Fate of Cd in Agricultural Soils: A Stable Isotope Approach to

Article Cite This: Environ. Sci. Technol. 2018, 52, 1919−1928

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Fate of Cd in Agricultural Soils: A Stable Isotope Approach to Anthropogenic Impact, Soil Formation, and Soil-Plant Cycling Martin Imseng,† Matthias Wiggenhauser,‡ Armin Keller,§ Michael Müller,§ Mark Rehkam ̈ per,∥ ∥ ∥ ‡ ⊥ Katy Murphy, Katharina Kreissig, Emmanuel Frossard, Wolfgang Wilcke, and Moritz Bigalke*,† †

Institute of Geography, University of Bern, Hallerstrasse 12, CH-3012 Bern, Switzerland Institute of Agricultural Sciences, ETH Zurich, Eschikon 33, CH-8315 Lindau, Switzerland § Swiss Soil Monitoring Network (NABO), Agroscope, Reckenholzstrasse 191, CH-8046 Zürich, Switzerland ∥ Department of Earth Science & Engineering, Imperial College London, SW7 2AZ London, U.K. ⊥ Institute of Geography and Geoecology, Karlsruhe Institute of Technology (KIT), Reinhard-Baumeister-Platz 1, 76131 Karlsruhe, Germany

Environ. Sci. Technol. 2018.52:1919-1928. Downloaded from pubs.acs.org by UNIV OF LOUISIANA AT LAFAYETTE on 01/27/19. For personal use only.

‡

S Supporting Information *

ABSTRACT: The application of mineral phosphate (P) fertilizers leads to an unintended Cd input into agricultural systems, which might affect soil fertility and quality of crops. The Cd fluxes at three arable sites in Switzerland were determined by a detailed analysis of all inputs (atmospheric deposition, mineral P fertilizers, manure, and weathering) and outputs (seepage water, wheat and barley harvest) during one hydrological year. The most important inputs were mineral P fertilizers (0.49 to 0.57 g Cd ha−1 yr−1) and manure (0.20 to 0.91 g Cd ha−1 yr−1). Mass balances revealed net Cd losses for cultivation of wheat (−0.01 to −0.49 g Cd ha−1 yr−1) but net accumulations for that of barley (+0.18 to +0.71 g Cd ha−1 yr−1). To trace Cd sources and redistribution processes in the soils, we used natural variations in the Cd stable isotope compositions. Cadmium in seepage water (δ114/110Cd = 0.39 to 0.79‰) and plant harvest (0.27 to 0.94‰) was isotopically heavier than in soil (−0.21 to 0.14‰). Consequently, parent material weathering shifted bulk soil isotope compositions to lighter signals following a Rayleigh fractionation process (ε ≈ 0.16). Furthermore, soilplant cycling extracted isotopically heavy Cd from the subsoil and moved it to the topsoil. These long-term processes and not anthropogenic inputs determined the Cd distribution in our soils.

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activities, but also from anthropogenic emissions.7 Anthropogenic Cd emissions have been strongly correlated with both air Cd concentrations and atmospheric Cd deposition rates to terrestrial surfaces.8 Moreover, a strong correlation between industrial Cd uses and environmental Cd concentrations was revealed by peat cores.7,9 In industry, Cd is used in Ni−Cd batteries, pigments, coatings, and in stabilizers for plastic and nonferrous alloys.10 In Europe, total industrial Cd emissions peaked in the 1960s and decreased thereafter.8 Cd is additionally added to agriculturally used soils through mineral P fertilizers, manure, and sewage sludge application. These fertilizers were increasingly applied during the 20th century, after the intensification of agricultural practices.11 As a result, Cd inputs to agricultural soils increased.12,13 In mineral P fertilizers, Cd concentrations vary and reflect different Cd

INTRODUCTION The application of mineral phosphate (P) fertilizers leads to an unintended Cd input into agricultural soils. This Cd can be stored in the soil, leached with seepage water, or taken up by crops and thus enter the human food chain.1 However, Cd is toxic for plants and humans and accumulates in human bodies.2 Even low Cd concentrations in edible plant parts can pose a risk for human health because its biological half-life is 10−30 years.3 Cd is a natural constituent of soil parent material, which is physically and chemically weathered during soil formation. In crustal rocks, Cd concentrations vary between 0.01 and 2.6 mg kg−1, with typically higher abundances in sedimentary than in igneous rocks.4 Weathering of parent material depends on the soil forming factors5 and is quantitatively the most important natural Cd source to soils. Typical Cd concentrations in uncontaminated soils range from 0.1 to 1.0 mg kg−1.6 Another Cd source to soils is atmospheric deposition. Cd in the atmosphere can originate from natural sources like local transport of particles, long-range transport of dust, and volcanic © 2018 American Chemical Society

Received: Revised: Accepted: Published: 1919

October 25, 2017 December 15, 2017 January 8, 2018 January 8, 2018 DOI: 10.1021/acs.est.7b05439 Environ. Sci. Technol. 2018, 52, 1919−1928

Article

Environmental Science & Technology

Figure 1. Cadmium abundance and stable isotope mass balances of the three arable soils at OE (a), WI (b), and NE (c) for one hydrological year (May 2014−May 2015). Mass balances were calculated for wheat (I) and barley cultivation (II). System inputs are shown in red; system losses are shown in green. Sizes of the boxes are proportional to the size of Cd fluxes (compared to the reference box for 1 g Cd ha−1 yr−1). Sizes of the bulk soil boxes had to be reduced and would be 100× (OE), 50× (WI), and 500× (NE) bigger to proportionally represent real values. Net losses and net accumulations represent the mass balance values after one hydrological year for the two crops. Calculated δ114/110Cd values of inputs, outputs, and bulk soil (0−50 cm) are shown next to the boxes. The bulk soil Cd isotope compositions after 100 hydrological years were calculated with current fluxes (current)* and with maximal inputs through atmospheric deposition, mineral P fertilizers, and manure (max)** during the 100 year model.

concentrations in rock phosphates.14 Imports of such fertilizers to Switzerland peaked in 1980 and decreased afterward by a factor of ∼4 until 2008.15 Still, Cd inputs through mineral P fertilizers are a relevant soil pollution pathway, depending on the Cd concentrations and application rates.12,16,17 In manure, Cd is less concentrated than in mineral P fertilizers and reflects the Cd concentrations of the animal diet, including crops, pasture grasses and herbs, and feed additives.18,19 However, high manure application rates can also considerably increase Cd inputs to soils.20−22 Sewage sludge is an additional relevant Cd source, and Cd concentrations depend on its origin and quality. Sewage sludge application to agricultural soils was prohibited in Switzerland in 2006; nevertheless, earlier applications might have contributed considerably to the present Cd stock of agricultural soils. The most important Cd outputs from arable soils are with seepage water and crop harvest. First, the output with seepage water is determined by the Cd concentration and the amount

of water. Soil solution Cd concentrations are primarily controlled by sorption processes.6 The pH of the soil is thereby the main factor determining soil solution Cd concentrations, followed by the bulk soil Cd concentration.5,23,24 The amount of seepage water depends on the water balance of a soil (precipitation, evapotranspiration, and change in soil water content). Previous studies assumed constant Cd leaching fluxes25,26 or calculated them based on laboratory adsorption experiments and meteorological data.27 In contrast, this study presents, to our knowledge, the first Cd leaching fluxes calculated with in situ measured water flux data. Second, output with crop harvest is controlled by crop Cd concentrations,19,26,27 which vary because of the different acquisition and sequestration strategies of plants.6,18,19 It has been shown that the most important driver of Cd concentrations in plants is the soil Cd concentration, followed by soil pH.6 1920

DOI: 10.1021/acs.est.7b05439 Environ. Sci. Technol. 2018, 52, 1919−1928


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In soils, Cd derives partly from geogenic sources and partly from anthropogenic inputs of the past. Hence, tools are needed to better distinguish between these different sources. A wellestablished biogeochemical tool for tracing metal contaminants in the environment is the stable isotope composition.28 The δ114/110Cd values of terrestrial rocks and minerals show only limited variability (−0.4 and 0.4‰).29−32 In contrast, industrial processes can generate substantially larger Cd isotopic fractionations (−2.3 to 5.8‰),30,33,34 mainly through partial evaporation and condensation of the metal.30,33,34,35 Notably, soils and sediments near smelters are commonly enriched in anthropogenic Cd. In such environments, stable isotopes have been used to differentiate between anthropogenic and geogenic Cd.34,36−38 Moreover, despite smaller isotopic variabilities, a recent study successfully used stable isotopes to trace Cd from mineral P fertilizers in agricultural soils.39 Besides different sources, natural processes can also produce pronounced variations in Cd isotope compositions of agricultural soils. First, processes between solid-phases and liquid-phases lead to the enrichment of heavy isotopes in solutions. For example, after natural weathering, river sediments were more enriched in heavy isotopes than riverbank soil (Δ114/110Cdsoil‑stream sediment ≥ −0.50‰).40 Similarly, after simulated weathering, Cd in leachates was isotopically heavier than Cd in Pb−Zn ores (Δ114/110CdPb−Zn ore‑leachate = −0.53 to −0.36‰).40 Other studies examined Cd isotopic fractionation during Cd adsorption to Mn oxyhydroxides and Cd coprecipitation with calcite.41,42 In both cases, the dissolved Cd was isotopically heavier than the adsorbed Cd (Δ 114/110 Cd solid−liquid = −0.54 to −0.24‰) 41 and the coprecipitated Cd (Δ114/110CdCaCO3‑Cd(aq) ≈ −0.45‰).42 Second, biological processes also cause isotopic Cd fractionation. For example, phytoplankton preferentially take up light Cd isotopes,43 leaving residual seawater Cd that isotopically heavier (∼0 to 3.8‰).44 Similarly, Cd-tolerant plants were more enriched in light isotopes than hydroponic solutions (Δ114/110Cdplant‑solution = −0.70 to −0.22‰).45 However, Cd in plants was isotopically heavier than Cd in bulk soils (Δ114/110Cdsoil‑wheat = −0.39 to −0.13).46 This might be an effect of the isotopically heavier Cd in liquid-phases compared to solid-phases,40−42 because plants mainly take up Cd from soil solutions. During the 20th century, the Cd concentrations of European soils have increased by a factor of 1.3 to 2.6.13 In contrast, models predict a reversal of this trend, such that Cd concentrations are expected to remain constant17 or even decrease13,47 in European soils over the next 100 years. However, mass balances based on in situ measured data are lacking. Furthermore, there is only one study which used stable isotopes to trace Cd sources in agricultural soils.39 Here, we used in situ measured data to establish Cd mass balances for three arable study sites. Soil Cd concentrations and all Cd inputs (atmospheric deposition, mineral P fertilizers, manure, and parent material) and outputs (seepage water, wheat and barley harvest) were determined during one hydrological year, from May 2014 to May 2015. In addition, a novel approach that uses Cd stable isotope compositions was applied to evaluate the importance of anthropogenic Cd inputs and to investigate Cd cycling in the soils. The aims were to: (i) determine if Cd accumulates in soils under current agricultural practices, (ii) differentiate between anthropogenic and natural Cd in the soil, and (iii) understand Cd redistribution processes within the soils.

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MATERIALS AND METHODS

See more details in the SI. Study Sites. The study was carried out at two arable monitoring sites (Figure S1) of the Swiss Soil Monitoring Network (NABO)48 in Oensingen (OE) and Wiedlisbach (WI), situated on the Swiss Plateau. In addition, one arable monitoring site was chosen from the cantonal soil monitoring network Basel-Landschaft in Nenzlingen (NE), located in the Swiss Jura. These three sites were selected because of contrasting geology, soil properties, and Cd concentrations in the soils. The lowest Cd concentrations were found at WI (0.13 to 0.17 mg kg−1), and the highest concentrations were found at NE (0.97 to 1.66 mg kg−1, Table S1). The soils developed on calcareous alluvial deposits (OE), mixed calcareous, siliceous moraine material (WI), and limestone (NE), respectively. At OE, the soil is classified as a Stagnic Calcaric Eutric Fluvic Cambisol, WI is classified as a Eutric Cambisol, and NE is classified as a Leptic Calcaric Eutric Cambisol. Sampling. Soil samples were taken from four fixed depths (0−20 cm, 20−50 cm, 50−75 cm, and >75 cm). Inputs and outputs (Figure 1) were sampled during one hydrological year between May 2014 and May 2015, and barley harvest samples were taken after that period, in July 2015. Soil parent material was obtained at each site. The C horizon was sampled at OE (240 to 270 cm depth) and WI (110 to 130 cm depth); at NE, limestone samples were collected from the soil surface. Mineral P fertilizers were obtained from the farmers for each application while liquid cattle manure was sampled once at OE and WI. No manure was sampled at NE, but formerly reported Cd concentration data were used for calculations.19 Atmospheric deposition and seepage water were sampled cumulatively every second week, while the volumetric water content of the soil was determined with 1-h resolution by time domain reflectometry at 50 cm soil depth. Plants were sampled during two cropping seasons (wheat harvest in summer 2014, barley harvest in summer 2015), with roots and shoots (aboveground plant material consisting of straw and grains) of plants harvested at full maturity. Laboratory Analyses. Basic soil properties including pH, cation-exchange capacity (CEC), texture, C, N, and S concentrations, and bulk density were determined, and the soils were characterized according to the World Reference Base for Soil Resources.49 Soil, parent material, plant, manure, and mineral fertilizer samples were digested using a microwave oven (ETHOS, MLS, Leutkirch, Germany). Cadmium concentrations were determined for the sample digests, atmospheric deposition, and seepage water by inductively-coupled mass spectrometry (ICP-MS, 7700x, Agilent Technology, Waldbronn, Germany). Titanium (Ti) concentrations were additionally measured in digests of soil and parent material samples to calculate Cd mass gains or losses per unit volume of soils relative to parent materials (τCd values, eqs S1 and S2).50 The stable Cd isotope compositions of all samples were determined (as described in detail in the SI) using a doublespike technique by multiple collector inductively coupled plasma mass spectrometry (MC-ICP-MS, Nu Plasma HR, Nu Instruments Ltd., Wrexam, UK).46,51,52 The total procedural Cd blank (n = 11) for the isotopic analyses ranged from 110 to 1011 pg. This was equivalent to less than 2.5% of the smallest indigenous Cd mass among the samples, while the typical blank proportion was about 0.4%. Hence, no blank corrections were required for the isotope data. Several standard reference 1921


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where ε is the Rayleigh fractionation factor for soil formation and f is the remaining Cd fraction in the soil, relative to the parent material (τCd values + 1). A soil-plant cycling model was used to test the hypothesis that trees, which formerly covered the agricultural soils,57−60 took up Cd from the deeper soil horizons and added it to the upper soil horizons, over the entire time of soil formation. First, the soils were subdivided into two layers (0−35 cm and 35−75 cm), and the remaining Cd fractions (τCd values + 1) and δ114/110Cd values were averaged for both layers (named as “current values in 2015”). Furthermore, the Cd surplus in the upper (0−35 cm) relative to the deeper horizon soil-layer (35− 75 cm), presumably cycled by trees, was calculated with the help of τCd values. This Cd surplus was divided by the age of the soils (13700 years) to obtain the annually cycled Cd. Afterward, the annually cycled Cd was subtracted from the upper and added to the deeper soil-layer, in 13700 steps, in the reverse direction as the trees did it before. Additionally, the Cd isotope composition change of the two soil-layers was calculated (eq 1), by subtracting the Cd isotope composition of the annually cycled Cd from the upper and adding it to the deeper soil-layer in 13700 annual steps. The isotope composition of the cycled Cd was thereby determined for each calculation step with Δ114/110Cdsoil‑trees = −0.25‰. After 13700 calculation steps, the remaining Cd fractions and δ114/110Cd values were averaged for the two soil-layers and named as “values 2015 without soil-plant cycling”. Error propagation was calculated according to eqs S6−S9.

materials (SRMs) were analyzed together with the samples for quality control, and the results showed good agreement with published values (Table S3). The double-spike method also yielded precise Cd concentrations.53 For the SRMs, the measured Cd concentrations were slightly lower than the certified values, but our data were in line with the results of other recent studies.54−56 The Cd isotope compositions of the samples were reported relative to the NIST 3108 Cd isotope reference material using a δ notation based on the 114Cd/110Cd ratio (eq S2). Two samples were considered significantly different in their isotope composition if the results differed by more than 2× the standard deviation of each sample. The Δ114/110Cd values, which denote the apparent isotopic fractionation between two reservoirs and/or two fluxes (e.g., between soil and seepage water), were calculated according eq S3. Mass Balance Calculations. Individual Cd abundance mass balances were calculated for each study site soil, considering inputs from weathering, atmospheric deposition, mineral P fertilizers, and manure, and outputs through seepage water and crop harvest (wheat and barley). Input from weathering was thereby calculated from dissolution of the coarse soil (>2 mm) which introduced Cd to the bulk soil. Separate mass balances for wheat and barley cultivation were calculated for each soil (Figure 1, Table S2). Additionally, stable isotope mass balances were calculated. The isotope composition of a mass balance reservoir or flux (input or output) was composed of several fractions (e.g., wheat harvest = straw harvest + grain harvest), and therefore the mean isotope composition had to be calculated. The mean value for each reservoir or flux was calculated with eq 1

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RESULTS AND DISCUSSION Cd Abundance Mass Balances. Input Fluxes. Cd input from weathering was only important at NE where it accounted for ∼17% of total Cd inputs; in contrast, this share was less than 1% at OE and WI (Figure 1, Table S2). The high Cd input from weathering at NE can be attributed first to the type of coarse soil (limestone), second to the high coarse soil volumetric content (5−9% for the two upper soil layers), and third to the high Cd concentrations in limestone (Table S1). At OE, weathering was relatively unimportant because the coarse soil volumetric content was below 0.5% (Table S1). At WI, the coarse soil volumetric content (>6%) was higher than at OE. Nevertheless, the Cd input with weathering was negligible for the mass balances. The reason for this was the siliceous parent material at WI for which weathering rates61,62 were 3 orders of magnitude smaller than those for calcareous material (at OE and NE).63 Comparable weathering rates were found by previous studies.61−63 The Cd input (0.11 ± 0.01 g ha−1 yr−1) from atmospheric deposition and the Cd concentration in atmospheric deposition (∼0.01 μg L−1) were similar among the three sites. This input contributed between 7 and 11% to the total Cd inputs. Based on air concentration measurements, Keller et al.19 estimated a median Cd atmospheric deposition rate of ∼0.7 g ha−1 yr−1 for Swiss soils in 2003, which is ∼7 times higher than the deposition rates found in this study. More recent studies reported lower rates between 0.2 and 0.4 g ha−1 yr−1.26,64 The difference between these estimates and our results most likely reflected the further reduction of anthropogenic Cd emissions in Europe in the past decade.8 In addition to this atmospheric deposition, there might be dry deposition, which we did not quantify and which is also not considered in the literature on arable soils.

n

δ

114/110

Cd =

∑ f = 1 δ114/110Cdf ·mC d f n

∑ f = 1 mCd f

(1)

where δ114/110Cd is the isotope composition of the reservoir or flux, δ114/110Cdf is the isotope composition of the fraction of the reservoir or flux, and mCdf is the Cd mass in the fraction of the reservoir or flux. The isotope mass balance for each study site was calculated with the same method, with arbitrarily defined mCdf > 0 for bulk soil and inputs, and mCdf < 0 for outputs: This yields new predicted δ114/110Cd values for the bulk soils. The budgeted unit was the 0−50 cm soil layer. To estimate long-term changes in bulk soil isotope compositions, the balances were extrapolated over 1 to 100 hydrological years, with alternating wheat and barley cultivation. Because Cd inputs from fertilizer use and atmospheric deposition might have been higher than today for a significant time period in the last century, an additional scenario was calculated. This assumed the highest possible Cd inputs for the last century and examined the impact on bulk soil isotope compositions. Error propagation was calculated for each step according to eqs S6-S9. Model Calculations. During soil formation, parent material was physically and chemically weathered, and isotopically heavy Cd was leached with seepage water. This Cd isotopic fractionation was described with the Rayleigh model (eq 2) and named as parent material weathering Δ110/114 Cd soil ‐ parent material = ε ln f

(2) 1922


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such regulation exists. Finally, the Cd accumulation in soils depends also on other properties of the agricultural system, like soil pH, which influences Cd output with seepage water, and manure application. Contributions of Natural and Anthropogenic Cd Sources to the Total Soil Cd. The Cd distribution in soils is the result of Cd inputs (weathering, atmospheric deposition, mineral P fertilizers, and manure) and Cd outputs (seepage water, crop harvest), as well as soil formation processes. Cd stable isotopes were used here as a tool to assess the importance of natural and anthropogenic Cd sources in the studied soils. The Cd isotope compositions of the inputs showed significant isotopic variation (δ114/110Cd = −0.15 to 0.38‰, Figure 2, Table S4). First, the parent materials differed in their

For all study sites, fertilization was quantitatively the most important Cd input. At OE and NE, Cd inputs from mineral P fertilizers were higher than inputs from manure, while the reverse was true for WI. The application of mineral P fertilizers accounted for 32% to 70% of total Cd inputs with fluxes of 0.75, 0.49, and 0.57 g ha−1 yr−1 for OE, WI, and NE, respectively. Similar input rates of 0.10 to 0.79 g ha−1 yr−1 were previously reported for other European soils.13,26,64 However, with the exception of one mineral P fertilizer that was applied at OE, the Cd concentrations of the mineral P fertilizers were found to be below the average value of 67 mg Cd (kg P)−1 determined for such fertilizers in Switzerland.65 Due to the highly variable Cd concentration of mineral P fertilizers (65% of total outputs. The reason for this was the seepage water concentrations which were highest at WI (0.156 μg L−1), followed by NE (0.011 μg L−1), and OE (0.003 μg L−1). The high Cd concentrations in seepage water at WI were related to the low pH. The Cd seepage water flux for this site agrees well with the literature (0.4 to 1.6 g ha−1 yr−1).26,27 For OE and NE, the crop harvest was a more important Cd output than leaching and accounted for more than 93% of the total Cd output at both sites and for both crops (wheat and barley). The higher the soil Cd concentration, the higher the output with crop harvest, with the highest observed at NE (1.77 and 0.57 g ha−1 yr−1 for the wheat and barley harvests, respectively) followed by OE (1.47 and 0.33 g ha−1 yr−1) and WI (0.52 and 0.33 g ha−1 yr−1). These results agreed well with the findings of previous studies concerning the coupling of soil Cd concentrations with crop Cd concentrations66−68 and crop Cd outputs.13,26,27 For all three sites, Cd abundances in wheat and Cd outputs with wheat harvest were higher than the respective values for barley. At WI, the Cd output difference between the harvesting of the two crops was smallest because barley provided a higher crop yield than wheat. Budget. The most influential driver for the soil Cd budgets was the crop species, because wheat and barley cultivation were associated with net Cd losses and net Cd accumulations, respectively, at all three sites (Figure 1, Table S2). Second, mineral P fertilizer Cd concentrations and application rates were other influential variables for the mass balances. The Scientific Committee on Toxicity, Ecotoxicity and the Environment (CSTEE) stated in 200269 that the application of mineral P fertilizers with Cd concentrations below 50 mg (kg P)−1 would most probably not lead to Cd accumulations in soils, which was supported by our findings. However, the use of fertilizers with higher Cd concentrations (these can be up to 213 mg (kg P)−1)65 will probably lead to Cd accumulations in soils (Figure S3). Thus, it is important to enforce the legal limit of 50 mg (kg P)−1 or introduce limits in countries where no

Figure 2. Cd isotope compositions of the inputs, outputs, and different depths of the bulk soils at the study sites OE (●), WI (▲), and NE (■). Mineral fertilizers are not site specific (⧫). Error bars represent 2 × standard deviations of sample replicates where n > 1 and measurement replicates where n = 1. Isotope values of wheat and barley harvest were calculated according to eq 1 and error propagation according to eqs S6−S9.

Cd isotope compositions, with the lowest δ114/110Cd values recorded at WI (−0.14 ± 0.10‰) and higher values at OE (0.04 ± 0.06‰) and NE (0.36 ± 0.04‰). The Cd isotope compositions of the bulk soils were not significantly different from the parent material at OE and WI. However, the soils at NE were isotopically lighter than the parent limestone. Second, the Cd isotope compositions of atmospheric deposition at OE and NE were not significantly different. Bridgestock et al.70 found that marine atmospheric aerosols from the Tropical Atlantic Ocean were characterized by a relatively narrow range of Cd isotope composition (−0.19 to 0.19‰), and they were unable to differentiate between anthropogenic and natural Cd sources. The Cd isotope composition of the atmospheric deposition analyzed here was not only within the range of industrial waste materials (−0.64 to 0.46‰)30,34,38 but also in 1923


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Figure 3. Relationships between the remaining Cd fraction in the soils (τCd values + 1) from the parent material (pm) and the apparent fractionation between the soils and parent materials (Δ114/110Cdsoil‑pm). a: values in 2015 for the 4 soil horizons and 3 sites; ε = 0.16. b: current values in 2015, averaged for the two layers of the soil-plant cycling model (0−35 cm and 35−75 cm); ε = 0.17. c: values in 2015 without soil-plant cycling; ε = 0.16.

important Cd output, which was associated with the wheat and barley harvest (straw and grains), was also enriched in heavy Cd isotopes (0.38 to 0.94‰) and agrees with the literature.46,71 Stable isotope mass balances (eq 1) offer us a tool to assess the importance of the different inputs and outputs on the Cd stock of the soils. For these calculations, we simplified our agricultural systems and assumed that they were anthropogenically influenced only during the last 100 years. First, atmospheric deposition of Cd is driven mainly by anthropogenic Cd emissions8 which have increased the Cd stock of soils since 1846.12 Thus, before industrialization, atmospheric deposition rates of Cd were lower than at present (2015) and can likely be neglected for most of the soil formation period. This is supported by a number of studies which found that Cd enrichment factors in peat cores were ∼20 times lower72 and Cd deposition rates at least 1 order of magnitude lower in preindustrial times compared to the last 20 years of the 20th century.73−76 Second, agricultural practices were intensified after World War 1,11 and this coincided with the use of mineral P fertilizers and concentrated animal food,15 which were associated with a net import of Cd to the agricultural systems. Before that time, the agricultural systems can be considered as closed. Thus, inputs from fertilization did not exceed outputs from harvest,77 and these outputs were by far lower than during the 20th century.11 The Cd isotope mass balances showed that δ114/110Cd values in the 0−50 cm layer of our soils will change by less than 0.03‰ during 100 years with current (2014−2015) agricultural practices and atmospheric deposition (Figure 1, Table S2). At OE, δ114/110Cd would change from 0.10 to 0.08‰, with alternating wheat and barley cultivation. At WI, the δ114/110Cd values will decrease from −0.18 to −0.21‰. The smallest influence of the different inputs and outputs on the bulk soil isotope composition will occur at NE with a decrease of 0.01‰ in 100 years. Furthermore, calculations on the maximal possible change for the Cd isotope composition of the bulk soils (0−50 cm) during the last century revealed changes of less than

accordance with data for aboveground plant material (0.20 to 0.57‰)46,71 which might emit organic aerosols and terrestrial minerals (−0.50 to 0.67‰).29,31 Thus, we were unable to identify the source of Cd in atmospheric deposition. However, a strong correlation between anthropogenic Cd emissions and atmospheric Cd deposition was shown by Pacyna et al.8 Third, the δ114/110Cd values of mineral P fertilizers (−0.15‰ to 0.15‰) were in the range of Earth crust minerals and rocks (−0.50 to 0.67‰).29−31 These results suggested that Cd was not fractionated during the manufacturing of mineral P fertilizers which is consistent with a recent work on mineral P fertilizers in New Zealand.39 Furthermore, the similar isotope ratios of bedrock and mineral fertilizers rendered it difficult to trace Cd from mineral P fertilizers in agricultural soils. This was different from the work of Salmanzadeh et al.,39 in which topsoils and phosphate fertilizers had clearly distinct Cd isotope compositions. Finally, the enrichment of heavy Cd isotopes in manure of OE and WI (0.35 to 0.38‰) was in line with the origin of the manure Cd. The cattle of the studied farms mainly fed on grass produced on the farm (either during grazing or as hay) and concentrated feedstuff (cereal grains). Pasture plants might show similar Cd fractionation patterns as wheat and barley, whose aboveground parts were enriched in heavy isotopes (0.38 to 0.94‰). Similar δ114/110Cd values have been found in wheat shoots and grains (0.20 to 0.57‰)46 and birch leaves (0.70‰).71 It is unknown, however, whether Cd isotopic fractionation occurs during digestion in the cattle rumen, but the small difference between the Cd isotope compositions of the manure and the plants suggested that any fractionation should be minor. Cd in outputs was isotopically heavier than Cd in bulk soils (Figure 2, Table S4). First, seepage water from all three sites was enriched in heavy isotopes (0.39 to 0.79‰). These results were in line with findings from simulated and natural weathering,40 Cd adsorption to Mn-oxyhydroxides41 and calcite precipitation42 studies in which the liquid-phase Cd was always isotopically heavier than the solid-phase Cd. Second, the most 1924


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Figure 4. Results of the soil-plant cycling model at Oensingen. The remaining Cd fractions ( f Cd = τCd + 1) and the isotope compositions of the two soil-layers (0−35 and 35−75 cm) in gray indicate values in 2015 and include soil-plant cycling over the entire soil formation period. Input parameters for the soil-plant cycling model (in green) were: The cycling time (i.e., age of the soil), Δ114/110Cdsoil‑trees, and the cycled Cd. The remaining Cd fractions and isotope compositions of the two soil-layers (0−35 and 35−75 cm) in red indicate values in 2015 if soil-plant cycling would not have occurred. Remaining Cd fractions are illustrated with red and gray shading, respectively, and δ114/110Cd values are indicated with dotted horizontal lines.

However, if only weathering and leaching influenced the Cd distribution in the bulk soils, the largest Cd losses and the lightest Cd isotope compositions should have been found in the oldest, uppermost horizons. The remaining Cd fractions in the soil, however, indicated an inverse distribution with apparently smaller losses of Cd in the upper than in the deeper horizons (Figures 3a). Thus, there must have been a process that added Cd to the surface soil. Interestingly, the Cd surplus in the upper relative to the deeper soil horizons correlated with the Cd concentrations of the parent materials (Figure S4). Therefore, the inverse distribution of the Cd depletion, indicated by the remaining Cd fractions in soils, was most likely caused by a Cd redistribution within the soils rather than a net external input. Previous studies have already revealed the importance of the plant pump for the distribution of nutrients78,79 and also for Cd between the C and O horizons.80−82 This pump may have also been important at our sites. To assess the importance of the plant pump, a soil-plant cycling model was introduced (Figures 4, S6, and S7). In the model, the soils were subdivided in two layers. Among all sites, the remaining Cd fractions and δ114/110Cd values in 2015, which included the plant pump effect, indicated more and isotopically heavier Cd in the upper (0−35 cm) than in the deeper (35−75 cm) soil-layer. Like for the four soil depths, we plotted the remaining Cd fractions and the Δ114/110Cdsoil‑parent material values of the two layers and fit the same Rayleigh fractionation model for soil formation (Figure 3b). In the next step, the soil-plant cycling model was applied to reckon back the effect of the plant pump. Without soil plant-cycling, less and isotopically lighter Cd was found in the upper (0−35 cm) than in the deeper (35− 75 cm) soil-layer, among all sites. This is exactly the Cd distribution which we would expect if parent material weathering were the dominating soil formation process and plants had not have cycled Cd. The remaining Cd fractions and Δ114/110Cdsoil‑parent material values were again plotted. The best fit of the Rayleigh fractionation model resulted thereby in a soil formation factor ε of 0.16, similarly to the situation with “current values in 2015”. Overall, the Cd distribution in our soils can be explained with two processes: (i) Parent material was physically and chemically weathered, and heavy Cd isotopes were leached

0.05‰ which is smaller than the measurement error. These calculations were based on: (i) The evolution of European Cd emissions,8 (ii) the Cd isotope compositions of industrial waste,30 (iii) Swiss mineral P fertilizer and feedstuff imports,15 and (iv) the Cd concentrations of mineral P fertilizers.65 These findings demonstrated that a much longer time scale is needed to produce significant changes in bulk soil Cd isotope compositions because known annual inputs and outputs are about 3 (OE and WI) to 4 (NE) orders of magnitude smaller than bulk soil Cd pools (0−50 cm). Therefore, not anthropogenic inputs and outputs but long-term fractionation processes during pedogenesis have controlled the Cd isotope compositions of the bulk soil. Consequently, the isotope compositions of our soils can be used to investigate long-term soil formation processes. Redistribution of Cd in the Soil. Looking at the predominant part of the soil formation period (13700 to 100 years B.P.), i.e. during preagricultural and preindustrial times, we can assume our soils to be semiclosed systems, in which Cd leaching with seepage water was the only output flux. The τCd values of our soils indicate (except for 0−20 cm at OE and WI) that 25−86% of the initial Cd in the parent material was lost, most likely with seepage water. Seepage water was more enriched in heavy isotopes than the soils (Δ114/110Cdsoil‑seepage water = −0.59 to −0.69‰). Consequently, bulk soil Cd isotope compositions shifted to lighter values relative to the parent material. Assuming that agricultural inputs/outputs and atmospheric deposition did not significantly influence the Cd isotope compositions of the bulk soils, as outlined above, the evolution of the bulk soil isotope compositions can be described with a Rayleigh fractionation model.28 To this end, the remaining Cd fractions and Δ114/110Cdsoil‑parent material values were plotted (Figure 3a). A best fit for the current soil data was thereby achieved with a Rayleigh fractionation factor (ε) of 0.16. At NE, we observed Δ114/110Cdsoil‑parent material between −0.22 and −0.32‰. At OE a n d W I , l e s s o f t h e in i t i a l C d w a s los t , an d Δ114/110Cdsoil‑parent material values were between −0.05 and 0.10‰. Consequently, the soil formation effect was well observable at NE with a better model fit than at the two other sites (Figure 3a). 1925


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of Bern for support in the laboratory and helpful discussions and Amy Deonarine for editing the manuscript.

with seepage water and shifted the bulk soil isotope compositions toward lighter values and (ii) plants simultaneously cycled heavy Cd from the deeper to the upper soil horizons and inverted the vertical Cd distribution and isotope compositions in the soils. Environmental Implications. The Cd mass balances revealed a balanced system with either net loss or net accumulation, depending on crop type grown and fertilizer Cd concentrations. Currently, Cd will not further accumulate in soils if legal limits of Cd in fertilizers are enforced. Isotope mass balances are a promising tool to estimate the anthropogenic share of Cd contamination in agricultural soils. For the three systems, the long-term natural parent material weathering and soil-plant cycling over ∼13700 years dominated over the recent decreasing anthropogenic impacts. These anthropogenic fluxes have become more important only during the last century, but annual fluxes with industry-induced atmospheric deposition, fertilizer applications, and crop harvests were still 3−4 orders of magnitude smaller than the soil Cd pools.

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ASSOCIATED CONTENT

S Supporting Information *

The Supporting Information is available free of charge on the ACS Publications website at DOI: 10.1021/acs.est.7b05439. Section 1: Detailed information on the materials and method. Figure S1: Map with locations of the study sites. Figure S2: Sampling at the study sites. Figure S3: Cd abundance mass balances as a function of the Cd concentration in mineral P fertilizers. Figure S4: Relationship between Cd surplus in the topsoils and Cd concentration in parent materials. Figure S5: Rayleigh fractionation model for soil formation after removal of the soil-plant cycling effect with alternative Δ114/110Cdsoil‑trees values. Figure S6: Soil-plant cycling model results for WI and NE. Table S1: Soil properties. Table S2: Calculated Cd abundance and stable isotope mass balances. Table S3: Standard reference materials. Table S4: Measured isotope compositions (PDF)

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REFERENCES

AUTHOR INFORMATION

Corresponding Author

*Phone: +41(0)316314055. E-mail: moritz.bigalke@giub. unibe.ch. ORCID

Armin Keller: 0000-0002-4977-4205 Moritz Bigalke: 0000-0002-6793-6159 Notes

The authors declare no competing financial interest.

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ACKNOWLEDGMENTS This study was funded by the Swiss Parliament via the National Research Program (NRP) 69 “Healthy Nutrition and Sustainable Food Production” (SNSF grant no. 406940_145195/1). We thank the farmers from the study sites for their cooperation, the FaBo of the canton BaselLandschaft for the information on the site NE, Lorenz Schwab for the characterization of soils, Barry Coles for help in the MAGIC laboratories, and the Plant Nutrition group at ETHZ for their support with plant digestions. Many thanks to the members of the Soil Science and TrES group at the University 1926


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