performed on different occasions, and natural variations in isotopic composition below this level cannot be discerned.


### 2.3.2. Accuracy

Elemental concentrations in the aqua regia digests were within the 90%–110% range of the certified values for the CRMs except for Sr in CRM052 (Table3). Reanalysis of the digests by an alternative technique (ICP-optical emission spectrometry) confirmed the double-focusing sector field ICP-MS (ICP-SFMS) results and the reason for our high reported Sr concentrations remains unclear. The overall accuracy of the SEP was calculated by summing the elemental concentrations in all the fractions in GBW 07410 and ERM-CC141. The majority of elements were within 10% of the certified values, but Cr concentrations samples are around 80% of the certified values.The reference materials utilized in this study are not certified for isotopic composition, and, to the authors’ knowledge, there is no other published isotope data for the measured CRMs. Therefore, the accuracy of the presented isotope ratio data cannot be directly evaluated. Isotopic information for CRMs presented in Table3 can aid future interlaboratory calibrations of new reference standards for such matrices.


## 2.3.1. Precision

The intermediate precision for concentration data, defined as the reproducibility of an analytic technique from digestion to measurements on multiple occasions by different analysts, for the reference standards BCR-146R and CRM052 is <7% for most elements (Table3). For isotopic ratios, attainable precision varies significantly between isotope systems and matrices studied. It should be stressed that intermediate precision is about two times greater than repeatability (Table 3) due to varying element concentrations, slight variations in column yield, efficiency of matrix separation and contamination during column chemistry, instrumental optimization, etc. Intermediate precision, defined in this manner, is therefore considered to provide a valid assessment of the overall method uncertainty or the analytical “resolution” of the procedure. For example, due in large part to low absolute B concentrations, B isotope ratio measurements in mushrooms have a mean uncertainty of approximately 5‰ if performed on different occasions, and natural variations in isotopic composition below this level cannot be discerned.


## 2.3.2. Accuracy

Elemental concentrations in the aqua regia digests were within the 90%–110% range of the certified values for the CRMs except for Sr in CRM052 (Table3). Reanalysis of the digests by an alternative technique (ICP-optical emission spectrometry) confirmed the double-focusing sector field ICP-MS (ICP-SFMS) results and the reason for our high reported Sr concentrations remains unclear. The overall accuracy of the SEP was calculated by summing the elemental concentrations in all the fractions in GBW 07410 and ERM-CC141. The majority of elements were within 10% of the certified values, but Cr concentrations samples are around 80% of the certified values.The reference materials utilized in this study are not certified for isotopic composition, and, to the authors’ knowledge, there is no other published isotope data for the measured CRMs. Therefore, the accuracy of the presented isotope ratio data cannot be directly evaluated. Isotopic information for CRMs presented in Table3 can aid future interlaboratory calibrations of new reference standards for such matrices.


## 3. Results and Discussion

### 3.1. Element Concentrations and Isotope Ratios in Environmental Samples

Isotopic composition and concentration data for each element studied is presented in Tables4–12. The tables are formatted to show the soil profile information for all six SEP fractions in the city and suburb locations (with the reported concentrations representing an average of the individual profiles). For some analytes, only pooled isotopic ratio data is available (F1 + F2 + F3 and F4 + F5 + F6) due to there being insufficient concentrations in the single extractions to make the isotopic measurements. Concentration and isotopic ratio data for the top soils, lysimetric waters, mushrooms, needles, leaves, lichens, and litter sample are reported, for comparison, below the profile data.Table 4
Boron concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
11B, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.57
0.24
0.48
1.05
1.71
3.87
7.91
2
−9
−17
−12
−12
−7
−9
16–30 cm
0.21
0.16
0.15
0.35
0.62
2.88
4.38
−3
−11
−16
−13
−10
−19
−16
31–45 cm
0.04
0.11
0.04
0.09
0.38
1.90
2.56
−9
−11
−10
−15
−16
−24
−22
46–60 cm
0.04
0.15
0.02
0.06
0.34
1.86
2.47
−4
−6
−7
−15
−12
−23
−21
Suburb (n = 4)
0–15 cm
0.16
0.06
0.10
0.17
0.83
5.15
6.47
−25
−24
−17
−2
−17
−14
−14
16–30 cm
0.11
0.06
0.06
0.10
0.60
5.01
5.94
−7
−13
−8
−11
−15
−2
−4
31–45 cm
0.06
0.11
0.04
0.07
0.80
5.10
6.17
−10
−4
−2
10
−6
−4
−4
46–60 cm
0.05
0.09
0.04
0.05
0.58
4.75
5.56
−6
−2
−5
12
−14
−8
−9
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
11B, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
8
7
7
2
53
−7
−8
7
−17
12
29
Lysimetric waters
10
7
12
5
54
4
4
3
−2
7
9
Mushroom
1.3
0.6
1.5
0.2
6.8
−8
−10
13
−24
3
27
Litter
21
NA
NA
NA
NA
8
NA
NA
NA
NA
NA
Wood ash
290
NA
NA
NA
NA
7
NA
NA
NA
NA
NA
Needles
14
13
6
6
31
17
19
9
−2
38
40
Leaves
21
18
13
7
76
10
10
9
−7
34
41
Lichens
2.7
2.4
1.1
1.6
6.6
32
37
9
13
40
27Table 5
Cadmium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
114Cd, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.006
0.016
0.427
0.149
0.122
0.036
0.756
0.08
0.04
0.08
−0.19
−0.19
—
−0.02
16–30 cm
0.003
0.012
0.137
0.056
0.049
0.032
0.289
0.17
0.40
0.09
−0.69
−0.31
—
−0.10
31–45 cm
0.001
0.012
0.019
0.015
0.016
0.019
0.081
0.25
0.26
−0.02
−0.91
−0.24
—
−0.15
46–60 cm
0.001
0.016
0.005
0.010
0.015
0.017
0.065
0.26
0.33
−0.06
0.00
−0.91
—
−0.09
Suburb (n = 4)
0–15 cm
0.002
0.010
0.027
0.010
0.013
0.012
0.074
0.23
—
—
—
—
—
16–30 cm
0.001
0.027
0.012
0.008
0.009
0.011
0.069
—
—
—
—
—
—
31–45 cm
0.001
0.026
0.008
0.005
0.010
0.010
0.061
—
—
—
—
—
—
46–60 cm
0.001
0.025
0.003
0.006
0.009
0.012
0.056
0.19
—
—
—
—
—
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
114Cd, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
0.66
0.51
0.32
0.13
2.40
0.08
0.09
0.14
−0.32
0.42
0.74
Lysimetric waters
0.04
0.03
0.05
0.01
0.22
0.22
0.19
0.07
0.14
0.34
0.20
Mushroom
1.6
1.2
1.4
0.03
5.0
0.15
0.23
0.28
−0.71
0.52
1.23
Litter
0.30
NA
NA
NA
NA
0.17
NA
NA
NA
NA
NA
Wood ash
3.3
NA
NA
NA
NA
−0.33
NA
NA
NA
NA
NA
Needles
0.06
0.04
0.04
0.01
0.16
0.09
0.10
0.26
−0.52
0.56
1.08
Leaves
0.33
0.29
0.16
0.06
0.83
0.46
0.48
0.29
−0.60
1.31
1.91
Lichens
0.13
0.12
0.03
0.09
0.18
0.08
0.07
0.03
0.05
0.18
0.13Table 6
Chromium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
53Cr, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.09
0.18
0.14
7.5
7.7
9.5
25
−0.16
−0.11
0.38
0.04
0.04
0.11
0.04
16–30 cm
0.09
0.10
0.12
4.3
11
11
27
−0.13
−0.12
0.37
0.02
0.03
0.09
0.03
31–45 cm
0.09
0.03
0.06
2.8
11
8.8
23
0.05
0.10
0.21
0.04
0.02
0.11
0.04
46–60 cm
0.04
0.04
0.05
1.7
15
9.2
26
0.01
0.12
0.28
0.11
0.01
0.12
0.04
Suburb
a (n = 4)
0–15 cm
0.08
0.13
0.13
2.4
8.5
11
22
0.22
—
—
0.11
—
—
0.11
16–30 cm
0.09
0.06
0.13
2.0
5.8
10
18
—
—
—
—
—
—
—
31–45 cm
0.08
0.04
0.14
2.0
8.6
10
21
—
—
—
—
—
—
—
46–60 cm
0.10
0.02
0.16
1.9
7.8
9.0
19
0.16
—
—
0.12
—
—
0.12
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
53Cr, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
21
18
16
4
68
0.10
0.07
0.143
−0.16
0.41
0.57
Lysimetric waters
4.3
4.4
0.4
3.9
5.1
0.26
0.26
0.01
0.25
0.27
0.02
Mushroom
0.12
0.10
0.12
0.01
0.63
NA
NA
NA
NA
NA
NA
Litter
1.8
NA
NA
NA
NA
NA
NA
NA
NA
NA
NA
Wood ash
70
NA
NA
NA
NA
0.12
NA
NA
NA
NA
NA
Needles
0.23
0.21
0.19
0.05
0.97
NA
NA
NA
NA
NA
NA
Leaves
0.26
0.22
0.15
0.10
0.95
NA
NA
NA
NA
NA
NA
Lichens
2.2
1.6
1.1
1.5
4.2
0.36
0.36
0.11
0.21
0.57
0.36
aValues reported as empty entries are due to pooling of several fractions. The isotopic values reported for the outmost top and bottom layers for F1 and F4 correspond to averaged values of respectively soil profiles F1+F2+F3 and F4+F5+F6 fractions.Table 7
Copper concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
65Cu, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.33
0.58
0.08
26
11
1.2
39
0.10
0.05
0.38
0.23
0.29
0.06
0.26
16–30 cm
0.18
0.21
0.06
9.4
5.7
0.46
16
0.28
0.30
0.11
0.40
0.22
−0.23
0.31
31–45 cm
0.16
0.11
0.03
3.1
3.5
0.31
7.2
0.15
0.30
0.92
0.16
0.25
0.51
0.26
46–60 cm
0.14
0.15
0.05
2.0
3.9
0.34
6.6
0.27
0.41
1.04
0.68
0.22
−0.47
0.33
Suburb (n = 4)
0–15 cm
0.13
0.50
0.06
2.1
3.0
0.58
6.4
0.35
—
—
−0.14
—
—
−0.06
16–30 cm
0.12
0.17
0.06
1.9
2.1
0.37
4.8
—
—
—
—
—
—
—
31–45 cm
0.09
0.07
0.07
1.5
2.6
0.58
4.9
—
—
—
—
—
—
—
46–60 cm
0.08
0.05
0.06
1.2
2.0
0.39
3.8
0.06
—
—
−0.11
—
—
−0.10
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
65Cu, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
15
11
11
3
84
0.06
0.01
0.21
−0.51
0.51
1.02
Lysimetric waters
0.6
0.5
0.2
0.4
1.1
0.76
0.72
0.17
0.64
0.99
0.35
Mushroom
44
39
25
10
120
−0.56
0.74
−2.4
0.62
3.02
Litter
7
NA
NA
NA
NA
−0.08
NA
NA
NA
NA
NA
Wood ash
180
NA
NA
NA
NA
−1.00
NA
NA
NA
NA
NA
Needles
3.2
3.0
0.9
2.1
5.2
−1.09
−1.15
0.58
−2.0
0.05
2.08
Leaves
7.1
5.3
3.4
3
17
−0.35
−0.33
0.35
−1.34
0.83
2.15
Lichens
4.6
4.5
1.0
3.1
7.1
0.05
0.05
0.20
−0.28
0.30
0.58Table 8
Iron concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg g−1 DW
δ
56Fe, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
26
110
420
2700
16000
6800
26000
0.21
0.21
−2.0
0.33
0.22
0.17
0.19
16–30 cm
48
31
290
2100
14000
6000
22000
0.10
0.24
−1.8
0.36
0.20
0.16
0.18
31–45 cm
75
15
200
740
12000
5300
18000
0.07
−0.67
−1.3
0.88
0.18
0.15
0.17
46–60 cm
39
17
160
330
14000
6000
21000
0.07
−1.4
−1.1
0.75
0.19
0.11
0.16
Suburb (n = 4)
0–15 cm
45
66
560
530
7000
6100
14000
−0.87
—
—
0.09
—
—
0.04
16–30 cm
73
33
620
780
5800
5100
13000
—
—
—
—
—
—
—
31–45 cm
54
10
630
550
7400
5500
14000
—
—
—
—
—
—
—
46–60 cm
54
7
580
460
7000
5400
13000
−0.49
—
—
0.20
—
—
0.16
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
56Fe, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
19000
17000
9000
4100
72000
0.07
0.10
0.13
−0.33
0.45
0.78
Lysimetric waters
5200
5400
900
3600
5900
0.19
0.15
0.43
−0.20
0.91
1.11
Mushroom
130
40
330
17
2100
−0.48
−0.47
0.35
−1.16
0.26
1.42
Litter
1180
NA
NA
NA
NA
0.07
NA
NA
NA
NA
NA
Wood ash
3500
NA
NA
NA
NA
0.67
NA
NA
NA
NA
NA
Needles
140
110
110
33
440
−0.41
−0.35
0.41
−1.4
0.05
1.45
Leaves
200
160
150
61
1500
−0.29
−0.26
0.20
−0.84
0.09
0.93
Lichens
250
210
110
150
500
−0.09
−0.09
0.04
−0.14
−0.02
0.12Table 9
Lead concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,μg·g−1 DW
206Pb/207Pb/208Pb/207Pb
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.31
0.02
3.2
52
30
5.9
91
1.14/2.37
1.16/2.41
1.15/2.39
1.15/2.42
1.17/2.43
1.10/2.34
1.15/2.41
16–30 cm
0.17
0.02
0.75
9.4
18
6.6
35
1.17/2.43
1.20/2.43
1.16/2.43
1.17/2.43
1.20/2.44
1.09/2.33
1.17/2.41
31–45 cm
0.08
0.02
0.27
1.3
7.7
4.3
14
1.28/2.50
1.23/2.46
1.22/2.49
1.28/2.51
1.35/2.49
1.13/2.34
1.27/2.44
46–60 cm
0.02
0.03
0.08
0.15
4.3
4.9
9.4
1.42/2.61
1.35/2.54
1.42/2.60
1.42/2.58
1.54/2.62
1.13/2.34
1.32/2.47
Suburb (n = 4)
0–15 cm
0.04
0.04
0.54
1.2
5.9
5.9
14
1.32/2.57
1.35/2.58
1.29/2.54
1.32/2.56
1.38/2.55
1.08/2.32
1.24/2.44
16–30 cm
0.04
0.08
0.34
0.26
4.6
5.5
11
1.30/2.55
1.25/2.53
1.26/2.48
1.30/2.51
1.37/2.55
1.08/2.32
1.22/2.43
31–45 cm
0.04
0.08
0.19
0.52
4.2
6.8
12
1.33/2.56
1.23/2.50
1.29/2.52
1.38/2.64
1.42/2.58
1.08/2.32
1.21/2.42
46–60 cm
0.02
0.07
0.07
0.05
3.2
7.4
11
1.44/2.64
1.22/2.50
1.46/2.61
1.54/2.69
1.55/2.64
1.08/2.32
1.21/2.41
Concentration,µg·g−1 DW (µg·L−1 for waters)
206Pb/207Pb/208Pb/207Pb
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
18
16
21
5
470
1.35/2.49
1.34/2.50
0.15/0.01
1.05/2.30
1.77/2.61
0.72/0.31
Lysimetric waters
0.50
0.40
0.40
0.03
1.1
1.17/2.45
1.17/2.44
0.03/0.02
1.10/2.42
1.20/2.47
0.10/0.05
Mushroom
0.17
0.11
0.14
0.01
0.51
1.18/2.45
1.17/2.45
0.04/0.03
1.10/2.41
1.30/2.56
0.20/0.15
Wood ash
6.4
NA
NA
NA
NA
1.15/2.40
NA
NA
NA
NA
NA
Litter
2.3
NA
NA
NA
NA
1.16/2.42
NA
NA
NA
NA
NA
Needles
0.15
0.12
0.11
0.02
0.54
1.18/2.42
1.18/2.42
0.03/0.03
1.11/2.34
1.26/2.47
0.15/0.21
Leaves
0.29
0.21
0.29
0.04
2.1
1.18/2.44
1.18/2.43
0.03/0.02
1.11/2.39
1.25/2.49
0.14/0.10
Lichens
1.9
1.8
0.4
1.3
2.6
1.14/2.38
1.14/2.38
0.01/0.01
1.14/2.37
1.15/2.40
0.01/0.03Table 10
Strontium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
87Sr/86Sr
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.5
2.3
11
5.4
6.4
141
167
0.730
0.734
0.734
0.733
0.732
0.727
0.727
16–30 cm
0.3
1.7
5.1
3.0
6.0
138
154
0.727
0.734
0.733
0.735
0.733
0.731
0.732
31–45 cm
0.1
1.2
1.0
0.70
7.0
161
171
0.724
0.734
0.728
0.726
0.735
0.727
0.727
46–60 cm
0.1
1.2
0.60
0.50
7.7
170
180
0.727
0.743
0.724
0.727
0.747
0.727
0.728
Suburb (n = 4)
0–15 cm
0.3
0.6
1.2
0.62
6.5
146
146
0.727
—
—
0.732
—
—
0.732
16–30 cm
0.2
1.1
0.69
0.42
4.8
148
148
—
—
—
—
—
—
—
31–45 cm
0.1
1.5
0.41
0.33
6.0
179
179
—
—
—
—
—
—
—
46–60 cm
0.1
1.4
0.32
0.31
5.1
188
188
0.729
—
—
0.733
—
—
0.733
Concentration,µg·g−1 DW (µg·L−1 for waters)
87Sr/86Sr
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
25
23
15
3
150
0.731
0.731
0.004
0.723
0.739
0.016
Lysimetric waters
12
10
2
8
12
0.733
0.733
0.001
0.732
0.733
0.010
Mushroom
0.5
0.3
0.2
0.1
1.8
0.729
0.727
0.006
0.721
0.750
0.039
Litter
28
NA
NA
NA
NA
0.731
NA
NA
NA
NA
NA
Wood ash
950
NA
NA
NA
NA
0.732
NA
NA
NA
NA
NA
Needles
18
15
16
2
63
0.734
0.733
0.007
0.724
0.754
0.030
Leaves
34
31
16
6
120
0.730
0.730
0.005
0.721
0.742
0.024
Lichens
8.3
7.4
3.9
2.5
16
0.733
0.731
0.006
0.725
0.742
0.017Table 11
Thallium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
205 Tl, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.004
0.002
0.024
0.046
0.058
0.32
0.45
0.36
0.10
−0.02
−0.32
−0.45
−0.47
−0.42
16–30 cm
0.001
0.001
0.009
0.024
0.070
0.40
0.50
0.36
0.12
0.00
−0.39
−0.40
−0.49
−0.46
31–45 cm
0.0003
0.0007
0.002
0.006
0.051
0.30
0.36
0.20
−0.10
−0.21
−0.28
−0.27
−0.54
−0.50
46–60 cm
0.0002
0.0006
0.002
0.004
0.064
0.31
0.39
0.18
−0.07
−0.26
−0.38
−0.28
−0.57
−0.52
Suburb (n = 4)
0–15 cm
0.001
0.001
0.004
0.007
0.081
0.48
0.57
−0.08
—
—
−0.52
—
—
−0.51
16–30 cm
0.001
0.0008
0.003
0.005
0.054
0.50
0.56
—
—
—
—
—
—
—
31–45 cm
0.0007
0.0007
0.002
0.004
0.074
0.53
0.62
—
—
—
—
—
—
—
46–60 cm
0.0005
0.0006
0.002
0.003
0.056
0.55
0.61
−0.12
—
—
−0.62
—
—
−0.62
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
205 Tl, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
0.26
0.20
0.26
0.03
3.2
−0.61
−0.61
0.17
−0.95
−0.20
0.70
Lysimetric waters
0.04
0.04
0.024
0.002
0.07
−0.14
−0.17
0.07
−0.22
−0.05
0.17
Mushroom
0.015
0.009
0.016
0.002
0.081
−0.18
−0.28
0.30
−0.62
0.42
1.04
Litter
0.030
NA
NA
NA
NA
−0.41
NA
NA
NA
NA
NA
Wood ash
0.230
NA
NA
NA
NA
−0.27
NA
NA
NA
NA
NA
Needles
0.010
0.010
0.020
0.001
0.090
−0.31
−0.38
0.21
−0.63
0.16
0.89
Leaves
0.006
0.004
0.007
0.001
0.043
−0.30
−0.39
0.16
−0.42
−0.09
0.33
Lichens
0.023
0.009
0.024
0.004
0.060
−0.53
−0.54
0.10
−0.72
−0.41
0.31Table 12
Zinc concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
66Zn, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
7.2
230
180
96
38
13
560
−0.13
−0.07
0.01
0.02
−0.24
0.30
−0.04
16–30 cm
17
100
260
120
45
14
560
−0.17
−0.17
−0.14
−0.11
−0.31
0.32
−0.14
31–45 cm
5.4
49
35
18
23
11
140
0.01
−0.07
−0.09
−0.06
−0.01
0.34
−0.01
46–60 cm
4.9
35
12
7.4
22
11
91
0.01
0.02
0.04
0.00
0.30
0.37
0.15
Suburb (n = 4)
0–15 cm
7.9
75
27
5.6
15
12
140
−0.23
—
—
0.11
—
—
−0.09
16–30 cm
10
49
24
5.5
11
11
110
—
—
—
—
—
—
—
31–45 cm
7.6
110
13
3.4
14
10
160
—
—
—
—
—
—
—
46–60 cm
10
28
14
3.6
15
10
84
−0.13
—
—
0.10
—
—
0.03
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
66Zn, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
93
83
72
28
640
0.18
0.16
0.20
−0.47
0.69
1.16
Lysimetric waters
5.0
4.6
3.2
1.3
11
0.15
0.14
0.13
−0.05
0.30
0.35
Mushroom
120
110
50
40
260
0.58
0.55
0.36
−0.16
1.25
1.41
Litter
220
NA
NA
NA
NA
0.00
NA
NA
NA
NA
NA
Wood ash
6200
NA
NA
NA
NA
−0.45
NA
NA
NA
NA
NA
Needles
51
50
19
22
96
−0.09
−0.08
0.30
−0.96
0.67
1.64
Leaves
220
180
140
11
800
−0.13
−0.11
0.21
−0.94
0.24
1.18
Lichens
57
60
8
36
70
0.04
0.07
0.06
−0.07
0.11
0.17Discussion in this section will start with an examination of multielement patterns which help identify major processes affecting all the samples. The multielement patterns will be followed by a section focused on element-specific patterns including relative differences between the city and suburban samples and relative differences a function of soil depth. Comparing the data between the city and the suburb locations (and between upper and lower soil layers) gives an indication of the isotopic and elemental signature of anthropogenic activity. Depth-related differences in the isotope ratios of labile SEP fractions within the soil profiles might reaffirm a potential role of gradual soil thawing during spring-early summer in the availability of specific element pools with variable isotopic composition to plant root system, as suggested in previous studies [2, 30, 31]. It is important to point out that differences in soil characteristics/morphology at each location may play an important role in the differences observed. The final area of discussion will highlight a case study involving environmental pollution.


#### 3.1.1. Multielement Patterns

(1) Batch-Type Leach Water and Lysimeritc Waters. The batch-type water leaches (fraction F1) and lysimetric waters have similar elemental concentrations, with the exception of Cu, Pb, and Zn, (assuming an average water to soil mass ratio of 1 : 10 for the F1 fraction). The concentrations of the latter analytes are several orders of magnitude lower in lysimetric waters than in the F1 fraction. Most of the isotopic compositions of the elements follow a similar pattern. Isotopic ratios of radiogenic elements (Pb and Sr) in the F1 fractions from upper soil layers overlap the compositions of lysimetric waters. The differences in the isotopic compositions of B, Cd, and Fe between these two matrices are also very minor. However, lysimetric waters were found to be preferentially enriched in the heavy isotopes of Cr, Cu, and Zn relative to the batch-type leach waters.The overall isotopic and elemental pattern is most readily explained as the product of exchange between rainwater and soil particles. In natural systems, weakly sorbed elements such as Cu and Pb likely undergo reversible sorption and their retention is strongly depended on meteoric percolation dynamics.At least for Cu and Zn, this portioning/sorption process induces stable isotope fractionation [32].(2) Biologic Samples. Comparing the compositions of the biologic samples, i.e., lichen, mushrooms, and vascular plant tissue, from the same location can help differentiate biochemical variability from geochemical variability. Lichens do not contain roots, and therefore, their composition is expected to provide information on aerial (precipitation, sea aerosols, and long range pollution) sources of elements [33]. Unlike lichens, fruit bodies of mushrooms and vascular plant tissue are much less affected by direct contribution from airborne sources, both because of very short duration of exposure and significantly lower surface area/volume ratio.For many elements (Cd, Cu, Fe, Pb, and Zn), lichens display a significantly narrower range of isotopic variability than mushrooms, leaves, and needles. This is probably a reflection of the isotopically homogenous nature of Aeolian inputs combined with limited biologic fractionation of stable isotopes within lichen [16, 34, 35]. Lichens have significantly higher concentrations of Cr, Pb, and Tl and lower concentrations of B and Sr relative to leaves and needles. This indicates that atmospheric pollution is a significant source for heavy metals in the region relative to potential geologic sources.The mushrooms are not only accumulating Cd, Cu, and Zn relative to the water-leachable element fraction of soils, but, with the exception of Cd, the isotopic composition of these metals also differs between the mushrooms and lysimeric waters and/or the local soil. The most likely explanation of this isotopic fractionation is the active uptake of heavy metals by siderophilic root exudates. Lithophilic and chalcophilic elements (B, Cd, Pb, Sr, and Tl) do not appear to be significantly fractionated by mushrooms. The mushrooms’ ability to accumulate Cd without inducing isotopic fraction may indicate an alternative biochemical mechanism for element uptake in mushrooms.It is difficult to identify any clear patterns in the leaf and needle data (Tables4–12). This may be a result of the far greater biochemical complexities of higher plants causing a much wider spread of interspecies and intertree isotopic variability. The litter layer was sampled to study potential isotopic shift related to nutrient reabsorption back into tree during late stages of senescence [36]. However, preliminary analysis of Fe and Pb concentration data demonstrate that the litter had become significantly contaminated by soil particles. The isotope signature of leaves in late stage of development therefore overlapped with the isotopic composition of the top soils.


#### 3.1.2. Single-Element Patterns

(1) Boron. Total B concentrations in the soil profile decrease with depth in the city samples, but not in the suburban samples (Table 4). Between 80% and 95% of the total B content was associated with the refractory phases (F5-F6) consistent with mineral bound B being the main source of B in the soils [37]. Secondary mineral formation is associated with the preferential incorporation of 10B into the secondary minerals [38] resulting in a heavier residual B composition in solution. This process appears to be the best explanation of the composition of the lysimetric waters in the present study (δ11Bwater-soil ≈ +11‰). The B isotopic composition of the mobile fraction trends towards a heavier signature in the upper soil layers, probably reflecting input from vegetation with plant biomass having distinctly heavier values (δ11Bleaves/needles-soil ≈ +20‰).There is a notable trend towards heavier B isotopic signatures in the direction soil < plants < lichens with soil consistently characterized by negativeδ-values and plant materials always having positive δ11B. Boron is not thought to be strongly fractionated by biological activity [39]; thus, this trend can, at least partially, also be explained by source mixing. The isotopic composition of the lichens (mean value of +32% for δ11B) will be affected by aerial marine aerosols with δ11B of about +40% [40], and the influence from this source could also explain the isotopic composition of leaves and needles in coastal regions. The total span of δ11B values for our samples vary by around 64‰ (Table 4), corresponding to almost half of the published span of δ11B values [41]. More interestingly, the results for our bioindicator samples (mushrooms, needles, leaves, and lichens) show similar variability to coffee beans collected from vastly different geographic areas [8, 42] (Table 4). Overall, the B isotope systems appear to have characteristics which favor its use as an abiotic tracer of source mixing.(2) Cadmium. The soil in the city locations contained significantly more Cd than the suburban location (Table 5). Such concentration difference is more pronounced in the surface soil layers compared to deeper profiles. For example, the upper most layers of the city soil profiles contain, on average, about 10 times the concentration found in the deepest inorganic layer. The major part of Cd is present in relatively mobile phases as about 70% of the total soil Cd was found in fractions (F1-F2-F3-F4). The reducible fraction (F3) contains especially high concentrations of Cd. This pattern suggests an anthropogenic source of Cd in the urban soil samples, but Cd isotopes do not appear a reliable means of identifying the pollution source.Published variations ofδ114Cd values in rock and mineral samples do not exceed 1‰, excluding the extreme fractionation values published for extraterrestrial material [43]. This relatively narrow fractionation span (corresponding to 0.25‰ per mass unit) is small compared to light elements such as Li and B, reflecting less relative mass difference between Cd isotopes. The mass balanced soil Cd pool has an isotopic composition equal within measurement uncertainty to δ114Cd = 0‰ and the fractions with highest Cd concentrations do not have a distinct isotope signature. Cadmium isotopes do however appear to be influenced by biological activity.There are limited published data on the Cd isotope ratios of nongeologic material, while geologic matrixes display a narrow range of isotope compositions. The range inδ114Cd values found in the leaves from the studied area (almost 2‰, Table 5) by far exceeds the variability of the geologic samples and the soil and lysimetric waters in this study. Thus, significant Cd fractionation occurs during Cd uptake or incorporation into the leaves. Biologically mediated fractionation appears to be the best explanation of the heavier Cd isotopic composition in bioindicators [2, 21]. It has been proposed [44] that carrier-mediated transport plays a major role in the root uptake process for Zn, and such process, also defined high-affinity transport, has been associated to a preferential translocation of heavier isotopes. Preferential incorporation of the heavy isotopes could explain also the observed shift between soil and leave isotope signatures (average δ114Cdsoil-leaves ≈ −0.4‰), as confirmed in recent studies [45], as well as the negative δ114Cd for the residual/immobile Cd pool in the soils.(3) Chromium. There are minor differences in soil Cr concentrations between the sample locations (Table 6). Top soils have slightly lower Cr contents, which is probably due to dilution by Cr-poor organic material (offal). The mobile fractions contain only a minor share of the total Cr pool irrespective of location or depth; on average, 83–88% of the total Cr is associated with residual phases. Cr isotopic compositions are very homogenous with practically all ratios in soils being the same within the uncertainty of the method (Table 3).The Cr content of mushrooms, needles, and leaves was too low for accurate isotopic ratio measurements.δ53Cr values increased from soil-to-soil solution to lichens. Wet deposition could be the explanation for the heavy signature found for δ53Cr in lichens [46]. There is a positive correlation between Cr concentrations and increasing proximity to chromite processing steelworks and a negative correlation between δ53Cr values and increasing proximity to the steelworks implicating the smelter as the primary airborne Cr contributor in the area.(4) Copper. Highest concentrations of Cu were found in the upper soil horizons from the city location and concentrations decrease with depth (Table 7). Similarly to Cd soil distribution, Cu is significantly less stratified in the suburb soil than in the soil from the city. However, Cu is bound in soils in a different pool than Cd. Most of the Cu in top soil resides in the oxidizable fraction (F4), generally associated with organic matter. The smallest Cu pool was found within the F3 fraction in all depths and at all sample locations. Hence, Cu is not associated with Mn and Fe-oxides in the soil profiles.The Cu isotopic ratios show no notable variations with soil depth. The Cu in the city soils has a heavy isotopic signature, while the suburban soil has aδ65Cu value of approximately −0.1‰. This is consistent with previously reported findings for soil systems affected by Cu from an anthropogenic source [47], affirming that Cu isotopes can be used an indicator of anthropogenic pollution.The biological samples have lighter Cu isotopic composition relative to the soil and lysimetric waters (Table7). A shift towards lighter δ65Cu in vegetation is consistent with the previous reports of Cu fractionation in plants (e.g., [48]), and a similar general pattern was reported for other nutrients [21, 49]. However, the fractionation may not be a sole result of a biomediated reaction. While reduction in the rhizosphere by organic exudates is associated with the fractionation of the bioavailable pools of Fe and Cu towards lighter values, a biotic reduction has the same effect at least for Fe [50].(5) Iron. The total concentrations of Fe in city soil samples are approximately twice than those found in the suburbs (Table 8). However, unlike Cu and Cd, Fe concentrations do not change significantly with depth, and the majority of Fe was bound on the F5 and F6 fractions thus associated with primary bedrock mineral phases. Fe is one of the least mobile elements during chemical weathering creating the potential for soil iron concentrations to increase with increasing weathering intensity. This is consistent with the elevated Fe concentrations in the city soil probably reflecting a higher degree of chemical weathering, caused by a longer exposure, than the suburban soils. The iron isotopic composition of the city soil with the average δ56Fe value = 0.16‰ is within the range of values reported for granite reference materials (0.13 ± 0.12‰, [51]).Clear iron isotopic variability within soil fractions is consistent with chemical weathering being the dominant driver of iron cycling in the soil. Iron isotopic composition of the F3 and F4 fractions resemble findings of previous studies [52, 53] attributing such variations to kinetic fractionation as a result of chemical weathering. The composition of leaching solutions used here for F1 and F2 soil fractions are different from those used in separation schemes designed specifically for Fe [54], which makes it difficult to compare the patterns. However, as mentioned in the previous section, redox processes may strongly fractionate iron (δ56FeII-III = −3‰ [55]). It is possible that the Fe isotopic fractionation between the F1 and F2 fractions in the upper 30 cm and lower 30 cm reflects a soil redox change with the lower (deeper?) soils being enriched in Fe2+.(6) Lead. Lead concentrations display the classic pattern expected for anthropogenic pollutant in soils. In deeper soil layers (depths >30 cm), Pb concentrations are constant at both locations. In the city location, there is a significant increase in Pb concentrations in the upper soil layers while Pb concentrations are constant at the surburb location. The excess Pb in the upper most city soil also has a significantly different Pb isotope composition than the geologic Pb in the region.The isotopic composition of the Pb pool in the suburban samples is within the range of agricultural soils reported for northern Sweden [56]. The upper soil horizons from the city soil contain Pb with a significantly less radiogenic value. Back calculating the isotopic composition of this excess Pb (assuming end-member mixing) provides a value near that found in modern lichen 206Pb/207Pb = 1.14 and 208Pb/207Pb = 2.38 (Table 9) [57]. All the bioindicators studied here have a significantly less radiogenic isotopic composition than the presumed natural Pb baseline in deep soil horizons.The absence of increased Pb in the suburban samples suggests that pollution is more local than what might be expected based on other locations in northern Sweden [58], and it might be explained by the relatively short time interval since the area emerged from the sea. The existence of various local pollution sources also appears to be evident in the wide spread of Pb isotopic ratios found in birch leaves and pine needles around Luleå.Moving away from using Pb as a pollution tracer, the selective extractions also highlight that the influence preferential mineral weathering can have on the isotopic compositions of Pb pools within soils. The residual fraction F6 (HF digestion) of the SEP used in the present study contains a uniform Pb concentration at all locations and depths with significantly less radiogenic Pb isotopic composition than in other fractions (Table9). Similarly, in a study of sediments from 31 lakes in Sweden [59], lower 206Pb/207Pb ratios were found in samples prepared using HF digestion compared to those treated using HNO3 + HClO4 (10 : 1 v/v). This was attributed to the Pb contribution from feldspars, which are more resistant to chemical weathering than most other minerals. In the present study, potassium feldspar is the main Pb carrier in the silicate soil fractions [60]. The majority of radiogenic Pb, formed in silicates by 238U, 235U, or 232Th decay, might be efficiently leached in the first five SEP fractions. This leaves the final HF fractionation with a less radiogenic isotope composition reflecting those for the time of mineral formation approximately 2 Ga years ago.(7) Strontium. Total Sr concentrations display little variability across the dataset (Table 10). Top soils have slightly lower Sr concentrations, as for Cr most likely reflecting dilution effects by organic matter. The majority of Sr is found in the residual fractions (F5-F6), suggesting most of the element is bound in refractory mineral phases within the soil.Mean87Sr/86Sr ratios in all environmental matrices from Luleå fall into a relatively narrow range (0.729–0.734) with little differences in isotopic composition between soil and bioindicators. Thus, unlike B, Sr in needles, leaves, and lichens appears to be of a terrestrial rather than marine origin; seawater aerosols have less radiogenic Sr isotope ratios [61]. To a significant degree, the homogeneity of the 87Sr/86Sr ratios is expected given the composition of the local bedrock [60, 62].Strontium isotopic ratios, primary variations in radiogenic87Sr abundance, have been extensively used for authentication and provenance studies [4]. Waters, crops, livestock, a variety of food products and ultimately man are known to reflect the Sr isotopic ratios typical for the geological setting in which they occur [63]. Strontium isotopic systematics has been also used, in combination with other systems, to trace anthropogenic sources in the environment [10, 11, 64].(8) Thallium. Total Tl concentrations in soils from city and suburban locations vary over a very limited range of approximately 0.4–0.6 µg·g−1 at all depths (Table 11). Thallium predominantly resides in the residual fractions (98% of Tl recovered in leachates F5-F6) most likely in the crystalline structure of silicate minerals such as potassium feldspar and quartz [65]. Concentration of the remaining Tl fractions, associated with reducible and oxidizable phases, is significantly higher in top soil from the city than that in the suburb. Our findings reaffirm previously reported Tl speciation data for rhizospheric soils [66].There is very limited data on Tl isotopes in environmental samples if compared to other more “traditionally” studied isotopic systems. Tl isotopic ratio data from contaminated soils have been reported in literature with aδ205Tl value of ≈ −0.3‰ relative to the natural background, with average Tl concentrations of 0.75 µg·g−1 [67]. The same study reported a lighter Tl signature with increasing soil depth in both the extractable and the residual fractions which is similar to our findings (Table 11).F1 and F2 soil fractions have positiveδ205Tl values. This heavier signature is then can be traced in significantly higher δ205Tl found in lysimetric waters, which in turn may contribute to the heavier Tl ratios found in mushrooms, needles, and leaves (Table 11).(9) Zinc. Zinc concentrations follow a similar pattern as for Pb. The top soil layers from the city are significantly enriched in Zn while deeper soil horizons are characterized by more uniform concentrations (Table 12). The majority of Zn was found in the first four fractions (80–90% leached in F1−F4), suggesting that source of anthropogenic Zn, like Pb, contains the element in a readily mobile form. Isotopic composition patterns for Zn and Pb show little similarities.The deep soil layers (46–60 cm) have Zn isotopic compositions consistent with that of the local bedrock (−0.05–1.5‰; converted from the “Lyon” JMC 3–0749 L standard) [47]. The soil horizons with the highest Zn concentrations seem to be slightly enriched in the light isotopes of Zn, but the trend is not overly convincing. Previous studies reported that exogenous dust deposition does cause measurable shift in soils Zn isotopic composition [68] which otherwise is relatively constant [30] for less contaminated soils. This suggests that the source of anthropogenic Zn has a Zn isotope composition very close to the local bedrock. Previously, Zn fractionation in soil horizons was attributed to sorption onto the Fe oxyhydroxides [47].The meanδ66Zn of top soils and lysimetric waters is approximately +0.2‰, while a significantly higher value of +0.6‰ was found in mushrooms indicating preferential uptake of heavier isotopes. The mechanism(s) of uptake of heavy metal ions by fungi can be via either an active or passive [69], and the prevailing heavier Zn signature in mushrooms compared to the soil pool suggests an active uptake strategy. On the contrary, Zn in needles and leaves is isotopically lighter most likely as a result of fractionation processes during Zn translocation through the shoot [70], favoring lighter isotopes.


### 3.2. Landfills and Industrial Wastes

Pollution source tracing using isotopic data can be challenging for a number of reasons:(i)
The composition of potential sources is seldom represented by isotopically well-defined end members(ii)
The isotopic signature of potential sources may overlap natural isotopic variability(iii)
Even where end-member compositions are distinct and well-constrained, there might be a large number of potential sources(iv)
For stable isotopes, numerous postdeposition fractionating processes may alter the original ratios (see, e.g., [4])In order to demonstrate the severity of these complicating factors, concentration and isotopic data for waste samples from local industries (Cu slag, Fe slag, and fly ash) and two heavily contaminated soils (landfills) were obtained (Table13). These waste samples are very likely to be a major contributor to the landfills, and the goal of the exercise was to attempt identification of the presence of the industrial waste materials in the landfill using concentration patterns and isotopic fingerprints.Table 13
Concentration and isotopic data for two contaminated soils (landfill A and landfill B) and waste samples from local industries (Fe, Cu slag, and fly ash).
Cd,µg·g−1
δ
114Cd
Cr,µg·g−1
δ
53Cr
Cu,µg·g−1
δ
63Cu
Fe, %
δ
56Fe
Zn,µg·g−1
δ
66Zn
Pb,µg·g−1
206Pb/207Pb
Landfill A
1.5
0.0
450
0.2
2700
−1.0
15
0.4
1100
1.4
40
1.32
Landfill B
0.6
−1.5
2600
0.1
170
−1.4
10
1.0
180
−0.2
170
1.17
Fe slag
0.2
0.1
4100
0.1
100
0.7
12
0.9
150
−0.7
250
1.16
Cu slag
11
−0.2
650
0.1
16000
0.1
35
0.4
12000
0.0
200
1.17
Fly ash
1.1
1.7
50
0.2
25
0.3
2.7
0.2
50
0.6
15
1.21Both landfills are high in Cd with Cd concentrations at least 10 times higher than those found in the soil from the suburb location. The Cd in landfill A is relatively unfractionated which may point towards Cu slag as the most likely source of the element as Cd found in Cu slag has an isotopic composition undistinguishable from the mean for top soils. Fly ash, on the contrary, is significantly enriched in heavier Cd isotopes. Copper slag is also significantly enriched in Cu, Zn, and Fe relative to the other pollution sources so these elements would be expected to be enriched in landfill A if Cu slag was indeed the source of Cd. This fits very well with the concentrations measurements of landfill A (Table13). This raises the question of why the Zn and Cu isotopic compositions of landfill A are nothing like the Zn and Cu isotopic compositions of Cu slag.Based on the overall elemental concentrations of Zn and Cu in landfill A, it is hard to imagine that source mixing can account for the isotopic offset between the slag and the landfill. This is because it would take an enormous quantity of these elements from a highly fractionated source to attain the isotope composition of the landfill if there is really slag present in the landfill. Alternatively, post depositional processes might significantly alter the isotopic composition of landfill, though this contradicts by the observed lack of fractionation of Fe isotopes in landfill A. The Fe isotope compositions of landfill A and Cu slag are identical, and most processes which heavily fractionate Cu and Zn isotopes would also be expected to fractionate Fe isotopes.The picture is not clarified by the evaluation of landfill B. Landfill B has a number of characteristics pointing towards Fe slag being the primary source of contamination with fly ash being a second significant source of contaminants. The Fe, Zn, Cu, Cr, and Cd concentrations and Cr, Fe, and Zn isotope compositions of landfill B are consistent with Fe slag mixed with some fly ash. At the same time, the Cu and Cd isotopic composition of landfill B requires an alternative explanation. It is possible that Cu isotopes are just not a reliable tracer of pollution sources in these landfills, but it is harder to account for Cr and Zn isotopes. The systems appear reliable in one of the landfills but not in the other.Overall this case study highlights that pollution source mixing can be challenging, but the difficulty is proportional to the number of elements and isotopes measured. We cannot readily account for the behaviour of all the systems we measured, but a weight-of-evidence approach allows for the potential sources of pollution identified with some certainty. That is while any number of factors may complicate source tracing, they do not render the process total ineffective.


## 3.1. Element Concentrations and Isotope Ratios in Environmental Samples

Isotopic composition and concentration data for each element studied is presented in Tables4–12. The tables are formatted to show the soil profile information for all six SEP fractions in the city and suburb locations (with the reported concentrations representing an average of the individual profiles). For some analytes, only pooled isotopic ratio data is available (F1 + F2 + F3 and F4 + F5 + F6) due to there being insufficient concentrations in the single extractions to make the isotopic measurements. Concentration and isotopic ratio data for the top soils, lysimetric waters, mushrooms, needles, leaves, lichens, and litter sample are reported, for comparison, below the profile data.Table 4
Boron concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
11B, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.57
0.24
0.48
1.05
1.71
3.87
7.91
2
−9
−17
−12
−12
−7
−9
16–30 cm
0.21
0.16
0.15
0.35
0.62
2.88
4.38
−3
−11
−16
−13
−10
−19
−16
31–45 cm
0.04
0.11
0.04
0.09
0.38
1.90
2.56
−9
−11
−10
−15
−16
−24
−22
46–60 cm
0.04
0.15
0.02
0.06
0.34
1.86
2.47
−4
−6
−7
−15
−12
−23
−21
Suburb (n = 4)
0–15 cm
0.16
0.06
0.10
0.17
0.83
5.15
6.47
−25
−24
−17
−2
−17
−14
−14
16–30 cm
0.11
0.06
0.06
0.10
0.60
5.01
5.94
−7
−13
−8
−11
−15
−2
−4
31–45 cm
0.06
0.11
0.04
0.07
0.80
5.10
6.17
−10
−4
−2
10
−6
−4
−4
46–60 cm
0.05
0.09
0.04
0.05
0.58
4.75
5.56
−6
−2
−5
12
−14
−8
−9
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
11B, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
8
7
7
2
53
−7
−8
7
−17
12
29
Lysimetric waters
10
7
12
5
54
4
4
3
−2
7
9
Mushroom
1.3
0.6
1.5
0.2
6.8
−8
−10
13
−24
3
27
Litter
21
NA
NA
NA
NA
8
NA
NA
NA
NA
NA
Wood ash
290
NA
NA
NA
NA
7
NA
NA
NA
NA
NA
Needles
14
13
6
6
31
17
19
9
−2
38
40
Leaves
21
18
13
7
76
10
10
9
−7
34
41
Lichens
2.7
2.4
1.1
1.6
6.6
32
37
9
13
40
27Table 5
Cadmium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
114Cd, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.006
0.016
0.427
0.149
0.122
0.036
0.756
0.08
0.04
0.08
−0.19
−0.19
—
−0.02
16–30 cm
0.003
0.012
0.137
0.056
0.049
0.032
0.289
0.17
0.40
0.09
−0.69
−0.31
—
−0.10
31–45 cm
0.001
0.012
0.019
0.015
0.016
0.019
0.081
0.25
0.26
−0.02
−0.91
−0.24
—
−0.15
46–60 cm
0.001
0.016
0.005
0.010
0.015
0.017
0.065
0.26
0.33
−0.06
0.00
−0.91
—
−0.09
Suburb (n = 4)
0–15 cm
0.002
0.010
0.027
0.010
0.013
0.012
0.074
0.23
—
—
—
—
—
16–30 cm
0.001
0.027
0.012
0.008
0.009
0.011
0.069
—
—
—
—
—
—
31–45 cm
0.001
0.026
0.008
0.005
0.010
0.010
0.061
—
—
—
—
—
—
46–60 cm
0.001
0.025
0.003
0.006
0.009
0.012
0.056
0.19
—
—
—
—
—
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
114Cd, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
0.66
0.51
0.32
0.13
2.40
0.08
0.09
0.14
−0.32
0.42
0.74
Lysimetric waters
0.04
0.03
0.05
0.01
0.22
0.22
0.19
0.07
0.14
0.34
0.20
Mushroom
1.6
1.2
1.4
0.03
5.0
0.15
0.23
0.28
−0.71
0.52
1.23
Litter
0.30
NA
NA
NA
NA
0.17
NA
NA
NA
NA
NA
Wood ash
3.3
NA
NA
NA
NA
−0.33
NA
NA
NA
NA
NA
Needles
0.06
0.04
0.04
0.01
0.16
0.09
0.10
0.26
−0.52
0.56
1.08
Leaves
0.33
0.29
0.16
0.06
0.83
0.46
0.48
0.29
−0.60
1.31
1.91
Lichens
0.13
0.12
0.03
0.09
0.18
0.08
0.07
0.03
0.05
0.18
0.13Table 6
Chromium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
53Cr, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.09
0.18
0.14
7.5
7.7
9.5
25
−0.16
−0.11
0.38
0.04
0.04
0.11
0.04
16–30 cm
0.09
0.10
0.12
4.3
11
11
27
−0.13
−0.12
0.37
0.02
0.03
0.09
0.03
31–45 cm
0.09
0.03
0.06
2.8
11
8.8
23
0.05
0.10
0.21
0.04
0.02
0.11
0.04
46–60 cm
0.04
0.04
0.05
1.7
15
9.2
26
0.01
0.12
0.28
0.11
0.01
0.12
0.04
Suburb
a (n = 4)
0–15 cm
0.08
0.13
0.13
2.4
8.5
11
22
0.22
—
—
0.11
—
—
0.11
16–30 cm
0.09
0.06
0.13
2.0
5.8
10
18
—
—
—
—
—
—
—
31–45 cm
0.08
0.04
0.14
2.0
8.6
10
21
—
—
—
—
—
—
—
46–60 cm
0.10
0.02
0.16
1.9
7.8
9.0
19
0.16
—
—
0.12
—
—
0.12
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
53Cr, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
21
18
16
4
68
0.10
0.07
0.143
−0.16
0.41
0.57
Lysimetric waters
4.3
4.4
0.4
3.9
5.1
0.26
0.26
0.01
0.25
0.27
0.02
Mushroom
0.12
0.10
0.12
0.01
0.63
NA
NA
NA
NA
NA
NA
Litter
1.8
NA
NA
NA
NA
NA
NA
NA
NA
NA
NA
Wood ash
70
NA
NA
NA
NA
0.12
NA
NA
NA
NA
NA
Needles
0.23
0.21
0.19
0.05
0.97
NA
NA
NA
NA
NA
NA
Leaves
0.26
0.22
0.15
0.10
0.95
NA
NA
NA
NA
NA
NA
Lichens
2.2
1.6
1.1
1.5
4.2
0.36
0.36
0.11
0.21
0.57
0.36
aValues reported as empty entries are due to pooling of several fractions. The isotopic values reported for the outmost top and bottom layers for F1 and F4 correspond to averaged values of respectively soil profiles F1+F2+F3 and F4+F5+F6 fractions.Table 7
Copper concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
65Cu, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.33
0.58
0.08
26
11
1.2
39
0.10
0.05
0.38
0.23
0.29
0.06
0.26
16–30 cm
0.18
0.21
0.06
9.4
5.7
0.46
16
0.28
0.30
0.11
0.40
0.22
−0.23
0.31
31–45 cm
0.16
0.11
0.03
3.1
3.5
0.31
7.2
0.15
0.30
0.92
0.16
0.25
0.51
0.26
46–60 cm
0.14
0.15
0.05
2.0
3.9
0.34
6.6
0.27
0.41
1.04
0.68
0.22
−0.47
0.33
Suburb (n = 4)
0–15 cm
0.13
0.50
0.06
2.1
3.0
0.58
6.4
0.35
—
—
−0.14
—
—
−0.06
16–30 cm
0.12
0.17
0.06
1.9
2.1
0.37
4.8
—
—
—
—
—
—
—
31–45 cm
0.09
0.07
0.07
1.5
2.6
0.58
4.9
—
—
—
—
—
—
—
46–60 cm
0.08
0.05
0.06
1.2
2.0
0.39
3.8
0.06
—
—
−0.11
—
—
−0.10
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
65Cu, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
15
11
11
3
84
0.06
0.01
0.21
−0.51
0.51
1.02
Lysimetric waters
0.6
0.5
0.2
0.4
1.1
0.76
0.72
0.17
0.64
0.99
0.35
Mushroom
44
39
25
10
120
−0.56
0.74
−2.4
0.62
3.02
Litter
7
NA
NA
NA
NA
−0.08
NA
NA
NA
NA
NA
Wood ash
180
NA
NA
NA
NA
−1.00
NA
NA
NA
NA
NA
Needles
3.2
3.0
0.9
2.1
5.2
−1.09
−1.15
0.58
−2.0
0.05
2.08
Leaves
7.1
5.3
3.4
3
17
−0.35
−0.33
0.35
−1.34
0.83
2.15
Lichens
4.6
4.5
1.0
3.1
7.1
0.05
0.05
0.20
−0.28
0.30
0.58Table 8
Iron concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg g−1 DW
δ
56Fe, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
26
110
420
2700
16000
6800
26000
0.21
0.21
−2.0
0.33
0.22
0.17
0.19
16–30 cm
48
31
290
2100
14000
6000
22000
0.10
0.24
−1.8
0.36
0.20
0.16
0.18
31–45 cm
75
15
200
740
12000
5300
18000
0.07
−0.67
−1.3
0.88
0.18
0.15
0.17
46–60 cm
39
17
160
330
14000
6000
21000
0.07
−1.4
−1.1
0.75
0.19
0.11
0.16
Suburb (n = 4)
0–15 cm
45
66
560
530
7000
6100
14000
−0.87
—
—
0.09
—
—
0.04
16–30 cm
73
33
620
780
5800
5100
13000
—
—
—
—
—
—
—
31–45 cm
54
10
630
550
7400
5500
14000
—
—
—
—
—
—
—
46–60 cm
54
7
580
460
7000
5400
13000
−0.49
—
—
0.20
—
—
0.16
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
56Fe, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
19000
17000
9000
4100
72000
0.07
0.10
0.13
−0.33
0.45
0.78
Lysimetric waters
5200
5400
900
3600
5900
0.19
0.15
0.43
−0.20
0.91
1.11
Mushroom
130
40
330
17
2100
−0.48
−0.47
0.35
−1.16
0.26
1.42
Litter
1180
NA
NA
NA
NA
0.07
NA
NA
NA
NA
NA
Wood ash
3500
NA
NA
NA
NA
0.67
NA
NA
NA
NA
NA
Needles
140
110
110
33
440
−0.41
−0.35
0.41
−1.4
0.05
1.45
Leaves
200
160
150
61
1500
−0.29
−0.26
0.20
−0.84
0.09
0.93
Lichens
250
210
110
150
500
−0.09
−0.09
0.04
−0.14
−0.02
0.12Table 9
Lead concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,μg·g−1 DW
206Pb/207Pb/208Pb/207Pb
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.31
0.02
3.2
52
30
5.9
91
1.14/2.37
1.16/2.41
1.15/2.39
1.15/2.42
1.17/2.43
1.10/2.34
1.15/2.41
16–30 cm
0.17
0.02
0.75
9.4
18
6.6
35
1.17/2.43
1.20/2.43
1.16/2.43
1.17/2.43
1.20/2.44
1.09/2.33
1.17/2.41
31–45 cm
0.08
0.02
0.27
1.3
7.7
4.3
14
1.28/2.50
1.23/2.46
1.22/2.49
1.28/2.51
1.35/2.49
1.13/2.34
1.27/2.44
46–60 cm
0.02
0.03
0.08
0.15
4.3
4.9
9.4
1.42/2.61
1.35/2.54
1.42/2.60
1.42/2.58
1.54/2.62
1.13/2.34
1.32/2.47
Suburb (n = 4)
0–15 cm
0.04
0.04
0.54
1.2
5.9
5.9
14
1.32/2.57
1.35/2.58
1.29/2.54
1.32/2.56
1.38/2.55
1.08/2.32
1.24/2.44
16–30 cm
0.04
0.08
0.34
0.26
4.6
5.5
11
1.30/2.55
1.25/2.53
1.26/2.48
1.30/2.51
1.37/2.55
1.08/2.32
1.22/2.43
31–45 cm
0.04
0.08
0.19
0.52
4.2
6.8
12
1.33/2.56
1.23/2.50
1.29/2.52
1.38/2.64
1.42/2.58
1.08/2.32
1.21/2.42
46–60 cm
0.02
0.07
0.07
0.05
3.2
7.4
11
1.44/2.64
1.22/2.50
1.46/2.61
1.54/2.69
1.55/2.64
1.08/2.32
1.21/2.41
Concentration,µg·g−1 DW (µg·L−1 for waters)
206Pb/207Pb/208Pb/207Pb
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
18
16
21
5
470
1.35/2.49
1.34/2.50
0.15/0.01
1.05/2.30
1.77/2.61
0.72/0.31
Lysimetric waters
0.50
0.40
0.40
0.03
1.1
1.17/2.45
1.17/2.44
0.03/0.02
1.10/2.42
1.20/2.47
0.10/0.05
Mushroom
0.17
0.11
0.14
0.01
0.51
1.18/2.45
1.17/2.45
0.04/0.03
1.10/2.41
1.30/2.56
0.20/0.15
Wood ash
6.4
NA
NA
NA
NA
1.15/2.40
NA
NA
NA
NA
NA
Litter
2.3
NA
NA
NA
NA
1.16/2.42
NA
NA
NA
NA
NA
Needles
0.15
0.12
0.11
0.02
0.54
1.18/2.42
1.18/2.42
0.03/0.03
1.11/2.34
1.26/2.47
0.15/0.21
Leaves
0.29
0.21
0.29
0.04
2.1
1.18/2.44
1.18/2.43
0.03/0.02
1.11/2.39
1.25/2.49
0.14/0.10
Lichens
1.9
1.8
0.4
1.3
2.6
1.14/2.38
1.14/2.38
0.01/0.01
1.14/2.37
1.15/2.40
0.01/0.03Table 10
Strontium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
87Sr/86Sr
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.5
2.3
11
5.4
6.4
141
167
0.730
0.734
0.734
0.733
0.732
0.727
0.727
16–30 cm
0.3
1.7
5.1
3.0
6.0
138
154
0.727
0.734
0.733
0.735
0.733
0.731
0.732
31–45 cm
0.1
1.2
1.0
0.70
7.0
161
171
0.724
0.734
0.728
0.726
0.735
0.727
0.727
46–60 cm
0.1
1.2
0.60
0.50
7.7
170
180
0.727
0.743
0.724
0.727
0.747
0.727
0.728
Suburb (n = 4)
0–15 cm
0.3
0.6
1.2
0.62
6.5
146
146
0.727
—
—
0.732
—
—
0.732
16–30 cm
0.2
1.1
0.69
0.42
4.8
148
148
—
—
—
—
—
—
—
31–45 cm
0.1
1.5
0.41
0.33
6.0
179
179
—
—
—
—
—
—
—
46–60 cm
0.1
1.4
0.32
0.31
5.1
188
188
0.729
—
—
0.733
—
—
0.733
Concentration,µg·g−1 DW (µg·L−1 for waters)
87Sr/86Sr
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
25
23
15
3
150
0.731
0.731
0.004
0.723
0.739
0.016
Lysimetric waters
12
10
2
8
12
0.733
0.733
0.001
0.732
0.733
0.010
Mushroom
0.5
0.3
0.2
0.1
1.8
0.729
0.727
0.006
0.721
0.750
0.039
Litter
28
NA
NA
NA
NA
0.731
NA
NA
NA
NA
NA
Wood ash
950
NA
NA
NA
NA
0.732
NA
NA
NA
NA
NA
Needles
18
15
16
2
63
0.734
0.733
0.007
0.724
0.754
0.030
Leaves
34
31
16
6
120
0.730
0.730
0.005
0.721
0.742
0.024
Lichens
8.3
7.4
3.9
2.5
16
0.733
0.731
0.006
0.725
0.742
0.017Table 11
Thallium concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
205 Tl, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
0.004
0.002
0.024
0.046
0.058
0.32
0.45
0.36
0.10
−0.02
−0.32
−0.45
−0.47
−0.42
16–30 cm
0.001
0.001
0.009
0.024
0.070
0.40
0.50
0.36
0.12
0.00
−0.39
−0.40
−0.49
−0.46
31–45 cm
0.0003
0.0007
0.002
0.006
0.051
0.30
0.36
0.20
−0.10
−0.21
−0.28
−0.27
−0.54
−0.50
46–60 cm
0.0002
0.0006
0.002
0.004
0.064
0.31
0.39
0.18
−0.07
−0.26
−0.38
−0.28
−0.57
−0.52
Suburb (n = 4)
0–15 cm
0.001
0.001
0.004
0.007
0.081
0.48
0.57
−0.08
—
—
−0.52
—
—
−0.51
16–30 cm
0.001
0.0008
0.003
0.005
0.054
0.50
0.56
—
—
—
—
—
—
—
31–45 cm
0.0007
0.0007
0.002
0.004
0.074
0.53
0.62
—
—
—
—
—
—
—
46–60 cm
0.0005
0.0006
0.002
0.003
0.056
0.55
0.61
−0.12
—
—
−0.62
—
—
−0.62
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
205 Tl, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
0.26
0.20
0.26
0.03
3.2
−0.61
−0.61
0.17
−0.95
−0.20
0.70
Lysimetric waters
0.04
0.04
0.024
0.002
0.07
−0.14
−0.17
0.07
−0.22
−0.05
0.17
Mushroom
0.015
0.009
0.016
0.002
0.081
−0.18
−0.28
0.30
−0.62
0.42
1.04
Litter
0.030
NA
NA
NA
NA
−0.41
NA
NA
NA
NA
NA
Wood ash
0.230
NA
NA
NA
NA
−0.27
NA
NA
NA
NA
NA
Needles
0.010
0.010
0.020
0.001
0.090
−0.31
−0.38
0.21
−0.63
0.16
0.89
Leaves
0.006
0.004
0.007
0.001
0.043
−0.30
−0.39
0.16
−0.42
−0.09
0.33
Lichens
0.023
0.009
0.024
0.004
0.060
−0.53
−0.54
0.10
−0.72
−0.41
0.31Table 12
Zinc concentrations and isotopic composition in environmental samples from Luleå.
Soil profiles
Concentration,µg·g−1 DW
δ
66Zn, ‰
Fractions
F1
F2
F3
F4
F5
F6
Total
F1
F2
F3
F4
F5
F6
Total
City (n = 2)
0–15 cm
7.2
230
180
96
38
13
560
−0.13
−0.07
0.01
0.02
−0.24
0.30
−0.04
16–30 cm
17
100
260
120
45
14
560
−0.17
−0.17
−0.14
−0.11
−0.31
0.32
−0.14
31–45 cm
5.4
49
35
18
23
11
140
0.01
−0.07
−0.09
−0.06
−0.01
0.34
−0.01
46–60 cm
4.9
35
12
7.4
22
11
91
0.01
0.02
0.04
0.00
0.30
0.37
0.15
Suburb (n = 4)
0–15 cm
7.9
75
27
5.6
15
12
140
−0.23
—
—
0.11
—
—
−0.09
16–30 cm
10
49
24
5.5
11
11
110
—
—
—
—
—
—
—
31–45 cm
7.6
110
13
3.4
14
10
160
—
—
—
—
—
—
—
46–60 cm
10
28
14
3.6
15
10
84
−0.13
—
—
0.10
—
—
0.03
Concentration,µg·g−1 DW (µg·L−1 for waters)
δ
66Zn, ‰
Mean
Median
σ
Min.
Max.
Mean
Median
σ
Min.
Max.
Range
Top soils
93
83
72
28
640
0.18
0.16
0.20
−0.47
0.69
1.16
Lysimetric waters
5.0
4.6
3.2
1.3
11
0.15
0.14
0.13
−0.05
0.30
0.35
Mushroom
120
110
50
40
260
0.58
0.55
0.36
−0.16
1.25
1.41
Litter
220
NA
NA
NA
NA
0.00
NA
NA
NA
NA
NA
Wood ash
6200
NA
NA
NA
NA
−0.45
NA
NA
NA
NA
NA
Needles
51
50
19
22
96
−0.09
−0.08
0.30
−0.96
0.67
1.64
Leaves
220
180
140
11
800
−0.13
−0.11
0.21
−0.94
0.24
1.18
Lichens
57
60
8
36
70
0.04
0.07
0.06
−0.07
0.11
0.17Discussion in this section will start with an examination of multielement patterns which help identify major processes affecting all the samples. The multielement patterns will be followed by a section focused on element-specific patterns including relative differences between the city and suburban samples and relative differences a function of soil depth. Comparing the data between the city and the suburb locations (and between upper and lower soil layers) gives an indication of the isotopic and elemental signature of anthropogenic activity. Depth-related differences in the isotope ratios of labile SEP fractions within the soil profiles might reaffirm a potential role of gradual soil thawing during spring-early summer in the availability of specific element pools with variable isotopic composition to plant root system, as suggested in previous studies [2, 30, 31]. It is important to point out that differences in soil characteristics/morphology at each location may play an important role in the differences observed. The final area of discussion will highlight a case study involving environmental pollution.


### 3.1.1. Multielement Patterns

(1) Batch-Type Leach Water and Lysimeritc Waters. The batch-type water leaches (fraction F1) and lysimetric waters have similar elemental concentrations, with the exception of Cu, Pb, and Zn, (assuming an average water to soil mass ratio of 1 : 10 for the F1 fraction). The concentrations of the latter analytes are several orders of magnitude lower in lysimetric waters than in the F1 fraction. Most of the isotopic compositions of the elements follow a similar pattern. Isotopic ratios of radiogenic elements (Pb and Sr) in the F1 fractions from upper soil layers overlap the compositions of lysimetric waters. The differences in the isotopic compositions of B, Cd, and Fe between these two matrices are also very minor. However, lysimetric waters were found to be preferentially enriched in the heavy isotopes of Cr, Cu, and Zn relative to the batch-type leach waters.The overall isotopic and elemental pattern is most readily explained as the product of exchange between rainwater and soil particles. In natural systems, weakly sorbed elements such as Cu and Pb likely undergo reversible sorption and their retention is strongly depended on meteoric percolation dynamics.At least for Cu and Zn, this portioning/sorption process induces stable isotope fractionation [32].(2) Biologic Samples. Comparing the compositions of the biologic samples, i.e., lichen, mushrooms, and vascular plant tissue, from the same location can help differentiate biochemical variability from geochemical variability. Lichens do not contain roots, and therefore, their composition is expected to provide information on aerial (precipitation, sea aerosols, and long range pollution) sources of elements [33]. Unlike lichens, fruit bodies of mushrooms and vascular plant tissue are much less affected by direct contribution from airborne sources, both because of very short duration of exposure and significantly lower surface area/volume ratio.For many elements (Cd, Cu, Fe, Pb, and Zn), lichens display a significantly narrower range of isotopic variability than mushrooms, leaves, and needles. This is probably a reflection of the isotopically homogenous nature of Aeolian inputs combined with limited biologic fractionation of stable isotopes within lichen [16, 34, 35]. Lichens have significantly higher concentrations of Cr, Pb, and Tl and lower concentrations of B and Sr relative to leaves and needles. This indicates that atmospheric pollution is a significant source for heavy metals in the region relative to potential geologic sources.The mushrooms are not only accumulating Cd, Cu, and Zn relative to the water-leachable element fraction of soils, but, with the exception of Cd, the isotopic composition of these metals also differs between the mushrooms and lysimeric waters and/or the local soil. The most likely explanation of this isotopic fractionation is the active uptake of heavy metals by siderophilic root exudates. Lithophilic and chalcophilic elements (B, Cd, Pb, Sr, and Tl) do not appear to be significantly fractionated by mushrooms. The mushrooms’ ability to accumulate Cd without inducing isotopic fraction may indicate an alternative biochemical mechanism for element uptake in mushrooms.It is difficult to identify any clear patterns in the leaf and needle data (Tables4–12). This may be a result of the far greater biochemical complexities of higher plants causing a much wider spread of interspecies and intertree isotopic variability. The litter layer was sampled to study potential isotopic shift related to nutrient reabsorption back into tree during late stages of senescence [36]. However, preliminary analysis of Fe and Pb concentration data demonstrate that the litter had become significantly contaminated by soil particles. The isotope signature of leaves in late stage of development therefore overlapped with the isotopic composition of the top soils.


### 3.1.2. Single-Element Patterns

(1) Boron. Total B concentrations in the soil profile decrease with depth in the city samples, but not in the suburban samples (Table 4). Between 80% and 95% of the total B content was associated with the refractory phases (F5-F6) consistent with mineral bound B being the main source of B in the soils [37]. Secondary mineral formation is associated with the preferential incorporation of 10B into the secondary minerals [38] resulting in a heavier residual B composition in solution. This process appears to be the best explanation of the composition of the lysimetric waters in the present study (δ11Bwater-soil ≈ +11‰). The B isotopic composition of the mobile fraction trends towards a heavier signature in the upper soil layers, probably reflecting input from vegetation with plant biomass having distinctly heavier values (δ11Bleaves/needles-soil ≈ +20‰).There is a notable trend towards heavier B isotopic signatures in the direction soil < plants < lichens with soil consistently characterized by negativeδ-values and plant materials always having positive δ11B. Boron is not thought to be strongly fractionated by biological activity [39]; thus, this trend can, at least partially, also be explained by source mixing. The isotopic composition of the lichens (mean value of +32% for δ11B) will be affected by aerial marine aerosols with δ11B of about +40% [40], and the influence from this source could also explain the isotopic composition of leaves and needles in coastal regions. The total span of δ11B values for our samples vary by around 64‰ (Table 4), corresponding to almost half of the published span of δ11B values [41]. More interestingly, the results for our bioindicator samples (mushrooms, needles, leaves, and lichens) show similar variability to coffee beans collected from vastly different geographic areas [8, 42] (Table 4). Overall, the B isotope systems appear to have characteristics which favor its use as an abiotic tracer of source mixing.(2) Cadmium. The soil in the city locations contained significantly more Cd than the suburban location (Table 5). Such concentration difference is more pronounced in the surface soil layers compared to deeper profiles. For example, the upper most layers of the city soil profiles contain, on average, about 10 times the concentration found in the deepest inorganic layer. The major part of Cd is present in relatively mobile phases as about 70% of the total soil Cd was found in fractions (F1-F2-F3-F4). The reducible fraction (F3) contains especially high concentrations of Cd. This pattern suggests an anthropogenic source of Cd in the urban soil samples, but Cd isotopes do not appear a reliable means of identifying the pollution source.Published variations ofδ114Cd values in rock and mineral samples do not exceed 1‰, excluding the extreme fractionation values published for extraterrestrial material [43]. This relatively narrow fractionation span (corresponding to 0.25‰ per mass unit) is small compared to light elements such as Li and B, reflecting less relative mass difference between Cd isotopes. The mass balanced soil Cd pool has an isotopic composition equal within measurement uncertainty to δ114Cd = 0‰ and the fractions with highest Cd concentrations do not have a distinct isotope signature. Cadmium isotopes do however appear to be influenced by biological activity.There are limited published data on the Cd isotope ratios of nongeologic material, while geologic matrixes display a narrow range of isotope compositions. The range inδ114Cd values found in the leaves from the studied area (almost 2‰, Table 5) by far exceeds the variability of the geologic samples and the soil and lysimetric waters in this study. Thus, significant Cd fractionation occurs during Cd uptake or incorporation into the leaves. Biologically mediated fractionation appears to be the best explanation of the heavier Cd isotopic composition in bioindicators [2, 21]. It has been proposed [44] that carrier-mediated transport plays a major role in the root uptake process for Zn, and such process, also defined high-affinity transport, has been associated to a preferential translocation of heavier isotopes. Preferential incorporation of the heavy isotopes could explain also the observed shift between soil and leave isotope signatures (average δ114Cdsoil-leaves ≈ −0.4‰), as confirmed in recent studies [45], as well as the negative δ114Cd for the residual/immobile Cd pool in the soils.(3) Chromium. There are minor differences in soil Cr concentrations between the sample locations (Table 6). Top soils have slightly lower Cr contents, which is probably due to dilution by Cr-poor organic material (offal). The mobile fractions contain only a minor share of the total Cr pool irrespective of location or depth; on average, 83–88% of the total Cr is associated with residual phases. Cr isotopic compositions are very homogenous with practically all ratios in soils being the same within the uncertainty of the method (Table 3).The Cr content of mushrooms, needles, and leaves was too low for accurate isotopic ratio measurements.δ53Cr values increased from soil-to-soil solution to lichens. Wet deposition could be the explanation for the heavy signature found for δ53Cr in lichens [46]. There is a positive correlation between Cr concentrations and increasing proximity to chromite processing steelworks and a negative correlation between δ53Cr values and increasing proximity to the steelworks implicating the smelter as the primary airborne Cr contributor in the area.(4) Copper. Highest concentrations of Cu were found in the upper soil horizons from the city location and concentrations decrease with depth (Table 7). Similarly to Cd soil distribution, Cu is significantly less stratified in the suburb soil than in the soil from the city. However, Cu is bound in soils in a different pool than Cd. Most of the Cu in top soil resides in the oxidizable fraction (F4), generally associated with organic matter. The smallest Cu pool was found within the F3 fraction in all depths and at all sample locations. Hence, Cu is not associated with Mn and Fe-oxides in the soil profiles.The Cu isotopic ratios show no notable variations with soil depth. The Cu in the city soils has a heavy isotopic signature, while the suburban soil has aδ65Cu value of approximately −0.1‰. This is consistent with previously reported findings for soil systems affected by Cu from an anthropogenic source [47], affirming that Cu isotopes can be used an indicator of anthropogenic pollution.The biological samples have lighter Cu isotopic composition relative to the soil and lysimetric waters (Table7). A shift towards lighter δ65Cu in vegetation is consistent with the previous reports of Cu fractionation in plants (e.g., [48]), and a similar general pattern was reported for other nutrients [21, 49]. However, the fractionation may not be a sole result of a biomediated reaction. While reduction in the rhizosphere by organic exudates is associated with the fractionation of the bioavailable pools of Fe and Cu towards lighter values, a biotic reduction has the same effect at least for Fe [50].(5) Iron. The total concentrations of Fe in city soil samples are approximately twice than those found in the suburbs (Table 8). However, unlike Cu and Cd, Fe concentrations do not change significantly with depth, and the majority of Fe was bound on the F5 and F6 fractions thus associated with primary bedrock mineral phases. Fe is one of the least mobile elements during chemical weathering creating the potential for soil iron concentrations to increase with increasing weathering intensity. This is consistent with the elevated Fe concentrations in the city soil probably reflecting a higher degree of chemical weathering, caused by a longer exposure, than the suburban soils. The iron isotopic composition of the city soil with the average δ56Fe value = 0.16‰ is within the range of values reported for granite reference materials (0.13 ± 0.12‰, [51]).Clear iron isotopic variability within soil fractions is consistent with chemical weathering being the dominant driver of iron cycling in the soil. Iron isotopic composition of the F3 and F4 fractions resemble findings of previous studies [52, 53] attributing such variations to kinetic fractionation as a result of chemical weathering. The composition of leaching solutions used here for F1 and F2 soil fractions are different from those used in separation schemes designed specifically for Fe [54], which makes it difficult to compare the patterns. However, as mentioned in the previous section, redox processes may strongly fractionate iron (δ56FeII-III = −3‰ [55]). It is possible that the Fe isotopic fractionation between the F1 and F2 fractions in the upper 30 cm and lower 30 cm reflects a soil redox change with the lower (deeper?) soils being enriched in Fe2+.(6) Lead. Lead concentrations display the classic pattern expected for anthropogenic pollutant in soils. In deeper soil layers (depths >30 cm), Pb concentrations are constant at both locations. In the city location, there is a significant increase in Pb concentrations in the upper soil layers while Pb concentrations are constant at the surburb location. The excess Pb in the upper most city soil also has a significantly different Pb isotope composition than the geologic Pb in the region.The isotopic composition of the Pb pool in the suburban samples is within the range of agricultural soils reported for northern Sweden [56]. The upper soil horizons from the city soil contain Pb with a significantly less radiogenic value. Back calculating the isotopic composition of this excess Pb (assuming end-member mixing) provides a value near that found in modern lichen 206Pb/207Pb = 1.14 and 208Pb/207Pb = 2.38 (Table 9) [57]. All the bioindicators studied here have a significantly less radiogenic isotopic composition than the presumed natural Pb baseline in deep soil horizons.The absence of increased Pb in the suburban samples suggests that pollution is more local than what might be expected based on other locations in northern Sweden [58], and it might be explained by the relatively short time interval since the area emerged from the sea. The existence of various local pollution sources also appears to be evident in the wide spread of Pb isotopic ratios found in birch leaves and pine needles around Luleå.Moving away from using Pb as a pollution tracer, the selective extractions also highlight that the influence preferential mineral weathering can have on the isotopic compositions of Pb pools within soils. The residual fraction F6 (HF digestion) of the SEP used in the present study contains a uniform Pb concentration at all locations and depths with significantly less radiogenic Pb isotopic composition than in other fractions (Table9). Similarly, in a study of sediments from 31 lakes in Sweden [59], lower 206Pb/207Pb ratios were found in samples prepared using HF digestion compared to those treated using HNO3 + HClO4 (10 : 1 v/v). This was attributed to the Pb contribution from feldspars, which are more resistant to chemical weathering than most other minerals. In the present study, potassium feldspar is the main Pb carrier in the silicate soil fractions [60]. The majority of radiogenic Pb, formed in silicates by 238U, 235U, or 232Th decay, might be efficiently leached in the first five SEP fractions. This leaves the final HF fractionation with a less radiogenic isotope composition reflecting those for the time of mineral formation approximately 2 Ga years ago.(7) Strontium. Total Sr concentrations display little variability across the dataset (Table 10). Top soils have slightly lower Sr concentrations, as for Cr most likely reflecting dilution effects by organic matter. The majority of Sr is found in the residual fractions (F5-F6), suggesting most of the element is bound in refractory mineral phases within the soil.Mean87Sr/86Sr ratios in all environmental matrices from Luleå fall into a relatively narrow range (0.729–0.734) with little differences in isotopic composition between soil and bioindicators. Thus, unlike B, Sr in needles, leaves, and lichens appears to be of a terrestrial rather than marine origin; seawater aerosols have less radiogenic Sr isotope ratios [61]. To a significant degree, the homogeneity of the 87Sr/86Sr ratios is expected given the composition of the local bedrock [60, 62].Strontium isotopic ratios, primary variations in radiogenic87Sr abundance, have been extensively used for authentication and provenance studies [4]. Waters, crops, livestock, a variety of food products and ultimately man are known to reflect the Sr isotopic ratios typical for the geological setting in which they occur [63]. Strontium isotopic systematics has been also used, in combination with other systems, to trace anthropogenic sources in the environment [10, 11, 64].(8) Thallium. Total Tl concentrations in soils from city and suburban locations vary over a very limited range of approximately 0.4–0.6 µg·g−1 at all depths (Table 11). Thallium predominantly resides in the residual fractions (98% of Tl recovered in leachates F5-F6) most likely in the crystalline structure of silicate minerals such as potassium feldspar and quartz [65]. Concentration of the remaining Tl fractions, associated with reducible and oxidizable phases, is significantly higher in top soil from the city than that in the suburb. Our findings reaffirm previously reported Tl speciation data for rhizospheric soils [66].There is very limited data on Tl isotopes in environmental samples if compared to other more “traditionally” studied isotopic systems. Tl isotopic ratio data from contaminated soils have been reported in literature with aδ205Tl value of ≈ −0.3‰ relative to the natural background, with average Tl concentrations of 0.75 µg·g−1 [67]. The same study reported a lighter Tl signature with increasing soil depth in both the extractable and the residual fractions which is similar to our findings (Table 11).F1 and F2 soil fractions have positiveδ205Tl values. This heavier signature is then can be traced in significantly higher δ205Tl found in lysimetric waters, which in turn may contribute to the heavier Tl ratios found in mushrooms, needles, and leaves (Table 11).(9) Zinc. Zinc concentrations follow a similar pattern as for Pb. The top soil layers from the city are significantly enriched in Zn while deeper soil horizons are characterized by more uniform concentrations (Table 12). The majority of Zn was found in the first four fractions (80–90% leached in F1−F4), suggesting that source of anthropogenic Zn, like Pb, contains the element in a readily mobile form. Isotopic composition patterns for Zn and Pb show little similarities.The deep soil layers (46–60 cm) have Zn isotopic compositions consistent with that of the local bedrock (−0.05–1.5‰; converted from the “Lyon” JMC 3–0749 L standard) [47]. The soil horizons with the highest Zn concentrations seem to be slightly enriched in the light isotopes of Zn, but the trend is not overly convincing. Previous studies reported that exogenous dust deposition does cause measurable shift in soils Zn isotopic composition [68] which otherwise is relatively constant [30] for less contaminated soils. This suggests that the source of anthropogenic Zn has a Zn isotope composition very close to the local bedrock. Previously, Zn fractionation in soil horizons was attributed to sorption onto the Fe oxyhydroxides [47].The meanδ66Zn of top soils and lysimetric waters is approximately +0.2‰, while a significantly higher value of +0.6‰ was found in mushrooms indicating preferential uptake of heavier isotopes. The mechanism(s) of uptake of heavy metal ions by fungi can be via either an active or passive [69], and the prevailing heavier Zn signature in mushrooms compared to the soil pool suggests an active uptake strategy. On the contrary, Zn in needles and leaves is isotopically lighter most likely as a result of fractionation processes during Zn translocation through the shoot [70], favoring lighter isotopes.


## 3.1.1. Multielement Patterns

(1) Batch-Type Leach Water and Lysimeritc Waters. The batch-type water leaches (fraction F1) and lysimetric waters have similar elemental concentrations, with the exception of Cu, Pb, and Zn, (assuming an average water to soil mass ratio of 1 : 10 for the F1 fraction). The concentrations of the latter analytes are several orders of magnitude lower in lysimetric waters than in the F1 fraction. Most of the isotopic compositions of the elements follow a similar pattern. Isotopic ratios of radiogenic elements (Pb and Sr) in the F1 fractions from upper soil layers overlap the compositions of lysimetric waters. The differences in the isotopic compositions of B, Cd, and Fe between these two matrices are also very minor. However, lysimetric waters were found to be preferentially enriched in the heavy isotopes of Cr, Cu, and Zn relative to the batch-type leach waters.The overall isotopic and elemental pattern is most readily explained as the product of exchange between rainwater and soil particles. In natural systems, weakly sorbed elements such as Cu and Pb likely undergo reversible sorption and their retention is strongly depended on meteoric percolation dynamics.At least for Cu and Zn, this portioning/sorption process induces stable isotope fractionation [32].(2) Biologic Samples. Comparing the compositions of the biologic samples, i.e., lichen, mushrooms, and vascular plant tissue, from the same location can help differentiate biochemical variability from geochemical variability. Lichens do not contain roots, and therefore, their composition is expected to provide information on aerial (precipitation, sea aerosols, and long range pollution) sources of elements [33]. Unlike lichens, fruit bodies of mushrooms and vascular plant tissue are much less affected by direct contribution from airborne sources, both because of very short duration of exposure and significantly lower surface area/volume ratio.For many elements (Cd, Cu, Fe, Pb, and Zn), lichens display a significantly narrower range of isotopic variability than mushrooms, leaves, and needles. This is probably a reflection of the isotopically homogenous nature of Aeolian inputs combined with limited biologic fractionation of stable isotopes within lichen [16, 34, 35]. Lichens have significantly higher concentrations of Cr, Pb, and Tl and lower concentrations of B and Sr relative to leaves and needles. This indicates that atmospheric pollution is a significant source for heavy metals in the region relative to potential geologic sources.The mushrooms are not only accumulating Cd, Cu, and Zn relative to the water-leachable element fraction of soils, but, with the exception of Cd, the isotopic composition of these metals also differs between the mushrooms and lysimeric waters and/or the local soil. The most likely explanation of this isotopic fractionation is the active uptake of heavy metals by siderophilic root exudates. Lithophilic and chalcophilic elements (B, Cd, Pb, Sr, and Tl) do not appear to be significantly fractionated by mushrooms. The mushrooms’ ability to accumulate Cd without inducing isotopic fraction may indicate an alternative biochemical mechanism for element uptake in mushrooms.It is difficult to identify any clear patterns in the leaf and needle data (Tables4–12). This may be a result of the far greater biochemical complexities of higher plants causing a much wider spread of interspecies and intertree isotopic variability. The litter layer was sampled to study potential isotopic shift related to nutrient reabsorption back into tree during late stages of senescence [36]. However, preliminary analysis of Fe and Pb concentration data demonstrate that the litter had become significantly contaminated by soil particles. The isotope signature of leaves in late stage of development therefore overlapped with the isotopic composition of the top soils.


## 3.1.2. Single-Element Patterns

(1) Boron. Total B concentrations in the soil profile decrease with depth in the city samples, but not in the suburban samples (Table 4). Between 80% and 95% of the total B content was associated with the refractory phases (F5-F6) consistent with mineral bound B being the main source of B in the soils [37]. Secondary mineral formation is associated with the preferential incorporation of 10B into the secondary minerals [38] resulting in a heavier residual B composition in solution. This process appears to be the best explanation of the composition of the lysimetric waters in the present study (δ11Bwater-soil ≈ +11‰). The B isotopic composition of the mobile fraction trends towards a heavier signature in the upper soil layers, probably reflecting input from vegetation with plant biomass having distinctly heavier values (δ11Bleaves/needles-soil ≈ +20‰).There is a notable trend towards heavier B isotopic signatures in the direction soil < plants < lichens with soil consistently characterized by negativeδ-values and plant materials always having positive δ11B. Boron is not thought to be strongly fractionated by biological activity [39]; thus, this trend can, at least partially, also be explained by source mixing. The isotopic composition of the lichens (mean value of +32% for δ11B) will be affected by aerial marine aerosols with δ11B of about +40% [40], and the influence from this source could also explain the isotopic composition of leaves and needles in coastal regions. The total span of δ11B values for our samples vary by around 64‰ (Table 4), corresponding to almost half of the published span of δ11B values [41]. More interestingly, the results for our bioindicator samples (mushrooms, needles, leaves, and lichens) show similar variability to coffee beans collected from vastly different geographic areas [8, 42] (Table 4). Overall, the B isotope systems appear to have characteristics which favor its use as an abiotic tracer of source mixing.(2) Cadmium. The soil in the city locations contained significantly more Cd than the suburban location (Table 5). Such concentration difference is more pronounced in the surface soil layers compared to deeper profiles. For example, the upper most layers of the city soil profiles contain, on average, about 10 times the concentration found in the deepest inorganic layer. The major part of Cd is present in relatively mobile phases as about 70% of the total soil Cd was found in fractions (F1-F2-F3-F4). The reducible fraction (F3) contains especially high concentrations of Cd. This pattern suggests an anthropogenic source of Cd in the urban soil samples, but Cd isotopes do not appear a reliable means of identifying the pollution source.Published variations ofδ114Cd values in rock and mineral samples do not exceed 1‰, excluding the extreme fractionation values published for extraterrestrial material [43]. This relatively narrow fractionation span (corresponding to 0.25‰ per mass unit) is small compared to light elements such as Li and B, reflecting less relative mass difference between Cd isotopes. The mass balanced soil Cd pool has an isotopic composition equal within measurement uncertainty to δ114Cd = 0‰ and the fractions with highest Cd concentrations do not have a distinct isotope signature. Cadmium isotopes do however appear to be influenced by biological activity.There are limited published data on the Cd isotope ratios of nongeologic material, while geologic matrixes display a narrow range of isotope compositions. The range inδ114Cd values found in the leaves from the studied area (almost 2‰, Table 5) by far exceeds the variability of the geologic samples and the soil and lysimetric waters in this study. Thus, significant Cd fractionation occurs during Cd uptake or incorporation into the leaves. Biologically mediated fractionation appears to be the best explanation of the heavier Cd isotopic composition in bioindicators [2, 21]. It has been proposed [44] that carrier-mediated transport plays a major role in the root uptake process for Zn, and such process, also defined high-affinity transport, has been associated to a preferential translocation of heavier isotopes. Preferential incorporation of the heavy isotopes could explain also the observed shift between soil and leave isotope signatures (average δ114Cdsoil-leaves ≈ −0.4‰), as confirmed in recent studies [45], as well as the negative δ114Cd for the residual/immobile Cd pool in the soils.(3) Chromium. There are minor differences in soil Cr concentrations between the sample locations (Table 6). Top soils have slightly lower Cr contents, which is probably due to dilution by Cr-poor organic material (offal). The mobile fractions contain only a minor share of the total Cr pool irrespective of location or depth; on average, 83–88% of the total Cr is associated with residual phases. Cr isotopic compositions are very homogenous with practically all ratios in soils being the same within the uncertainty of the method (Table 3).The Cr content of mushrooms, needles, and leaves was too low for accurate isotopic ratio measurements.δ53Cr values increased from soil-to-soil solution to lichens. Wet deposition could be the explanation for the heavy signature found for δ53Cr in lichens [46]. There is a positive correlation between Cr concentrations and increasing proximity to chromite processing steelworks and a negative correlation between δ53Cr values and increasing proximity to the steelworks implicating the smelter as the primary airborne Cr contributor in the area.(4) Copper. Highest concentrations of Cu were found in the upper soil horizons from the city location and concentrations decrease with depth (Table 7). Similarly to Cd soil distribution, Cu is significantly less stratified in the suburb soil than in the soil from the city. However, Cu is bound in soils in a different pool than Cd. Most of the Cu in top soil resides in the oxidizable fraction (F4), generally associated with organic matter. The smallest Cu pool was found within the F3 fraction in all depths and at all sample locations. Hence, Cu is not associated with Mn and Fe-oxides in the soil profiles.The Cu isotopic ratios show no notable variations with soil depth. The Cu in the city soils has a heavy isotopic signature, while the suburban soil has aδ65Cu value of approximately −0.1‰. This is consistent with previously reported findings for soil systems affected by Cu from an anthropogenic source [47], affirming that Cu isotopes can be used an indicator of anthropogenic pollution.The biological samples have lighter Cu isotopic composition relative to the soil and lysimetric waters (Table7). A shift towards lighter δ65Cu in vegetation is consistent with the previous reports of Cu fractionation in plants (e.g., [48]), and a similar general pattern was reported for other nutrients [21, 49]. However, the fractionation may not be a sole result of a biomediated reaction. While reduction in the rhizosphere by organic exudates is associated with the fractionation of the bioavailable pools of Fe and Cu towards lighter values, a biotic reduction has the same effect at least for Fe [50].(5) Iron. The total concentrations of Fe in city soil samples are approximately twice than those found in the suburbs (Table 8). However, unlike Cu and Cd, Fe concentrations do not change significantly with depth, and the majority of Fe was bound on the F5 and F6 fractions thus associated with primary bedrock mineral phases. Fe is one of the least mobile elements during chemical weathering creating the potential for soil iron concentrations to increase with increasing weathering intensity. This is consistent with the elevated Fe concentrations in the city soil probably reflecting a higher degree of chemical weathering, caused by a longer exposure, than the suburban soils. The iron isotopic composition of the city soil with the average δ56Fe value = 0.16‰ is within the range of values reported for granite reference materials (0.13 ± 0.12‰, [51]).Clear iron isotopic variability within soil fractions is consistent with chemical weathering being the dominant driver of iron cycling in the soil. Iron isotopic composition of the F3 and F4 fractions resemble findings of previous studies [52, 53] attributing such variations to kinetic fractionation as a result of chemical weathering. The composition of leaching solutions used here for F1 and F2 soil fractions are different from those used in separation schemes designed specifically for Fe [54], which makes it difficult to compare the patterns. However, as mentioned in the previous section, redox processes may strongly fractionate iron (δ56FeII-III = −3‰ [55]). It is possible that the Fe isotopic fractionation between the F1 and F2 fractions in the upper 30 cm and lower 30 cm reflects a soil redox change with the lower (deeper?) soils being enriched in Fe2+.(6) Lead. Lead concentrations display the classic pattern expected for anthropogenic pollutant in soils. In deeper soil layers (depths >30 cm), Pb concentrations are constant at both locations. In the city location, there is a significant increase in Pb concentrations in the upper soil layers while Pb concentrations are constant at the surburb location. The excess Pb in the upper most city soil also has a significantly different Pb isotope composition than the geologic Pb in the region.The isotopic composition of the Pb pool in the suburban samples is within the range of agricultural soils reported for northern Sweden [56]. The upper soil horizons from the city soil contain Pb with a significantly less radiogenic value. Back calculating the isotopic composition of this excess Pb (assuming end-member mixing) provides a value near that found in modern lichen 206Pb/207Pb = 1.14 and 208Pb/207Pb = 2.38 (Table 9) [57]. All the bioindicators studied here have a significantly less radiogenic isotopic composition than the presumed natural Pb baseline in deep soil horizons.The absence of increased Pb in the suburban samples suggests that pollution is more local than what might be expected based on other locations in northern Sweden [58], and it might be explained by the relatively short time interval since the area emerged from the sea. The existence of various local pollution sources also appears to be evident in the wide spread of Pb isotopic ratios found in birch leaves and pine needles around Luleå.Moving away from using Pb as a pollution tracer, the selective extractions also highlight that the influence preferential mineral weathering can have on the isotopic compositions of Pb pools within soils. The residual fraction F6 (HF digestion) of the SEP used in the present study contains a uniform Pb concentration at all locations and depths with significantly less radiogenic Pb isotopic composition than in other fractions (Table9). Similarly, in a study of sediments from 31 lakes in Sweden [59], lower 206Pb/207Pb ratios were found in samples prepared using HF digestion compared to those treated using HNO3 + HClO4 (10 : 1 v/v). This was attributed to the Pb contribution from feldspars, which are more resistant to chemical weathering than most other minerals. In the present study, potassium feldspar is the main Pb carrier in the silicate soil fractions [60]. The majority of radiogenic Pb, formed in silicates by 238U, 235U, or 232Th decay, might be efficiently leached in the first five SEP fractions. This leaves the final HF fractionation with a less radiogenic isotope composition reflecting those for the time of mineral formation approximately 2 Ga years ago.(7) Strontium. Total Sr concentrations display little variability across the dataset (Table 10). Top soils have slightly lower Sr concentrations, as for Cr most likely reflecting dilution effects by organic matter. The majority of Sr is found in the residual fractions (F5-F6), suggesting most of the element is bound in refractory mineral phases within the soil.Mean87Sr/86Sr ratios in all environmental matrices from Luleå fall into a relatively narrow range (0.729–0.734) with little differences in isotopic composition between soil and bioindicators. Thus, unlike B, Sr in needles, leaves, and lichens appears to be of a terrestrial rather than marine origin; seawater aerosols have less radiogenic Sr isotope ratios [61]. To a significant degree, the homogeneity of the 87Sr/86Sr ratios is expected given the composition of the local bedrock [60, 62].Strontium isotopic ratios, primary variations in radiogenic87Sr abundance, have been extensively used for authentication and provenance studies [4]. Waters, crops, livestock, a variety of food products and ultimately man are known to reflect the Sr isotopic ratios typical for the geological setting in which they occur [63]. Strontium isotopic systematics has been also used, in combination with other systems, to trace anthropogenic sources in the environment [10, 11, 64].(8) Thallium. Total Tl concentrations in soils from city and suburban locations vary over a very limited range of approximately 0.4–0.6 µg·g−1 at all depths (Table 11). Thallium predominantly resides in the residual fractions (98% of Tl recovered in leachates F5-F6) most likely in the crystalline structure of silicate minerals such as potassium feldspar and quartz [65]. Concentration of the remaining Tl fractions, associated with reducible and oxidizable phases, is significantly higher in top soil from the city than that in the suburb. Our findings reaffirm previously reported Tl speciation data for rhizospheric soils [66].There is very limited data on Tl isotopes in environmental samples if compared to other more “traditionally” studied isotopic systems. Tl isotopic ratio data from contaminated soils have been reported in literature with aδ205Tl value of ≈ −0.3‰ relative to the natural background, with average Tl concentrations of 0.75 µg·g−1 [67]. The same study reported a lighter Tl signature with increasing soil depth in both the extractable and the residual fractions which is similar to our findings (Table 11).F1 and F2 soil fractions have positiveδ205Tl values. This heavier signature is then can be traced in significantly higher δ205Tl found in lysimetric waters, which in turn may contribute to the heavier Tl ratios found in mushrooms, needles, and leaves (Table 11).(9) Zinc. Zinc concentrations follow a similar pattern as for Pb. The top soil layers from the city are significantly enriched in Zn while deeper soil horizons are characterized by more uniform concentrations (Table 12). The majority of Zn was found in the first four fractions (80–90% leached in F1−F4), suggesting that source of anthropogenic Zn, like Pb, contains the element in a readily mobile form. Isotopic composition patterns for Zn and Pb show little similarities.The deep soil layers (46–60 cm) have Zn isotopic compositions consistent with that of the local bedrock (−0.05–1.5‰; converted from the “Lyon” JMC 3–0749 L standard) [47]. The soil horizons with the highest Zn concentrations seem to be slightly enriched in the light isotopes of Zn, but the trend is not overly convincing. Previous studies reported that exogenous dust deposition does cause measurable shift in soils Zn isotopic composition [68] which otherwise is relatively constant [30] for less contaminated soils. This suggests that the source of anthropogenic Zn has a Zn isotope composition very close to the local bedrock. Previously, Zn fractionation in soil horizons was attributed to sorption onto the Fe oxyhydroxides [47].The meanδ66Zn of top soils and lysimetric waters is approximately +0.2‰, while a significantly higher value of +0.6‰ was found in mushrooms indicating preferential uptake of heavier isotopes. The mechanism(s) of uptake of heavy metal ions by fungi can be via either an active or passive [69], and the prevailing heavier Zn signature in mushrooms compared to the soil pool suggests an active uptake strategy. On the contrary, Zn in needles and leaves is isotopically lighter most likely as a result of fractionation processes during Zn translocation through the shoot [70], favoring lighter isotopes.


## 3.2. Landfills and Industrial Wastes

Pollution source tracing using isotopic data can be challenging for a number of reasons:(i)
The composition of potential sources is seldom represented by isotopically well-defined end members(ii)
The isotopic signature of potential sources may overlap natural isotopic variability(iii)
Even where end-member compositions are distinct and well-constrained, there might be a large number of potential sources(iv)
For stable isotopes, numerous postdeposition fractionating processes may alter the original ratios (see, e.g., [4])In order to demonstrate the severity of these complicating factors, concentration and isotopic data for waste samples from local industries (Cu slag, Fe slag, and fly ash) and two heavily contaminated soils (landfills) were obtained (Table13). These waste samples are very likely to be a major contributor to the landfills, and the goal of the exercise was to attempt identification of the presence of the industrial waste materials in the landfill using concentration patterns and isotopic fingerprints.Table 13
Concentration and isotopic data for two contaminated soils (landfill A and landfill B) and waste samples from local industries (Fe, Cu slag, and fly ash).
Cd,µg·g−1
δ
114Cd
Cr,µg·g−1
δ
53Cr
Cu,µg·g−1
δ
63Cu
Fe, %
δ
56Fe
Zn,µg·g−1
δ
66Zn
Pb,µg·g−1
206Pb/207Pb
Landfill A
1.5
0.0
450
0.2
2700
−1.0
15
0.4
1100
1.4
40
1.32
Landfill B
0.6
−1.5
2600
0.1
170
−1.4
10
1.0
180
−0.2
170
1.17
Fe slag
0.2
0.1
4100
0.1
100
0.7
12
0.9
150
−0.7
250
1.16
Cu slag
11
−0.2
650
0.1
16000
0.1
35
0.4
12000
0.0
200
1.17
Fly ash
1.1
1.7
50
0.2
25
0.3
2.7
0.2
50
0.6
15
1.21Both landfills are high in Cd with Cd concentrations at least 10 times higher than those found in the soil from the suburb location. The Cd in landfill A is relatively unfractionated which may point towards Cu slag as the most likely source of the element as Cd found in Cu slag has an isotopic composition undistinguishable from the mean for top soils. Fly ash, on the contrary, is significantly enriched in heavier Cd isotopes. Copper slag is also significantly enriched in Cu, Zn, and Fe relative to the other pollution sources so these elements would be expected to be enriched in landfill A if Cu slag was indeed the source of Cd. This fits very well with the concentrations measurements of landfill A (Table13). This raises the question of why the Zn and Cu isotopic compositions of landfill A are nothing like the Zn and Cu isotopic compositions of Cu slag.Based on the overall elemental concentrations of Zn and Cu in landfill A, it is hard to imagine that source mixing can account for the isotopic offset between the slag and the landfill. This is because it would take an enormous quantity of these elements from a highly fractionated source to attain the isotope composition of the landfill if there is really slag present in the landfill. Alternatively, post depositional processes might significantly alter the isotopic composition of landfill, though this contradicts by the observed lack of fractionation of Fe isotopes in landfill A. The Fe isotope compositions of landfill A and Cu slag are identical, and most processes which heavily fractionate Cu and Zn isotopes would also be expected to fractionate Fe isotopes.The picture is not clarified by the evaluation of landfill B. Landfill B has a number of characteristics pointing towards Fe slag being the primary source of contamination with fly ash being a second significant source of contaminants. The Fe, Zn, Cu, Cr, and Cd concentrations and Cr, Fe, and Zn isotope compositions of landfill B are consistent with Fe slag mixed with some fly ash. At the same time, the Cu and Cd isotopic composition of landfill B requires an alternative explanation. It is possible that Cu isotopes are just not a reliable tracer of pollution sources in these landfills, but it is harder to account for Cr and Zn isotopes. The systems appear reliable in one of the landfills but not in the other.Overall this case study highlights that pollution source mixing can be challenging, but the difficulty is proportional to the number of elements and isotopes measured. We cannot readily account for the behaviour of all the systems we measured, but a weight-of-evidence approach allows for the potential sources of pollution identified with some certainty. That is while any number of factors may complicate source tracing, they do not render the process total ineffective.


## 4. Conclusions

It is now technically feasible to rapidly analyze not only the trace metal composition of a broad range of the environmental samples but also the isotope compositions of all the metals. Expanding the number of elements utilized in isotope tracing provides a powerful way to decipher sources and fate of environmental exposure by adding degrees of freedom to the process. However, it also becomes increasingly complex to interpret large multielement data set. All the samples in this study were collected from spatially limited area, but a number of the analytes still displayed a significant range of concentration and isotopic values. As expected, the different elements also appear to be responding to different drivers such that for any given question, measuring more elements does not result in better/clearer answers. This highlights the need to simultaneously advance our understanding of single-element systems while progressing the technical capabilities required to measure more elements in more matrices. Natural variability, which often far exceeds the intermediate precision of the analytical method, needs to be considered when interpreting results of environmental studies.



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*Source: 7408767-2018-12-16.xml*