Geofluids / 2019 / Article
Special Issue

New Applications in Gas Geochemistry

View this Special Issue

Research Article | Open Access

Volume 2019 |Article ID 4783514 |

A. L. Gagliano, S. Calabrese, K. Daskalopoulou, J. Cabassi, F. Capecchiacci, F. Tassi, S. Bellomo, L. Brusca, M. Bonsignore, S. Milazzo, G. Giudice, L. Li Vigni, F. Parello, W. D’Alessandro, "Degassing and Cycling of Mercury at Nisyros Volcano (Greece)", Geofluids, vol. 2019, Article ID 4783514, 18 pages, 2019.

Degassing and Cycling of Mercury at Nisyros Volcano (Greece)

Guest Editor: Guodong Zheng
Received07 Feb 2019
Revised06 May 2019
Accepted01 Jul 2019
Published14 Aug 2019


Nisyros Island (Greece) is an active volcano hosting a high-enthalpy geothermal system. During June 2013, an extensive survey on Hg concentrations in different matrices (fumarolic fluids, atmosphere, soils, and plants) was carried out at the Lakki Plain, an intracaldera area affected by widespread soil and fumarolic degassing. Concentrations of gaseous elemental mercury (GEM), together with H2S and CO2, were simultaneously measured in both the fumarolic emissions and the atmosphere around them. At the same time, 130 samples of top soils and 31 samples of plants (Cistus creticus and salvifolius and Erica arborea and manipuliflora) were collected for Hg analysis. Mercury concentrations in fumarolic gases ranged from 10,500 to 46,300 ng/m3, while Hg concentrations in the air ranged from high background values in the Lakki Plain caldera (10-36 ng/m3) up to 7100 ng/m3 in the fumarolic areas. Outside the caldera, the concentrations were relatively low (2-5 ng/m3). The positive correlation with both CO2 and H2S in air highlighted the importance of hydrothermal gases as carrier for GEM. On the other hand, soil Hg concentrations (0.023-13.7 μg/g) showed no significant correlations with CO2 and H2S in the soil gases, whereas it showed a positive correlation with total S content and an inverse one with the soil pH, evidencing the complexity of the processes involving Hg carried by hydrothermal gases while passing through the soil. Total Hg concentrations in plant leaves (0.010-0.112 μg/g) had no direct correlation with soil Hg, with Cistus leaves containing higher values of Hg with respect to Erica. Even though GEM concentrations in the air within the caldera are sometimes orders of magnitude above the global background, they should not be considered dangerous to human health. Values exceeding the WHO guideline value of 1000 ng/m3 are very rare (<0.1%) and only found very close to the main fumarolic vents, where the access to tourists is prohibited.

1. Introduction

Volcanoes and geothermal areas are natural sources of environment pollutants potentially dangerous for human health. Paroxysmal eruptions and passive degassing emit huge amounts of gases such as CO2, H2S, SO2, and HF, including gaseous elemental mercury (GEM) [14]. Trace metals, being associated with uprising gases, are usually found at considerable concentrations in hydrothermal fluids [5]. Even at very low concentrations, they can have a strong impact on the atmosphere and hydrosphere and consequently on the biosphere [6].

Among the volcanic trace volatile elements, mercury (Hg) is one of the most environmentally significant [7] because of its extreme mobility and toxicity [8]. The biogeochemistry of Hg is extremely complex due to the exchanges between atmospheric, terrestrial, and marine pools [9]. These processes are mainly driven by microbial activity, dark abiotic and photochemical reactions affecting Hg speciation and bioaccumulation [10]. It is emitted in several forms: elemental (metallic) Hg and inorganic and organic Hg compounds. Metallic Hg (Hg0) is highly volatile due to its high vapour pressure and may experience long-range transport in the air due to its relatively long half-life in the atmosphere (1-2 years [11]). Monovalent and divalent Hg are both soluble in water; divalent Hg (HgII) is more stable and common in the environment than monovalent (HgI). This form also may undergo complexation, precipitation with inorganic ligands, and sorption onto the soil matrix. The toxicological properties of Hg for the environment and human health depend on the physical and chemical form in which it occurs. Hg vapours, for example, are very dangerous if inhaled, due to their ability to reach the lungs causing pulmonary oedema, pain, and peeling of the respiratory epithelium of the bronchi [12, 13].

Mercury, as a constituent of volcanic and geothermal fluids [14, 15], is discharged in water and released into the atmosphere as Hg0 being associated with reducing noncondensable gases [16, 17].

In the last decades, many authors underlined the correlation between Hg and H2S in discharged hydrothermal fluids (e.g., [18]), as testified by the formation of solid cinnabar (HgS) at the fumarolic vents. Hydrogen sulphide is a toxic pollutant; it is corrosive and poses severe concerns for human health [19, 20].

Nisyros Island is a quiescent volcano releasing hydrothermal gases from several fumarolic emissions and also diffusively through the soil. The hydrothermal fluids of Nisyros are rich in H2S [2123], and their diffuse emission creates an extremely acidic environment in soils affected by the hydrothermal degassing [24, 25].

Here, we report the results of an extensive survey on Hg concentrations in different media (fumarolic fluids, atmosphere, soils, and plants) at the Lakki Plain, an area intensively impacted by hydrothermal degassing on Nisyros Island. Even though the geogenic degassing of Nisyros Island has been greatly studied, most of the research conducted was mainly concentrated on the gaseous C compounds and the noble gas composition of the fumaroles. The significance and novelty of this work, with respect to the existing literature, is to add Hg on the puzzle. Furthermore, to the best of our knowledge, this is so far the first study that attempts to define the Hg cycling in an active volcanic/geothermal system by taking into consideration such a great variety of media. Gaseous elemental mercury (GEM) concentrations, together with H2S and CO2 in soil gas, were determined in both the fumarolic emissions and ambient air. Similarly, the relationships between fumarolic activity and Hg in the soils were investigated, comparing Hg concentrations to temperature, pH, hydrothermal gas, and the elemental concentrations of C, N, and S measured in the same soils. Leaves of two plant species (Cistus and Erica) were also collected and their Hg and S contents determined. Finally, a preliminary estimation of the Hg output to the atmosphere from the hydrothermal area of Nisyros was carried out.

2. Study Area

Nisyros Island (Figure 1) is a quiescent volcano located in the easternmost volcanic group of the South Aegean Active Volcanic Arc (SAAVA [26]). The volcanic edifice developed in the last 200 ka through five distinguished stages [27, 28] led to the formation of a caldera of about 4 km in diameter. The most recent activity consisted of hydrothermal explosions forming several phreatic craters, the last of which occurred in 1887 [27]. The Lakki Plain (Figure 1) represents the southeastern remnants of the calderic depression after the emplacement of a series of volcanic domes filling up the northwestern part. Fumarolic fields are currently active in this area, mainly within the hydrothermal craters strongly controlled by fracturing along the main NW- and NE-trending active fault systems [29], and are fed by a >1000 m deep hydrothermal system having a temperature of 300-350°C [30, 31]. The hydrothermal craters form three main groups (Figure 1): the oldest comprises the Kaminakia craters, the second consists of the Stefanos crater, whereas the third corresponds to the youngest area where a postcalderic dome (Lofos) is placed and includes the Phlegeton, Megalos Polybotes, and Mikros Polybotes craters [31, 32]. Water vapour (91-99%) is the main component of the fumarolic fluids, followed by CO2 and H2S [22]. The estimated total CO2 and H2S outputs are close to 1 kg/s and <0.3 kg/s, respectively [31, 32].

3. Materials and Methods

After the collection of few samples in 2009 and 2010, a multidisciplinary field campaign was carried out on June 2013 at the Lakki Plain, where soil gases, soils, and vegetation were sampled, and Hg, H2S, and CO2 concentrations in the air were measured.

A total of 106 soil gas samples was collected at the Lakki Plain mostly in the fumarolic areas of Kaminakia, Stefanos, Mikros Polybotes, and Phlegeton craters and in the areas of Ramos and Lofos (Figure 1). Soil gases were sampled at 50 cm depth using a Teflon tube of 5 mm ID equipped with a tight plastic syringe to avoid air contamination. Soil gas sampling sites were the same as those of the top soils. H2S and CO2 analysis was carried out on the overpressurised vials using a Micro GC MSHA CP-4900 having 3 independent modules. Soil temperature was measured at 20 cm depth by using thermal probes and a digital thermometer; these measurements were carried out 10–15 min after the insertion of the thermal probe in the soil in order to achieve thermal equilibrium.

Top soils were collected from the first 3 cm depth at 130 spots at the Lakki Plain. Soil samples were dried, homogenized, and powdered. An aliquot of the homogenized samples was used for the analysis of total Hg, which was performed using a DMA-80 analyser (an atomic absorption spectrophotometer, Milestone, Wesleyan University, Middletown, CT, USA). About 10 mg of dry soil was loaded into specific nickel boats and analysed according to the US-EPA 7473 method [33]. Accuracy was checked by running replicates of the reference materials NCSDC7701 () and MESS3 (). Bench quality control material was measured at the start of each analytical run (set of 15 samples) for quality assurance and control. The measured values were, on average, within ±8% of the recommended values.

Total C, N, and S were analysed on powdered samples by elemental analysis (Elementar Vario EL Cube, Hanau). The technique is based on “purge and trap” separation (C, N, and S), following high-temperature incineration (induction furnace) in a pure oxygen atmosphere and at a constant temperature exceeding 1150°C for the sample, with WO3 as catalyst. Helium was used as the carrier gas. Detection limits were 0.04 wt% for C and 0.003 wt% for N and S.

Soil pH values were measured using a specific combination electrode on soil suspensions that were made with deionized water with a soil/solution weight ratio of 1/2.5 [34].

A passive biomonitoring survey was carried out in order to determine the total Hg content in two local spontaneous plants and evaluate the possible contamination by Hg gas emissions. The collected vegetation consisted of 17 leaf samples of the genus Erica (manipuliflora and arborea spp.) and 14 leaf samples of the genus Cistus (creticus and salvifolius spp.). Both the plant species have evergreen leaves and grow widespread as small shrubs (10-50 cm height) in the Lakki Plain where soil degassing is at a lower level. To enhance the interpretation, soil samples were collected along a buffer area of few tens of centimetres close to the sampled plants. One sample of vegetation and soil was collected outside the caldera as local background blank. The sampling sites and the sampled plants were chosen randomly; for each site, three separate plants in a buffer area of 1.5 m were sampled and merged to obtain the final sample. Vegetation samples were dried in the oven at temperature below 40°C and powdered by agate planetary ball mill to avoid contamination. Analysis of total Hg was made with the use of PerkinElmer Inc. SMS 100 Solid Mercury Analysis. Each sample was heated in an oxygen-rich furnace to release all the decomposition products including Hg. These products were then carried in a stream of O2 to a catalytic section of the furnace; halogens and/or oxides of N and S were trapped on the catalyst. The remaining vapour was then carried to an amalgamation cell that selectively trapped Hg. After the system was flushed with O2 to remove any remaining gas or decomposition products, the amalgamation cell was rapidly heated, releasing Hg vapour. Flowing O2 carried the Hg vapour through an absorbance cell positioned in the light path of a single wavelength atomic absorption spectrophotometer. Absorbance was measured at the 253.7 nm wavelength as a function of the Hg concentration in the sample.

Collection of total gaseous mercury (TGM) was performed with gold-coated bead traps (Au traps), through which atmospheric air was pumped at flow rates between 0.5 and 0.6 L/min [35] over collection periods ranging from 2 to 60 min. At three fumaroles, the gas was collected downstream of a vapour condenser sucking with a graduated 100 mL syringe and sent to the same Au traps through a three-way valve [36]. The collected Hg was then measured by cold vapour atomic fluorescence spectrometry (CVAFS), based on the conventional thermal-desorption amalgamation technique (relative standard ; EPA Method IO-5; [33, 35, 37]). The results obtained were multiplied by the sampling volume and expressed in ng/m3.

The simultaneous real-time measurements of gaseous elemental mercury (GEM), CO2, H2S, and meteorological parameters (air temperature, pressure, and relative humidity) were carried out by coupling portable instruments (similarly to what was proposed by [20]). GEM was measured with a Lumex® RA-915M, which is an atomic absorption spectrometer with a Zeeman effect with high-frequency modulation of light polarization (ZAAS-HFMLP). The separation of the spectral lines (at ) is operated by a permanent external magnetic field, into which a source of radiation (Hg lamp) is placed [38, 39]. The Zeeman background correction and the multipath analytical cell provide high selectivity and sensitivity [39]. The instrument operates at a flow rate of 10 L/min, whereas its rechargeable battery allows up to 8 h of continuous measurements. The detection limit is 2 ng/m3, while the accuracy of the method is 20% from 2 to 50,000 ng/m3 [38, 39]. The remaining parameters were measured with a Multi-GAS analyser manufactured by INGV-Palermo. Atmospheric gas was drawn into the sampler with an air pump at 1.2 L/min through a 1 μm Teflon membrane particle filter and was pumped through a CO2/H2O gas detector (Licor LI-840 NDIR closed-path spectrometer) and a series of electrochemical sensors for SO2 (0–200 ppm; 3ST/F electrochemical sensor by City Technology Ltd.) and H2S (0–50 pm; EZ3H electrochemical sensor by City Technology Ltd.) detection. The sensors were housed in a weather-proof box mounted on a backpack frame and were calibrated, before and after fieldwork, with standard calibration gases (200 ppm SO2, 50 ppm H2S, and 3014 ppm CO2) mixed with ultrapure nitrogen to provide a range of desired concentrations [4, 40].

The spatial coordinates for each concentration value were simultaneously acquired through a GPS signal. All instruments were synchronized and set to high-frequency acquisition (every two seconds: 0.5 Hz). Measurements were carried out along four (Polybotes, Kaminakia, Stefanos, and Lofos) transect walks (about 15 km path, with a mean speed of 1.5 km/h) across the Lakki Plain caldera. The raw data have been processed by a dedicated software (RatioCalc [41]) that allows a derivation of mass ratios of various compounds (e.g., CO2/H2S, GEM/CO2, and GEM/H2S).

Dataset from the gas soil and air surveys were used to define the threshold values of Hg, H2S, and CO2. Data were processed following Sinclair’s portioning method extracting the main populations [42]. This method consists in the definition of single populations through the inflection points (main populations) or changes in direction (secondary populations) of the curvature on the probability plot by visual analysis. Finally, data were plotted by using the GIS platform; distribution maps were drawn and ranked according to the identified populations.

4. Results

4.1. Fumarolic Gases and Atmosphere

In 2009, TGM was measured with Au traps in the atmosphere at 9 sampling sites at different distances from the main fumarolic vents. These sampling sites were previously investigated by D’Alessandro et al. [43] measuring H2S concentrations in the atmosphere with passive samplers. The traps were placed in a range of distance always longer than 10 m and up to about 2 km from the fumarolic vent. Mercury values ranged from 9.4 to 420 ng/m3 (Table 1). Although not directly comparable due to the different and sometimes not overlapping measuring time intervals (2-60 min for TGM and 4 hours to 5 days for H2S), the two datasets show a positive correlation (Figure 2), with the highest values close to the fumaroles and the lowest on the caldera rim.

SampleDate (dd/mm/yyyy)Time (min)Flux (dm3/min)Volume (m3)TGM (ng/m3)

Stefanos 1(4)31/08/200950.50.0025266
Stefanos 2(5)31/08/200950.50.0025163
Volcano Cafe(8)01/09/2009300.50.01554.1
Polybotes bottom(2)02/09/200920.50.0010222
Polybotes rim(3)02/09/200950.50.0025133
AM fumarole31/08/2010n.a.n.a.0.0002546,300
K6 fumarole31/08/2010n.a.n.a.0.000241,200
PP9S fumarole31/08/2010n.a.n.a.0.000210,500

Sampling sites of 2009 and IDs in brackets are the same as in [43]; fumaroles sampled in 2010 are the same as in [44]. n.a. = not applicable.

In 2010, further 5 measurements with Au traps were performed. Two measurements were made in the atmosphere at less than 1 m far from the two main fumarolic vents and gave concentrations of 2360 and 4530 ng/m3 (Table 1). Three fumarolic vents were investigated by performing measurements on the undiluted hydrothermal fluid collected at the outlet of a condenser; results provided values from 10,500 to 46,300 ng/m3 (Table 1). The composition of the contemporaneously collected gases was published by [44].

In 2013, GEM measured with Lumex® gave atmospheric concentrations from 2 to 7132 ng/m3. Values measured with the Multi-GAS ranged from 393 μmol/mol, which is the background atmospheric value, up to saturation of the sensor (~4000 μmol/mol) for CO2, from 0.2 μmol/mol up to saturation of the sensor (~60 μmol/mol) for H2S, and from 0.39 to 1.34 μmol/mol for SO2. Saturated values, about 0.1% for CO2 and 1.6% for H2S, were not considered for Hg/CO2 and Hg/H2S calculations.

4.2. Soils

All parameters measured in the soil samples of the fumarolic areas of the Lakki Plain are shown in Table 2. Total Hg ranged from 0.023 to 13.7 μg/g of dry soil. Soil temperatures measured at 20 cm depth varied between 25.5 and 100°C, while concentrations of H2S and CO2 at 50 cm depth ranged from <0.001 to 17.8% vol and from 0.28 to 75.3% vol, respectively. Elemental C, N, and S contents in the soil were in the range 0.06-2.63, 0.004-0.23, and 0.014-56.3 weight %, respectively. Soil pH varied from 0.71 to 7.30.

SiteENHg (μg/g)N (%)C (%)S (%)pHH2S (%)CH4 (%)CO2 (%) (°C @ 20 cm)

023 A51468940485081.590.0530.8008.4471.8710.280.09247.35n.m.
024 A51467740485160.720.0240.2610.8692.7917.750.1575.27n.m.
025 A51466340485291.780.0210.4212.5691.9614.930.1364.31n.m.
026 A51465240485100.150.0180.0600.7792.987.630.08345.21n.m.
027 A51466740485070.230.0270.1031.6322.9210.200.1153.84n.m.
028 A51469540485260.210.0350.0978.9161.146.820.06735.73n.m.
029 A51470640485100.710.0110.0703.4922.77n.d.n.d.n.d.n.m.
030 A51466140485040.340.0130.3281.2452.6017.830.1575.22n.m.
031 A51464440485051.480.0090.0746.9682.027.010.07338.55n.m.
032 A51463540484880.330.0130.0951.9862.995.670.07136.07n.m.
033 A51464340484903.440.0070.19816.2601.3010.060.1056.13n.m.
034 A51462140484900.410.0190.0702.5362.96n.d.n.d.n.d.n.m.
035 A51512440486150.810.0200.44324.4681.05n.d.n.d.n.d.n.m.
036 A51514840486310.460.0650.4241.0572.58bdl0.049.26n.m.
037 A51515740486511.090.0090.1590.9152.730.0050.0115.80n.m.
039 A51547540481820.340.0220.3670.7834.15bdl0.00022.27n.m.
040 A51550040481660.680.0400.6931.0453.15bdl0.00048.99n.m.
041 A51551040481595.030.0160.4182.5931.390.660.4826.32n.m.
042 A51553540481270.760.0320.38833.5061.920.190.2413.25n.m.
043 A51555340481050.540.0210.2281.9733.350.0120.001913.50n.m.
044 A51555440481120.330.0790.9742.4243.73bdl0.00051.60n.m.
045 A51539440481800.620.0190.4344.3522.790.0130.1413.10n.m.
047 A51546540480960.190.0350.5870.2544.80bdl0.00057.66n.m.
048 A51540940480790.110.0100.2551.3222.880.0160.118.36n.m.
049 A51541440480500.790.0200.9612.6721.87bdl0.4930.67n.m.
050 A51541840480130.610.0220.9352.1591.642.150.9043.68n.m.
051 A51543240480030.320.0110.1511.5123.32bdl0.2227.23n.m.
053 A51548240479841.050.0160.2593.9543.280.0220.2525.17n.m.
054 A51551240479950.150.0210.2200.9333.27n.d.n.d.n.d.n.m.
186 A51554640480801.220.0230.2434.2803.450.100.3025.24n.m.
189 A51553040479980.140.0270.1731.2383.41bdl0.00155.25n.m.
212 A51520440487070.370.0931.7771.0183.77bdl0.00033.36n.m.
239 A51495840480620.200.0090.16440.3281.330.190.0232.80n.m.
240 A51499040480770.310.0060.1074.8422.48n.d.n.d.n.d.n.m.
241 A51503240480700.810.0220.3825.6901.2517.120.6872.01n.m.
242 A51502440481270.230.0210.0811.6533.470.100.0287.30n.m.
244 A51508840481700.390.0240.1941.4973.170.0150.05213.83n.m.
247 A51510040481460.340.0340.4511.7522.800.0060.00089.53n.m.
248 A51512240481110.410.0140.1783.2162.231.670.1620.21n.m.
249 A51510740480920.210.0320.7825.1722.00n.d.n.d.n.d.n.m.
251 A51508140481031.440.0590.6374.5632.73bdl0.00059.50n.m.
254 A51501340480470.820.0461.0473.6101.5913.750.5861.71n.m.
255 A51503940480330.630.0510.78056.2762.2214.970.7068.74n.m.
256 A51502040479810.580.0130.2522.3991.550.0870.0526.46n.m.
257 A51498640479920.580.0240.7282.9081.681.790.2629.13n.m.
259 A51514340480930.480.0090.15210.0401.776.860.2232.79n.m.

Sites 1 and Mandraki are background sites outside the Lakki caldera. n.d. = not determined; n.m. = not measured; bdl = below detection limit (<0.002 for H2S; <0.0002 for CH4). Easting (E) and northing (N) are expressed as UTM coordinates WGS84, all sites belonging to sector 35S. Data of S concentrations and pH of samples from 1 to 17 and from N-St-1 to N-St-28 are taken from [24]. Samples collected close to the plants of Table 3.
4.3. Plants

Total Hg concentrations in the leaves collected from the Lakki Plain are summarized in Table 3. Data analysis showed the Hg range from 0.014 to 0.066 μg/g for Erica leaves and from 0.010 to 0.112 μg/g for Cistus leaves. The Hg concentrations in the soils sampled near the plants vary from 0.045 to 0.619 μg/g with a pH ranging from 4.21 to 5.55 (Table 2). The highest pH value is 7.30 and was measured outside the caldera; the value is representative of the local background for the soils collected close to the plants (Table 2).

Total Hg (μg/g)Total S (μg/g)Total Hg (μg/g)Total S (μg/g)

1 NY-E0.02611801 NY-C0.0101080
2 NY-E0.04663402 NY-C0.0375950
3 NY-E0.02822103 NY-C0.0222420
4 NY-E0.0142310
5 NY-E0.02514105 NY-C0.0552550
6 NY-E0.01915406 NY-C0.0192290
7 NY-E0.01628407 NY-C0.0565290
8 NY-E0.06625608 NY-C0.1123350
9 NY-E0.0363630
10 NY-E0.0234360
11 NY-E0.039428011 NY-C0.0253570
12 NY-E0.030148012 NY-C0.0282430
13 NY-E0.036296013 NY-C0.0954260
14 NY-E0.065264014 NY-C0.0272340
15 NY-E0.024211015 NY-C0.0292860
16 NY-E0.023254016 NY-C0.0773610
17 NY-E0.034146017 NY-C0.1123140

Soil samples identified with the numbers from 1 to 17 in Table 2 were collected close to the plant samples with the above corresponding numbers.

5. Discussion

5.1. Mercury in the Fumarolic Fluids of Nisyros

Analyses of Hg directly on fumarolic fluids have rarely been performed. The values reported in literature related to several fumaroles worldwide [3, 35, 4549] cover a broad range from 1400 to 1,828,000 ng/m3 (Table 4). The values resulting from the three fumaroles sampled at Nisyros fall within this range. Correlating the obtained Hg values with the major composition of the fumarolic gases [44], Hg/H2S and Hg/CO2 ratios ranging from to and from to , respectively, were observed. The results obtained are coherent with values provided by other fumarolic fields at world scale (Table 4).

AreaTGM (ng/m3)References

Fumaroles Japan (>100 sites)1400-1,828,000[36, 45, 46]
Kilauea, Hawaii (U.S.A.)274-1031[47]
Colima volcano (Mexico)470-1442[47]
White Island, New Zealand (fumarole 3)22,000-38,000[48]
Yellowstone caldera, U.S.A. (9 fumaroles)415-30,000[3]
Solfatara di Pozzuoli, Italy (fumarole BG)93,500[49]
Nisyros, Greece10,500-46,300This study

The measured Hg/H2S and Hg/CO2 ratios should be regarded as lower limit values since water soluble HgII species plausibly are lost within the fumarolic condensate collected by the sampling device. As evidenced in previous studies, the lost Hg fraction could represent a significant part of the total emitted Hg. Bagnato et al. [49] suggested that up to 70% of the total Hg emitted from the Bocca Grande (BG) fumarole (Phlegrean Fields, southern Italy) remained in the collected condensate. However, of the 70 fumarolic samples in which Nakagawa [36, 45, 46] measured Hg both in the gas and in the condensed vapour, only in 8 of the samples was the Hg found in the condensed fraction that represented more than 20% of the total. Nevertheless, further studies will be necessary to ascertain the quantity of Hg lost in the condensed steam in the fumaroles of Nisyros.

5.2. Mercury in the Atmosphere of the Lakki Plain Area

Background values of atmospheric GEM in pristine unpolluted areas in the northern hemisphere are below 2 ng/m3, though a decreasing trend in the last decades was recognized [50]. In volcanic/geothermal areas, measured values are often significantly higher than the natural background (tens to hundreds of ng/m3, Table 5). This holds true also for the fumarolic area of the Lakki Plain at Nisyros both for the point measurements with Au traps and for measurements performed along transects with Lumex®.

AreaHg atmosphere (ng/m3)Hg/S (×10-6)Hg/CO2 (×10-8)Total Hg output (kg/a)References

Las Pailas, Rincon de la Vieja, Costa Rican.r.8.40.14-1.70.8-2.4[4]
Las Hornillas, Miravalles volcano, Costa Rican.r.2.010.35-104-12[4]
Poas, Costa Rican.r.0.03n.r.1.6-2[4]
Tatun volcanic field, Taiwan5.5-2922.4-54-405-50[71]
La Fossa crater, Vulcano, Italy4.8-3390.48-1.30.4-7[72]
Yellowstone caldera, U.S.A.n.r.n.r.0.16-0.2615-56[3]
Mt. Lassen fumaroles, Cascades, U.S.A.n.r.n.r.2-2296-167[3]
Solfatara di Pozzuoli, Italyn.r.n.r.1.37[49]
Solfatara di Pozzuoli, Italyn.r.n.r.1.342[54]
La Soufriere, Guadeloupe, Lesser Antilles15-1893.2n.r.0.8[73]
Nea Kameni, Greece4.5-121n.r.0.1-0.340.2-2[53]
White Island, New Zealand73-890.13-0.251.43-2.47n.r.[48
Nisyros, Greece (fumaroles)n.a.0.03-0.160.76-3.50.7This study
Nisyros, Greece (atmosphere: Au traps)9.4-420n.a.n.a.n.a.This study
Nisyros, Greece (atmosphere: Lumex®)2-713211-681.5-8.21.9This study

n.r. = not reported; n.a. = not applicable.

The data acquired in the air with the Lumex® and Multi-GAS were plotted as described by Sinclair [42] and are shown in Figure 3. The CO2 probability plot (Figure 3(a)) identifies three main populations (A, B, and C). The A population comprises 64.6% of the data with values ranging from 392 to 431 ppm and refers to the local atmospheric CO2 background, which is close to the global atmospheric value of unpolluted air in 2013 (395 ppm [51]). Population B (33.3% of the data; CO2 431-561 ppm) is the population with CO2 level slightly higher than average atmospheric air, probably due to diffuse soil degassing. Population C (2.1% of the data) includes the highest values (up to >4000 ppm), indicating a significant fumarolic CO2 contribution to the atmosphere.

Based on the probability plot (Figure 3(b)), the H2S dataset can be divided into four populations: A includes very low H2S concentrations (<0.47 ppm, 5% of the values); B population with values from 0.47 to 2.11 ppm (50% of the data) indicating a slight fumarolic contribution; C population (2.11-57 ppm, 43.5% of the data) indicating a significant H2S input into the atmosphere; D population (1.5% of the data) includes of H2S up to saturation of the sensor in the vicinity of the active fumaroles, suggesting a significant contribution of the hydrothermal fluids released from the subsurface.

Three distinct populations can be recognized (, B from 8.5 to 44.9, and C up to 7132 ng/m3; 12.2%, 82.8%, and 5.0%, respectively) for GEM concentrations in the air (Figure 3(c)) that were measured with the Lumex® instrumentation.

In Figure 4, an example of H2S, CO2, and GEM concentrations measured in the atmosphere through transect walk within the Lakki Plain is shown. GEM, H2S, and CO2 concentration peaks, in correspondence with the fumaroles of Phlegeton, show a good match, confirming the interdependence of these gaseous compounds and their common origin from the fumaroles. The main fumarolic emissions were clearly highlighted by anomalously high Hg concentrations (up to ~600 ng/m3) with respect to the surrounding air masses (~30 ng/m3). GEM concentrations above background values measured away from the main fumarolic vents were probably due to soil degassing. The Lakki Plain and especially the main hydrothermal craters are sites of strong hydrothermal degassing with CO2 fluxes up to 6175 g/m2/day [52]. Mercury fluxes from the soil have not been measured at Nisyros, but as reported from the literature [3, 49, 53, 54], soils at geothermal and hydrothermal systems also emit gaseous Hg. Nevertheless, the previous authors found Hg fluxes (1-2000 μg/m2/day) that are many orders of magnitude lower than those of CO2, with the latter gas often acting as carrier for Hg.

5.3. Mercury in the Soil

The soils of the Lakki Plain are strongly weathered by past and present fumarolic activity. This can be recognized by the widespread presence of secondary alteration minerals, mainly sulfates [24, 25]. The main drivers of the alteration process are fumarolic H2O and H2S. The former is the main carrier of thermal energy, which is reflected in soil temperatures reaching up to the boiling temperature of water. Soil temperatures provide indications regarding the hydrothermal uprising gases, allowing the identification of the actively degassing areas. High temperatures are to be considered related to both high fluxes of hydrothermal fluids and the enrichment of the hydrothermal component in the soil gases. The temperature distribution map at 20 cm depth indicates temperatures above 30°C in all the investigated sites, except for some points along the western flank of the Kaminakia crater (Figure 5(a)). Higher temperatures, from 50 to 100°C, were recorded at the southern part of the Stefanos crater, at Phlegeton and Mikros Polybotes (Figure 5(a)).

Hydrogen sulphide in the fumarolic gases of Nisyros is the third most abundant species after H2O and CO2 [22]. In the soil gases, on a dry basis, it represents up to nearly 18% vol. Within the soil, H2S is oxidised by atmospheric O2 forming sulfuric acid [55, 56], by the net reaction

Such reaction is responsible for the high S contents of the analysed soils (median ~2%, max ~56% (Table 2)) and the very low values of soil pH (from 0.71 to 5.55 (Table 2)). Both parameters show an inverse relationship (Figure 6(a)) indicating that, at the most actively exhaling zones, more sulfuric acid is produced and more sulfur is deposited.

The total amount of Hg trapped in the soil was plotted in a probability plot. As for the Hg concentrations in the air, three populations were detected (Figure 7); a secondary population containing the higher values was detected as indicated by the black arrow in Figure 7. High Hg concentrations were measured in the soil close to the main fumarolic vents (Figure 5(b)). As for sulfur, the inverse relationship between soil Hg and soil pH (Figure 6(b)) supports the transport and the deposition of Hg by fumarolic fluids. Daskalopoulou et al. [24] evidenced that also other volatile elements like As, Bi, Pb, Sb, Se, and Te are enriched in the soils of the Lakki Plain that are mostly affected by hydrothermal gases.

The accumulation of Hg in the soil matrix does not depend solely on the amount of Hg carried by the uprising hydrothermal gases but also on the soil retention capacity. Many studies demonstrated that Hg in soils shows generally a good correlation with soil organic matter (SOM). Ottesen et al. [57] evidenced such positive correlation at the continental scale, based on the analysis of more than 4000 soil samples from 33 countries in Europe. Martin et al. [58] found that the same correlation holds true for the volcanic soils of Mt. Etna. Elemental carbon, which can be considered a proxy for SOM, in the soils of the Lakki Plain does not show any correlation with the measured Hg values. This probably depends on the fact that most of the sampled soils are totally devoid of vegetation, limiting the presence of SOM to some vegetal debris and microbial communities. The low content of SOM may therefore not contribute much to Hg accumulation in the soils of the Lakki Plain. Sulphide, which could also react with Hg, is also very scarce in the surface soil levels due to the oxidising environment [24].

Soil temperatures are thought to play an important role in Hg retention in soils. This parameter has probably a contrasting effect because higher soil temperatures indicate stronger hydrothermal gases transporting more Hg from the depth, but at the same time, higher soil temperatures presuppose also a faster remobilization of Hg from the soils because of its high volatility [3].

Although hydrothermal gases like CO2 and H2S show their maxima close to the main fumarolic areas (Figures 5(d) and 5(e)), no correlation with soil Hg could be evidenced ( value 0.77 and 0.83, respectively, and correlation index 0.04 and 0.02, respectively). However, even though both soil and gas samples were collected at the same time and in the same place, they are not totally comparable as CO2 and H2S were measured on the gas phase collected at the 50 cm depth while Hg was measured on the solid phase at the soil surface. Nevertheless, a better correlation was expected.

5.4. Mercury in the Plants

Plant leaves present lower concentrations with respect to the soils where they grow, while the local background in both plant leaves and soils shows very low concentrations in total Hg. Results show a range of values regarding the total Hg concentrations that seem to be positively correlated with the intensity of the fumarolic activity. The highest concentrations were measured in sites located close to the hydrothermal drill and the craters of Stefanos, Phlegeton, Mikros Polybotes, and Kaminakia, confirming the impact of the hydrothermal activity on the surrounding environment.

Regarding the availability of soil Hg to plants, it is considered to be low as there is a tendency for Hg to accumulate in the roots, indicating that the roots serve as a barrier to Hg uptake [59, 60]. Mercury concentration in aboveground parts of plants appears to depend largely on foliar uptake of Hg0 volatilized from the soil [61, 62] and therefore on the age of the plant and the time of day and year [63]. The transfer of Hg (gaseous forms) from the atmosphere occurs by dry and wet deposition (rain and snow) and enters into the organism by the stomata of the leaves through the transpiration process [59, 61, 64, 65]. The soil-plant correlation diagram (Figures 8(a) and 8(b)) shows that Cistus samples were enriched in Hg with respect to Erica presenting a moderately good positive correlation. Taking into consideration that Hg uptake is mostly through the leaves and the samples of both species were collected on the same day, the relatively high concentrations of total Hg in the Cistus samples can be justified by the higher specific surface area of its leaflets with respect to Erica’s. Additionally, equally important factors that should be taken into consideration are the solar radiation and the humidity. These two factors along with the specific surface area of the leaflets may possibly explain the elevated Hg concentration of the local background sample that was noticed at Erica. It is worth mentioning that the local background samples of both species were collected at a place located close to the sea, at noontime during summer period.

On the other hand, sulfur is an essential macronutrient for plant growth. Its uptake and distribution are tightly controlled by the environmentally induced changes in nutrient demand [66, 67]. Therefore, the high concentrations in S as well as the good correlation between the soil and plant samples in both species can be regarded as mainly caused by its uptake by the roots through the metabolic processes of the plants (Figures 8(c) and 8(d)). Nevertheless, the contribution of the transpiration process via the stomata of the leaves may also be important.

5.5. Environmental and Human Health Issues

Mercury is considered to be among the most toxic metals that could be taken by the human body through different pathways [13], especially concerning methylated species. Furthermore, its deleterious effects can be enhanced through its biomagnification along the trophic chain [11]. One of the primary uptake paths of Hg is through the inhalation of GEM. For the World Health Organization [68], atmospheric concentrations of Hg in the range of 15,000–30,000 ng/m3 may have adverse effects on humans (tremors, renal tubular effects, change in plasma enzymes, and others). However, using an uncertainty factor of 20, the same organization proposed a guideline value for Hg concentration in air of 1000 ng/m3 [68].

At the same time, the US Occupational Safety and Health Administration considered a permissible occupational exposure limit for GEM of 100,000 ng/m3 in the air [69], while the National (US) Institute for Occupational Safety and Health (NIOSH) established a recommended exposure limit for GEM of 50,000 ng/m3 as a time-weighted average (TWA) for up to a 10 h workday and a 40 h workweek [69]. The American Conference of Governmental Industrial Hygienists assigned to GEM a threshold limit value of 25,000 ng/m3 as a TWA for a normal 8 h workday and a 40 h workweek [69]. The minimum risk level (MRL) for chronic inhalation of GEM is 200 ng/m3 [69, 70]. The MRL is an estimate of the daily human exposure to a hazardous substance that is likely to be without appreciable risk of adverse health effects over a specified duration of exposure. The US EPA reference concentration for inhalation is calculated to be 300 ng/m3 (TWA) [69].

Taking into consideration the above limits and thresholds, it may be deduced that, although the atmospheric GEM concentrations within the Nisyros Caldera are sometimes many orders of magnitude above the global background, they do not represent a general hazard for human health. The area is yearly visited by many tens of thousands of tourists, but the zones where they arrive show GEM concentrations rarely exceeding the MRL. Areas exceeding the WHO guideline value of 1000 ng/m3 are very close to the main fumarolic vents where tourists are not allowed to go and where other toxic gases of higher danger are present (i.e., H2S [19]). Moreover, people who work all day in the area (ticket operators, owner, and employees of the Volcano Café) spend most of their time in areas with atmospheric GEM concentrations well below the occupational limits and generally also below the MRL. Probably, only volcanologists that take gas samples from the main fumaroles may be exposed to atmospheric GEM levels of a few thousands of ng/m3 for some hour, which has still to be considered a low exposition. Even though results propose no particular risk, a more complete survey is highly suggested to have a more accurate picture.

5.6. Total Output from the Hydrothermal System of Nisyros

It has long been established that the contribution of volcanic activity to the total natural emissions of Hg to the atmosphere is substantial [2, 4, 47]. However, due to the limited number of data available, significant uncertainties on the annual emissions of volcanic Hg still remain. Estimates range between 0.6 and 1000 t/a representing a proportion that varies from <1% up to 50% of total natural emissions [2, 4, and references therein]. The strongest contribution (90%) of the total output of volcanic Hg derives from explosive eruptions while the rest derives from passive degassing [2]. Emissions of single open-conduit volcanoes like Etna (Italy), Ambrim (Vanuatu), or Masaya (Nicaragua) are in the order of units to tens of t/a [4], pointing to strong underestimation of global volcanic outputs lower than 50 t/a. The contribution of fumarolic emissions from closed-conduit volcanoes is instead very limited as it is found in the range from 0.2 to 167 kg/a (0.0002-0.167 t/a (Table 5)).

Most of the Hg flux estimations from volcanic systems have been indirectly obtained cross-correlating the measured SO2 fluxes with the Hg/SO2 ratios measured in the volcanic plume [4]. Such method cannot be used for low-temperature fumarolic areas because magmatic SO2 is strongly scrubbed by the hydrothermal system. To obtain output estimates for such areas, different methods have been proposed. One of which is the measurement of Hg fluxes from the soils with accumulation chambers (dynamic flux chambers or static closed chambers) and the consequent integration of the fluxes over the whole hydrothermal area. Such method was applied only few times [49, 53, 54]. Another method is the cross-correlation of the total CO2 release of the fumarolic area with the Hg/CO2 ratio being measured either in the fumarolic fluids or in the air close to the vents [4]. Both methods give the order of magnitude of the Hg output, but they coherently confirm much lower outputs of fumarolic areas with respect to open-conduit volcanoes. Following the second approach, a rough estimation of the Hg output of Nisyros can be obtained considering the total CO2 output, as determined by Bagnato et al. [53], which is 84 t/d, and the Hg/CO2 ratios measured in the fumaroles that range from to () or in the air ranging from to (), corresponding to the total Hg output of 0.7 and 1.9 kg/a, respectively. Such figures fall in the lower range of the outlet values for fumarolic areas (Table 5).

6. Conclusions

Mercury and its compounds are highly toxic for humans and ecosystems. Volcanic and hydrothermal emissions are major natural sources of Hg in the atmosphere. At Nisyros, a potentially active volcano with intense and widespread degassing activity, real-time measurements of GEM showed concentrations up to 7132 ng/m3 within the Lakki Plain. The good correlation between Hg and the main fumarolic gases (H2O, CO2, and H2S) confirms the hydrothermal origin of the former. In the fumarolic gases, Hg was estimated in the range 10,500-46,300 ng/m3; these values should be considered the lower limit due to the plausible Hg loss within the condensing fumarolic vapour. Relatively high Hg concentrations were also identified in the soils; the accumulation of Hg in the soil matrix is dependent on both the amount carried by the upflowing hydrothermal gases and the soil ability to fix a part of it. The lack of vegetation at the crater area maybe responsible of the poor correlation between elemental C and Hg in the soil. No bioavailability through the roots was noticed in the plants collected at the Lakki Plain. The slightly high concentrations of the vegetation samples could have therefore been caused by the transpiration process that takes place in the stomata of the leaves, making Cistus a better candidate for biomonitoring investigations with respect to Erica due to the greater specific area of its leaves.

The aforementioned synoptic analysis of the results highlights that more than one matrix can be affected by hydrothermal Hg from the degassing activity. Furthermore, it underscores that Hg concentrations are positively correlated with the distance of the sample/measurement from the emission point. Even though the measured Hg concentrations were enhanced and at cases exceed the WHO limits in terms of inhalation, they seem to be of minor risk for human health as the exposure is for a limited time and the access for nonvolcanologists is prohibited. However, an uptake originating from the trophic chain should not be disregarded.

Data Availability

Data will be available on request.


K. Daskalopoulou’s present address is GFZ-German Research Centre for Geosciences, Potsdam, Brandenburg, Germany. F. Capecchiacci’s present address is Istituto Nazionale di Geofisica e Vulcanologia, Osservatorio Vesuviano, Naples, Italy. G. Giudice’s present address is Istituto Nazionale di Geofisica e Vulcanologia, Osservatorio Etneo, Catania, Italy.

Conflicts of Interest

The authors declare that they have no conflicts of interest.


We are grateful to Emanuela Bagnato, who made the measurements of the Au traps at the University of Palermo, to Mario Sprovieri who allowed us to make the measurements of Hg in the soils at the laboratories of the Consiglio Nazionale delle Ricerche, IAMC, UOS di Capo Granitola, and to Jens Fiebig, Artemis Kontomichalou, and Konstantinos Kyriakopoulos for their help in the field. We kindly acknowledge the owner of the Volcano Café, Mr. Sideris Kontogiannis, for his logistical support to all volcanologists working in the Nisyros Caldera (and also for many beers spent for free and for the delightful music of his Cretan Lyra at dusk). Finally, we would like to thank the municipality of Nisyros Island for its hospitality and generosity.


  1. M. S. Gustin, “Are mercury emissions from geologic sources significant? A status report,” Science of The Total Environment, vol. 304, no. 1-3, pp. 153–167, 2003. View at: Publisher Site | Google Scholar
  2. D. M. Pyle and T. A. Mather, “The importance of volcanic emissions for the global atmospheric mercury cycle,” Atmospheric Environment, vol. 37, no. 36, pp. 5115–5124, 2003. View at: Publisher Site | Google Scholar
  3. M. A. Engle, M. S. Gustin, F. Goff et al., “Atmospheric mercury emissions from substrates and fumaroles associated with three hydrothermal systems in the western United States,” Journal of Geophysical Research, vol. 111, no. D17, article D17304, 2006. View at: Publisher Site | Google Scholar
  4. E. Bagnato, G. Tamburello, G. Avard et al., “Mercury fluxes from volcanic and geothermal sources: an update,” Geological Society, London, Special Publications, vol. 410, no. 1, pp. 263–285, 2015. View at: Publisher Site | Google Scholar
  5. S. Metz and J. H. Trefry, “Chemical and mineralogical influences on concentrations of trace metals in hydrothermal fluids,” Geochimica et Cosmochimica Acta, vol. 64, no. 13, pp. 2267–2279, 2000. View at: Publisher Site | Google Scholar
  6. A. Kabata-Pendias and A. Pendias, Trace Elements in Soils and Plants, CRC, third ed edition, 2001.
  7. R. P. Mason, W. F. Fitzgerald, and F. M. M. Morel, “The biogeochemical cycling of elemental mercury: anthropogenic influences,” Geochimica et Cosmochimica Acta, vol. 58, no. 15, pp. 3191–3198, 1994. View at: Publisher Site | Google Scholar
  8. C. H. Lamborg, C. M. Tseng, W. F. Fitzgerald, P. H. Balcom, and C. R. Hammerschmidt, “Determination of the mercury complexation characteristics of dissolved organic matter in natural waters with “reducible Hg” titrations,” Environmental Science & Technology, vol. 37, no. 15, pp. 3316–3322, 2003. View at: Publisher Site | Google Scholar
  9. W. F. Fitzgerald, R. P. Mason, and G. M. Vandal, “Atmospheric cycling and air-water exchange of mercury over mid-continental lacustrine regions,” Water, Air & Soil Pollution, vol. 56, no. 1, pp. 745–767, 1991. View at: Publisher Site | Google Scholar
  10. F. M. M. Morel, A. M. L. Kraepiel, and M. Amyot, “The chemical cycle and bioaccumulation of mercury,” Annual Review of Ecology and Systematics, vol. 29, no. 1, pp. 543–566, 1998. View at: Publisher Site | Google Scholar
  11. W. F. Fitzgerald and C. H. Lamborg, “Geochemistry of mercury in the environment,” in Environmental Geochemistry, Treatise on Geochemistry, H. Holland and K. Turekian, Eds., pp. 1–47, Elsevier, 2007. View at: Publisher Site | Google Scholar
  12. T. W. Clarkson and L. Magos, “The toxicology of mercury and its chemical compounds,” Critical Reviews in Toxicology, vol. 36, no. 8, pp. 609–662, 2006. View at: Publisher Site | Google Scholar
  13. WHO, Exposure to Mercury: A Major Public Health Concern, World Health Organization and United Nations Environment Programme, Geneva, Switzerland, 2007.
  14. H. L. Barnes and T. M. Seward, “Geothermal systems and mercury deposits,” in Geochemistry of Hydrothermal Ore Deposits, H. L. Barnes, Ed., pp. 699–736, John Wiley & Sons, New York, 3rd ed. edition, 1997. View at: Google Scholar
  15. E. Bagnato, A. Aiuppa, F. Parello et al., “Degassing of gaseous (elemental and reactive) and particulate mercury from Mount Etna volcano (Southern Italy),” Atmospheric Environment, vol. 41, no. 35, pp. 7377–7388, 2007. View at: Publisher Site | Google Scholar
  16. D. A. Nimick, R. R. Caldwell, D. R. Skaar, and T. M. Selch, “Fate of geothermal mercury from Yellowstone National Park in the Madison and Missouri Rivers, USA,” Science of The Total Environment, vol. 443, pp. 40–54, 2013. View at: Publisher Site | Google Scholar
  17. D. E. Robertson, E. A. Crecelius, J. S. Fruchter, and J. D. Ludwick, “Mercury emissions from geothermal power plants,” Science, vol. 196, no. 4294, pp. 1094–1097, 1977. View at: Publisher Site | Google Scholar
  18. S. Vitolo and M. Seggiani, “Mercury removal from geothermal exhaust gas by sulfur-impregnated and virgin activated carbons,” Geothermics, vol. 31, no. 4, pp. 431–442, 2002. View at: Publisher Site | Google Scholar
  19. W. D’Alessandro, L. Brusca, K. Kyriakopoulos, G. Michas, and G. Papadakis, “Hydrogen sulphide as a natural air contaminant in volcanic/geothermal areas: the case of Sousaki, Corinthia (Greece),” Environmental Geology, vol. 57, no. 8, pp. 1723–1728, 2009. View at: Publisher Site | Google Scholar
  20. J. Cabassi, F. Tassi, S. Venturi et al., “A new approach for the measurement of gaseous elemental mercury (GEM) and H2S in air from anthropogenic and natural sources: examples from Mt. Amiata (Siena, Central Italy) and Solfatara Crater (Campi Flegrei, Southern Italy),” Journal of Geochemical Exploration, vol. 175, pp. 48–58, 2017. View at: Publisher Site | Google Scholar
  21. L. Marini and J. Fiebig, “Fluid geochemistry of the magmatic-hydrothermal system of Nisyros (Greece),” Mémoires de Géologie (Lausanne), vol. 44, p. 192, 2005. View at: Google Scholar
  22. J. Fiebig, F. Tassi, W. D'Alessandro, O. Vaselli, and A. B. Woodland, “Carbon-bearing gas geothermometers for volcanic-hydrothermal systems,” Chemical Geology, vol. 351, pp. 66–75, 2013. View at: Publisher Site | Google Scholar
  23. K. Daskalopoulou, S. Calabrese, F. Grassa et al., “Origin of methane and light hydrocarbons in natural fluid emissions: a key study from Greece,” Chemical Geology, vol. 479, pp. 286–301, 2018. View at: Publisher Site | Google Scholar
  24. K. Daskalopoulou, S. Calabrese, S. Milazzo et al., “Trace elements mobility in soils from the hydrothermal area of Nisyros (Greece),” Annals of Geophysics, vol. 57, Fast Track 2, 2014. View at: Publisher Site | Google Scholar
  25. S. Venturi, F. Tassi, O. Vaselli et al., “Active hydrothermal fluids circulation triggering smallscale collapse events: the case of the 2001–2002 fissure in the Lakki Plain (Nisyros Island, Aegean Sea, Greece),” Natural Hazards, vol. 93, no. 2, pp. 601–626, 2018. View at: Publisher Site | Google Scholar
  26. P. Nomikou, D. Papanikolaou, and V. J. Dietrich, “Geodynamics and volcanism in the Kos-Yali-Nisyros volcanic field,” in Nisyros Volcano - The Kos - Yali - Nisyros Volcanic Field, V. J. Dietrich and E. Lagios, Eds., Series: Active Volcanoes of the World, pp. 13–55, Springer International Publishing, 2018. View at: Google Scholar
  27. J. C. Hunziker and L. Marini, The geology, geochemistry and evolution of Nisyros Volcano (Greece). Implications for the volcanic hazards, no. 44, Memoires de Geologie (Lausanne), 2005.
  28. V. J. Dietrich, “Geology of Nisyros Volcano,” in Nisyros Volcano - The Kos - Yali - Nisyros Volcanic Field, Series: Active Volcanoes of the World, V. J. Dietrich and E. Lagios, Eds., pp. 145–201, Springer International Publishing, 2018. View at: Google Scholar
  29. V. J. Dietrich, G. Chiodini, and F. M. Schwandner, “The hydrothermal system and geothermal activity,” in Nisyros Volcano - The Kos - Yali - Nisyros Volcanic Field, Series: Active Volcanoes of the World, V. J. Dietrich and E. Lagios, Eds., pp. 57–102, Springer International Publishing, 2018. View at: Google Scholar
  30. T. Brombach, S. Caliro, G. Chiodini, J. Fiebig, J. C. Hunziker, and B. Raco, “Geochemical evidence for mixing of magmatic fluids with seawater, Nisyros hydrothermal system, Greece,” Bulletin of Volcanology, vol. 65, no. 7, pp. 505–516, 2003. View at: Publisher Site | Google Scholar
  31. S. Caliro, G. Chiodini, D. Galluzzo et al., “Recent activity of Nisyros volcano (Greece) inferred from structural, geochemical and seismological data,” Bulletin of Volcanology, vol. 67, no. 4, pp. 358–369, 2005. View at: Publisher Site | Google Scholar
  32. W. D’Alessandro, A. L. Gagliano, K. Kyriakopoulos, and F. Parello, “Hydrothermal methane fluxes from the soil at Lakki plain (Nisyros, Greece),” in Proceedings of the 13th International Congress of the Geological Society of Greece, vol. 47, no. 3, pp. 1920–1928, Chania, Crete, Greece, September 2013, Bulletin of the Geological Society of Greece. View at: Google Scholar
  33. US EPA, “Method 7473 (SW-846): mercury in solids and solutions by thermal decomposition, amalgamation, and atomic absorption spectrophotometry,” 1998, February 2019, View at: Google Scholar
  34. G. W. Thomas, “Soil pH and soil acidity,” in Methods of soil analysis – Part 3 Chemical methods, D. L. Sparks, Ed., Book Series, no. 5, pp. 475–490, Soil Sci. Soc. Am, 1996. View at: Google Scholar
  35. R. Ebinghaus, S. G. Jennings, W. H. Schroeder et al., “International field intercomparison measurements of atmospheric mercury species at Mace head, Ireland,” Atmospheric Environment, vol. 33, no. 18, pp. 3063–3073, 1999. View at: Publisher Site | Google Scholar
  36. R. Nakagawa, “Estimation of mercury emissions from geothermal activity in Japan,” Chemosphere, vol. 38, no. 8, pp. 1867–1871, 1999. View at: Publisher Site | Google Scholar
  37. US EPA, Method IO-5: Sampling and Analysis for Atmospheric Mercury. Compendium of Methods for the Determination of Inorganic Compounds in Ambient Air, Center for Environmental Research Information Office of Research and Development, US Environmental Protection Agency, Cincinnati, OH, 1999.
  38. S. E. Sholupov and A. A. Ganeyev, “Zeeman atomic absorption spectrometry using high frequency modulated light polarization,” Spectrochimica Acta Part B: Atomic Spectroscopy, vol. 50, no. 10, pp. 1227–1236, 1995. View at: Publisher Site | Google Scholar
  39. S. Sholupov, S. Pogarev, V. Ryzhov, N. Mashyanov, and A. Stroganov, “Zeeman atomic absorption spectrometer RA-915+ for direct determination of mercury in air and complex matrix samples,” Fuel Processing Technology, vol. 85, no. 6-7, pp. 473–485, 2004. View at: Publisher Site | Google Scholar
  40. A. Aiuppa, C. Federico, G. Giudice, and S. Gurrieri, “Chemical mapping of a fumarolic field: La Fossa Crater, Vulcano Island (Aeolian Islands, Italy),” Geophysical Research Letters, vol. 32, no. 13, article L13309, 2005. View at: Publisher Site | Google Scholar
  41. G. Tamburello, “Ratiocalc: software for processing data from multicomponent volcanic gas analyzers,” Computers & Geosciences, vol. 82, pp. 63–67, 2015. View at: Publisher Site | Google Scholar
  42. A. J. Sinclair, “Selection of threshold values in geochemical data using probability graphs,” Journal of Geochemical Exploration, vol. 3, no. 2, pp. 129–149, 1974. View at: Publisher Site | Google Scholar
  43. W. D'Alessandro, A. Aiuppa, S. Bellomo et al., “Sulphur-gas concentrations in volcanic and geothermal areas in Italy and Greece: characterising potential human exposures and risks,” Journal of Geochemical Exploration, vol. 131, pp. 1–13, 2013. View at: Publisher Site | Google Scholar
  44. J. Fiebig, S. Hofmann, F. Tassi, W. D'Alessandro, O. Vaselli, and A. B. Woodland, “Isotopic patterns of hydrothermal hydrocarbons emitted from Mediterranean volcanoes,” Chemical Geology, vol. 396, pp. 152–163, 2015. View at: Publisher Site | Google Scholar
  45. R. Nakagawa, “Amounts of mercury discharged to atmosphere from fumaroles and hot spring gases in geothermal areas,” Nippon Kagaku Kaishi, vol. 1984, no. 5, pp. 709–715, 1984. View at: Publisher Site | Google Scholar
  46. R. Nakagawa, “Amounts of mercury discharged to atmosphere from fumaroles in geothermal areas of Hokkaido,” Nippon Kagaku Kaishi, vol. 1985, no. 4, pp. 703–708, 1985. View at: Publisher Site | Google Scholar
  47. J. C. Varekamp and P. R. Buseck, “Global mercury flux from volcanic and geothermal sources,” Applied Geochemistry, vol. 1, no. 1, pp. 65–73, 1986. View at: Publisher Site | Google Scholar
  48. B. W. Christenson and E. K. Mroczek, “Potential reaction pathways of Hg in some New Zealand hydrothermal environments,” in Volcanic, Geothermal, and Ore-Forming Fluids: Rulers and Witnesses of Processes within the Earth, S. F. Simmons and I. Graham, Eds., vol. 10, pp. 111–132, Spec. Publ. Soc. Economic Geologists, 2003. View at: Google Scholar
  49. E. Bagnato, F. Parello, M. Valenza, and S. Caliro, “Mercury content and speciation in the Phlegrean Fields volcanic complex: evidence from hydrothermal system and fumaroles,” Journal of Volcanology and Geothermal Research, vol. 187, no. 3-4, pp. 250–260, 2009. View at: Publisher Site | Google Scholar
  50. N. Pirrone, S. Cinnirella, A. Dastoor et al., “Atmospheric pathways, transport and fate,” Technical Background Report for the Global Mercury Assessment 2013, AMAP/UNEP. Arctic Monitoring and Assessment Programme, Oslo, Norway/UNEP Chemicals Branch, Geneva, Switzerland, 2013. View at: Google Scholar
  51. NOAA-ESRL, “National Oceanic & Atmospheric Administration – Earth System Research Laboratory – Global Monitoring Division,” 2019, February 2019, View at: Google Scholar
  52. C. Cardellini, G. Chiodini, and F. Frondini, “Application of stochastic simulation to CO2 flux from soil: mapping and quantification of gas release,” Journal of Geophysical Research, vol. 108, no. B9, article 2425, 2003. View at: Publisher Site | Google Scholar
  53. E. Bagnato, G. Tamburello, A. Aiuppa, M. Sprovieri, G. E. Vougioukalakis, and M. Parks, “Mercury emissions from soils and fumaroles of Nea Kameni volcanic centre, Santorini (Greece),” Geochemical Journal, vol. 47, no. 4, pp. 437–450, 2013. View at: Publisher Site | Google Scholar
  54. F. Tassi, J. Cabassi, S. Calabrese et al., “Diffuse soil gas emissions of gaseous elemental mercury (GEM) from hydrothermal-volcanic systems: an innovative approach by using the static closed-chamber method,” Applied Geochemistry, vol. 66, pp. 234–241, 2016. View at: Publisher Site | Google Scholar
  55. V. W. Lueth, R. O. Rye, and L. Peters, ““Sour gas” hydrothermal jarosite: ancient to modern acid-sulfate mineralization in the southern Rio Grande Rift,” Chemical Geology, vol. 215, no. 1-4, pp. 339–360, 2005. View at: Publisher Site | Google Scholar
  56. D. R. Zimbelman, R. O. Rye, and G. N. Breit, “Origin of secondary sulfate minerals on active andesitic stratovolcanoes,” Chemical Geology, vol. 215, no. 1-4, pp. 37–60, 2005. View at: Publisher Site | Google Scholar
  57. R. T. Ottesen, M. Birke, T. E. Finne et al., “Mercury in European agricultural and grazing land soils,” Applied Geochemistry, vol. 33, pp. 1–12, 2013. View at: Publisher Site | Google Scholar
  58. R. S. Martin, M. L. I. Witt, G. M. Sawyer et al., “Bioindication of volcanic mercury (Hg) deposition around Mt. Etna (Sicily),” Chemical Geology, vol. 310-311, pp. 12–22, 2012. View at: Publisher Site | Google Scholar
  59. M. Lodenius, “Use of plants for biomonitoring of airborne mercury in contaminated areas,” Environmental Research, vol. 125, pp. 113–123, 2013. View at: Publisher Site | Google Scholar
  60. A. Pérez-Sanz, R. Millán, M. J. Sierra et al., “Mercury uptake by Silene vulgaris grown on contaminated spiked soils,” Journal of Environmental Management, vol. 95, no. 2012, pp. S233–S237, 2012. View at: Publisher Site | Google Scholar
  61. L. Fay and M. S. Gustin, “Investigation of mercury accumulation in cattails growing in constructed wetland mesocosms,” Wetlands, vol. 27, no. 4, pp. 1056–1065, 2007. View at: Publisher Site | Google Scholar
  62. L. Windham-Myers, J. A. Fleck, J. T. Ackerman et al., “Mercury cycling in agricultural and managed wetlands: a synthesis of methylmercury production, hydrologic export, and bioaccumulation from an integrated field study,” Science of the Total Environment, vol. 484, no. 1, pp. 221–231, 2014. View at: Publisher Site | Google Scholar
  63. M. D. Tabatchnick, G. Nogaro, and C. R. Hammerschmidt, “Potential sources of methylmercury in tree foliage,” Environmental Pollution, vol. 160, no. 1, pp. 82–87, 2012. View at: Publisher Site | Google Scholar
  64. L. Poissant, H. H. Zhang, J. Canário, and P. Constant, “Critical review of mercury fates and contamination in the Arctic tundra ecosystem,” Science of the Total Environment, vol. 400, no. 1-3, pp. 173–211, 2008. View at: Publisher Site | Google Scholar
  65. A. Adjorlolo-Gasokpoh, A. A. Golow, and J. Kambo-Dorsa, “Mercury in the surface soil and cassava, Manihot esculenta (flesh, leaves and peel) near goldmines at Bogoso and Prestea, Ghana,” Bulletin of Environmental Contamination and Toxicology, vol. 89, no. 6, pp. 1106–1110, 2012. View at: Publisher Site | Google Scholar
  66. N. Yoshimoto, E. Inoue, K. Saito, T. Yamaya, and H. Takahashi, “Phloem-localizing sulfate transporter, Sultr1;3, mediates re-distribution of sulfur from source to sink organs in Arabidopsis,” Plant Physiology, vol. 131, no. 4, pp. 1511–1517, 2003. View at: Publisher Site | Google Scholar
  67. P. Buchner, C. E. E. Stuiver, S. Westerman et al., “Regulation of sulfate uptake and expression of sulfate transporter genes in Brassica oleracea as affected by atmospheric H2S and pedospheric sulfate nutrition,” Plant Physiology, vol. 136, no. 2, pp. 3396–3408, 2004. View at: Publisher Site | Google Scholar
  68. WHO, Air quality guidelines for Europe. WHO Regional Publications European Series 91, World Health Organization Regional Office for Europe, Copenhagen, 2000.
  69. US OSHA, “Health and safety (Hg). Occupational Hazards,” 2007, March 2018, View at: Google Scholar
  70. EPA/ATSDR, “National Mercury Cleanup Policy Workgroup: action levels for elemental mercury spills,” 2012, February 2019, View at: Google Scholar
  71. M. L. I. Witt, T. P. Fischer, D. M. Pyle, T. F. Yang, and G. F. Zellmer, “Fumarole compositions and mercury emissions from the Tatun Volcanic field, Taiwan: results from multi-component gas analyser, portable mercury spectrometer and direct sampling techniques,” Journal of Volcanology and Geothermal Research, vol. 178, no. 4, pp. 636–643, 2008. View at: Publisher Site | Google Scholar
  72. A. Aiuppa, E. Bagnato, M. L. I. Witt et al., “Real-time simultaneous detection of volcanic Hg and SO2 at La Fossa Crater, Vulcano (Aeolian Islands, Sicily),” Geophysical Research Letters, vol. 34, no. 21, article L21307, 2007. View at: Publisher Site | Google Scholar
  73. E. Bagnato, P. Allard, F. Parello, A. Aiuppa, S. Calabrese, and G. Hammouya, “Mercury gas emissions from La Soufrière Volcano, Guadeloupe Island (Lesser Antilles),” Chemical Geology, vol. 266, no. 3-4, pp. 267–273, 2009. View at: Publisher Site | Google Scholar

Copyright © 2019 A. L. Gagliano et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

More related articles

 PDF Download Citation Citation
 Download other formatsMore
 Order printed copiesOrder

Related articles

Article of the Year Award: Outstanding research contributions of 2020, as selected by our Chief Editors. Read the winning articles.