Total (fumarolic + diffuse soil) CO2 output from Furnas volcano
Earth, Planets and Space volume 67, Article number: 174 (2015)
Furnas volcano, in São Miguel island (Azores), being the surface expression of rising hydrothermal steam, is the site of intense carbon dioxide (CO2) release by diffuse degassing and fumaroles. While the diffusive CO2 output has long (since the early 1990s) been characterized by soil CO2 surveys, no information is presently available on the fumarolic CO2 output. Here, we performed (in August 2014) a study in which soil CO2 degassing survey was combined for the first time with the measurement of the fumarolic CO2 flux. The results were achieved by using a GasFinder 2.0 tunable diode laser. Our measurements were performed in two degassing sites at Furnas volcano (Furnas Lake and Furnas Village), with the aim of quantifying the total (fumarolic + soil diffuse) CO2 output. We show that, within the main degassing (fumarolic) areas, the soil CO2 flux contribution (9.2 t day−1) represents a minor (~15 %) fraction of the total CO2 output (59 t day−1), which is dominated by the fumaroles (~50 t day−1). The same fumaroles contribute to ~0.25 t day−1 of H2S, based on a fumarole CO2/H2S ratio of 150 to 353 (measured with a portable Multi-GAS). However, we also find that the soil CO2 contribution from a more distal wider degassing structure dominates the total Furnas volcano CO2 budget, which we evaluate (summing up the CO2 flux contributions for degassing soils, fumarolic emissions and springs) at ~1030 t day−1.
Volcano-hosted hydrothermal systems are the source of sizeable carbon dioxide (CO2) emissions, either vented by hydrothermal steam vents (Chiodini et al. 1998) or diffusively released by degassing soils (Chiodini et al. 1999; Rogie et al. 2001; Werner et al. 2008). While considerable work has been spent in the past to estimate the soil CO2 flux from hydrothermal areas (e.g., Chiodini et al. 1999, 2001a; Hernández et al. 2001; Werner et al. 2008; Viveiros et al. 2010), far less is known on the CO2 output from hydrothermal fumarolic vents (Werner et al. 2000; Fridriksson et al. 2006; Aiuppa et al. 2013; Pedone et al. 2014a, b), which are technically more difficult to study. Consequently, the total (fumarolic + soil degassing) budget remains unconstrained for most hydrothermal systems in our planet (with a few exceptions; Aiuppa et al. 2013).
The aim of the present work is to provide more information on the fumarolic vs. diffusive contribution to the hydrothermal CO2 output. Our test site is Furnas volcano, a quiescent polygenetic volcano located in the eastern part of São Miguel island, in the Azores, an archipelago of nine volcanic islands located in the North Atlantic Ocean at the triple junction between American, Eurasian, and Nubian plates (Searle 1980). Furnas volcano has frequently been active in the Holocene (the oldest volcanic products are dated back 100,000 years BP; Moore 1990). The last “magmatic” eruption occurred in 1630 (Cole et al. 1995). In recent times, hydrothermal explosions have re-occurred (in 1840–1841, 1944, and 1990) from the hydrothermal vent (named “Asmodeu”) belonging to the Furnas Village fumarolic field (Ferreira, T: Contribuição para o estudo das emanações gasosas associadas a processos de vulcanismo no arquipélago dos Açores, unpublished Master thesis). Hydrothermal activity is widespread on the island and includes soil diffuse degassing areas (Ferreira et al. 2005; Viveiros et al. 2010), steaming ground, thermal springs, cold CO2-rich springs, and low-temperature fumaroles (95–100 °C), mostly concentrated inside the Furnas caldera (where three main fumarolic fields are observed; Viveiros et al. 2010; Caliro et al. 2015). Further studies have been done since the early nineties to study CO2 diffuse emissions. The first soil CO2 surveys (Baubron et al. 1994; Baxter et al. 1999) in the Furnas caldera identified a CO2 degassing area in the proximity of Furnas village. Recently, Viveiros et al. (2010, 2012) estimated the soil CO2 fluxes emitted from the Furnas volcanic system using the accumulation chamber method (Chiodini et al. 1998); this led to identifying the presence of several diffuse degassing structures (DDS). The diffuse hydrothermal-volcanic CO2 output from Furnas volcano (Furnas caldera and the southern Ribeira Quente village area) was estimated at ~968 t day−1 (Viveiros et al. 2010), and the groundwater CO2 transport was evaluated at ~12 t day−1 (Cruz et al. 1999). As for the majority of the hydrothermal system worldwide, the fumarolic CO2 output is unknown.
In this study, we use a tunable diode laser spectrometer (TDLS) to estimate, for the first time, the fumarolic output of volcanic/hydrothermal CO2 at Furnas volcano. The TDLS technique is based on measuring the absorption of IR radiation (at specific wavelengths) by a target gas, and can suitably be adapted to measure the flux of volcanic CO2 from low-temperature hydrothermal manifestations (Pedone et al. 2014a, b), where the use of traditional UV spectroscopy remote-sensing techniques is prevented by the absence of SO2. TDLS employs a light source of very narrow line-width that is tunable over a narrow wavelength range. In other words, tunable diode laser (TDL) steams on absorption spectroscopy using a single isolated absorption line of the target species, allowing positive identification and unambiguous measurement of complex gas mixtures. A major disadvantage is that TDLS applications are better suited to accurate measurement of a specific target gas (known to be present in the atmosphere) than for identification of previously unidentified species (Pedone et al. 2014a). In addition, the quality of the measurements can be limited in highly condensed, optically thick fumarolic plumes.
The fumarole observations were complemented by simultaneous soil CO2 measurements with an accumulation chamber. This is the first time in which two methodologies are applied together to evaluate their relative CO2 contributions to the total CO2 output. Our results, while limited to only one single hydrothermal system, offer new information to understand the modes of hydrothermal carbon release. In addition, the sulfur output from the fumarolic system is quantified based on measurement of the fumarole CO2/H2S ratios (obtained with a Multi-GAS detector).
The two most important fumarolic fields on Furnas are referred to as “Furnas Lake” and “Furnas Village” (see Fig. 1). A small steaming ground exists in the eastern part of the caldera, and the steam emissions are visible in the southern flank of the volcano (Ribeira Quente village).
Our field campaign was carried out in August 2014 in the two main fumarolic fields: Furnas Lake, on the north side of the lake, and Furnas Village, in the eastern side of the caldera (Fig. 1). Figure 2 shows a view of the Furnas Lake area during the campaign carried out on 19 August 2014. The TDL was used to measure the CO2 concentration in air close to and/or above three degassing vents (Fig. 2): a vigorously degassing vent with boiling water jet (WJ, close to mirror position 3 in Fig. 2); two smaller fumaroles located in the northwestern part of the area (ST, close to mirror position 2 in Fig. 2); and a mud pool degassing vent (MP, close to mirror position 5 in Fig. 2). Furnas Village (Fig. 3) is the largest fumarolic field in the Furnas caldera. Several moderate to large fumaroles are active within an area of several hundred square meters. “Caldeira Grande” and “Caldeira do Asmodeu” are the main hydrothermal vent manifestations, and are referred to as “CG” and “CdA” in the subsequent text and figures. These fumarolic fields have hydrothermal origin (Ferreira and Oskarsson 1999), with outlet temperatures lower than 100 °C (~97 °C at Lake and ~99 °C at Village; Caliro et al. 2015). The discharge of these fumaroles derive from the shallow hydrothermal aquifers originating from heating of infiltrated local groundwater. The main components are water vapor, carbon dioxide, hydrogen sulfide, nitrogen, hydrogen, oxygen, methane, and argon (Ferreira and Oskarsson 1999; Ferreira et al. 2005; Caliro et al. 2015).
Tunable diode lasers are increasingly used in environmental monitoring applications (Gianfrani et al. 1997a) and for volcanic gas observations (Gianfrani et al. 1997b, 2000; De Natale et al. 1998; Richter et al. 2002). Pedone et al. (2014a, b) recently reported on the first direct observations of the volcanic CO2 flux by using a portable tunable diode laser (TDL) system.
Like in previous studies (Pedone et al. 2014a, b), we used a GasFinder 2.0 Tunable Diode Laser (produced by Boreal Laser Inc.), a transmitter/receiver unit operating in the 1.3–1.7 μm wavelength range. GasFinder 2.0 is designed to measure CO2 concentrations over linear open-paths of <1 km. In order to achieve this, radiation emitted by the IR laser transmitter propagates to a set of gold-plated retroreflector mirrors, where it is reflected back to the receiver and focused onto a photodiode detector. The CO2 column amount (in ppm∙m) along each optical path is calculated by the spectral analysis of reflected light, converted into electrical waveform, and processed by using the procedure described in Tulip (1997). CO2 column amounts are converted into average CO2 concentrations (in ppm) along the path by considering path lengths (measured with an IR manual telemeter, 1 m resolution).
In the field, the GasFinder was set to measure CO2 concentrations at a 1-Hz rate (Pedone et al. 2014a), along an optical (transmitter-retroreflector) path positioned at ~1.20 m height above ground level. Alignment between the laser unit and the retro-reflectors was optimized using a red visible aiming laser and a sighting scope. The GasFinder acquired for several consecutive hours at Furnas Lake (on 19 August 2014) and Furnas Village (on 22 August 2014), totally ~3600 and ~3200 successful readings, respectively. The plumes were fairly transparent during the observations, and the main plume dispersals directions are indicated by rose diagrams in Figs. 4 and 5. Background CO2 concentrations were obtained in each of the measurement days/sites by pointing the laser beam toward a mirror, positioned upwind of the fumarolic area. These background values were subtracted in the calculation of integrated column amount (ICA) (see below).
In both days, the position of the GasFinder laser unit was sequentially moved (e.g., from positions A to E in Figs. 2 and 3) to scan the fumaroles’ atmospheric plumes from different angles and viewing directions. The positions of transmitter-receivers were limited by time-logistic constraints (e.g., morphology and accessibility of the degassing areas); given the geometry of the optical paths, we admit some heterogeneities in our CO2 maps (Figs. 4 and 5) may result from inhomogeneous, incomplete coverage of the degassing areas. During operations, the GasFinder was left to acquire data along each single GasFinder-retroreflector path for ~3–5 min, before being rotated to measure along the successive path (an additional documentation file shows more details of acquisition-paths (see A1 in Additional file 1).
We considered the possibility of combining the available data to derive a two-dimensional model of CO2 distribution, and ultimately—by combination with derived plume vertical transport speeds (Table 1)—to estimate the CO2 output from the main investigated fumaroles. The initial step was to use a Matlab script (Pedone et al. 2014a) to obtain a 2D reconstruction of CO2 concentrations in the investigated areas, starting from the raw GasFinder dataset. In order to begin calculation, the Matlab script was initialized with the coordinates of GasFinder unit and retroreflector positions (Figs. 2 and 3). The additional input data was a column vector containing the mean CO2 column amount (in ppm∙m) obtained for each GasFinder-retroreflector path. With these inputs, the script performed a data inversion using a least-squares method, whose outputs were then processed with a stochastic simulation approach (see Additional file 1: Table S3 and S4), using GSLIB executables (Deutsch and Journel 1998) to obtain the distribution maps of CO2 concentrations, shown in Figs. 4 and 5. For each area, the dataset was initially converted by normal score transformation to follow a Gaussian distribution. This normal score-transformed dataset was then used to compute omnidirectional variograms, and finally interpolated with the sequential Gaussian simulations (sGs) method to produce 100 realizations. The maps of Figs. 4 and 5 were produced averaging results of the 100 simulations, using the E-type post-processes method (Cardellini et al. 2003). Grid resolution interpolation parameters are listed in Additional file 1: Table S5. Zonal statistics on the CO2 distribution maps was obtained by using the ArcMap 9.3 (ESRI) Spatial Analyst tool (Additional file 1: Table S5).
To convert the CO2 maps into a CO2 flux, we performed 2D integration inside the areas covered by the fumarolic plumes—the boxes delimited by black dashed lines in Figs. 4 and 5. These integration areas were delimited based on visual (field) observations of plume transport direction, and were mapped so as to include concentration data above fixed concentration thresholds (~600 ppm at lake and ~650 ppm at village). No integration was performed outside these areas, where the CO2 contribution was due either to the degassing soils or smaller fumaroles (for which manifestations—as for mud pool “MP”—the gas speed is more difficult to assess). The so-obtained CO2 ICAs were multiplied by vertical gas transport speed to obtain a CO2 flux (Table 1). Plume vertical transport speed was estimated from recordings of a video camera, pointing toward the fumarolic vents, and acquiring sequences of images of the atmospheric plume at 25 frames per second. The sequences of frames were later post-processed to calculate the time-averaged transport speed of the plume, after converting camera pixels into distances (using a graduated pole, positioned close to the vent).
During the field campaigns, we used a Multi-GAS (Aiuppa et al. 2011, 2012 for information about setup and performance of the instrument) to measure the compositions of the main gas manifestations. In detail, the Multi-GAS was exposed to the atmospheric plumes of the main fumaroles (WJ at Furnas Lake and CG at Furnas Village; blue triangles in Figs. 2, 3, 4, and 5) to measure the concentrations of CO2 (by NDIR spectroscopy), SO2, and H2S (by specific electrochemical sensors). The specific sensors mounted onboard the Multi-GAS were as follows: a Gascard Edinburgh Instruments infrared spectrometer for CO2 (0-3000 ppmv range, with a resolution of 0.8 ppmv), a 0- to 200-ppmv SO2 electrochemical sensor, and a 0- to 50-ppmv H2S electrochemical sensor (all from City Technology, and the manufacturer quoted a resolution of 0.5 ppmv). We also used a temperature-humidity Galltec sensor (T range, −30 to 70 °C; Rh range, 0–100 %). The Multi-GAS sensors were calibrated in the laboratory by using standard gas cylinders of concentrations within the sensor ranges (all in nitrogen matrixes). Laboratory tests indicate a typical measurement error in the CO2/H2S ratios of ≤20 %.
In both areas, we also performed a detailed soil CO2 flux survey using a portable accumulation chamber (Chiodini et al. 1998). A chamber of a known volume is placed on the soil surface, the variation of CO2 concentration is measured, and the CO2 flux is calculated from the increase rate of the CO2 concentration. The portable chamber is equipped with a LICOR LI-800 infrared CO2 detector that measures CO2 concentrations in the range 0–2 vol %. Calibration of the instrument was performed in the laboratory prior to field work. Considering that soil gas fluxes may be highly affected by meteorological conditions (e.g., Viveiros et al. 2008), measurements were performed during stable weather conditions and the CO2 flux values recorded in a permanent soil CO2 flux station (named GFUR2) used as control site; this station is installed close to Furnas Lake fumarolic field (Fig. 4). Soil CO2 fluxes in the permanent station showed a coefficient of variation (ratio between standard deviation and average value) of 0.02 and 0.03 during the surveys carried out in 19 and 22 August 2014, respectively, at Furnas Lake and Furnas Village fumarolic fields. At Furnas Lake, a total of 124 measurements were carried out in an area of approximately 3666 m2. At Furnas Village, a total of 95 soil CO2 flux measurements were carried out in an area of about 2300 m2. A sampling space varying between 3 and 5 m was used in these detailed surveys. The grid used was as regular as possible, considering the presence of steam vents, water streams, irregular topography, and some man-made structures in the study sites. The CO2 flux values were interpolated using sGs (Deutsch and Journel 1998; Cardellini et al. 2003), which consists in the production of numerous simulations of the spatial distribution of the CO2 flux. Considering that data has to follow normal distribution in order to apply sGs, normal score transformation was applied to the original data. Similarly as described above, in this case, omnidirectional variograms of normal scores for the two surveyed areas were also computed (Fig. 6). One-hundred realizations of the flux grid were created for each study site. Parameters used in the sGs procedure are available in A3 section of Additional file 1: Tables S6 and S7. The CO2 output was calculated by integrating the average values estimated from sGs over the area. The mean and the standard deviation computed for the 100 realizations are, thus, assumed to be, respectively, the CO2 output (Fig. 7) and its uncertainty for each area.
Results and discussion
TDL-based CO2 distribution maps
Figure 4 is a distribution map of atmospheric CO2 concentrations, calculated for a horizontal air cross-section taken at a 1.20-m height above the degassing soil and fumaroles of Furnas Lake (see Fig. 4). The calculated CO2 concentration values range from ~390 to >850 ppm. In detail, the lowest CO2 concentrations are detected in the eastern portion of the investigated area, far from the fumarolic field (close to laser positions B–E in Fig. 4). In contrast, two main clusters of higher CO2 concentrations (>580) are detected on the northern, northwestern, and western portion of the map, in the proximity of the main degassing fumarolic vents (crosses). Peak CO2 concentrations (>850 ppm), in particular, are observed close to the fumaroles WJ, MP, and ST (Fig. 4). It is worth noting that the CO2 peaks appear in the map as shifted toward the east-southeast relative to the fumaroles’ positions, in agreement with the prevalent plume transport direction during the observations (see wind rose diagram in Fig. 4).
Figure 5 is a similar map derived from interpolation of the GasFinder dataset acquired during operation field at Furnas Village. Again, the CO2 concentration anomalies are fairly consistent with the location of the main visible degassing areas. CO2 concentrations (~700–800 ppm) peak in a wide degassing area downwind (west of) fumarole CdA (the dominant plume transport directions during the observations were toward NW and SW; Fig. 5). A secondary, more moderate CO2 anomaly is observed north of CG fumarole. In contrast, the lowest CO2 concentrations are detected along paths A4 and E6, respectively, upwind and/or more remote from the fumaroles (Fig. 5; Additional file 1: Table S2).
Soil CO2 flux degassing
Soil CO2 fluxes (derived by using the accumulation chamber method) varied between 6 and 28,231 g m−2 day−1 in the Furnas Lake area, with a mean value of 1510 g m−2 day−1. For the Furnas Village fumarolic ground, soil CO2 flux average value was 1279 g m−2 day−1. Minimum and maximum values were, respectively, 5 and 22,154 g m−2 day−1 in this site (Table 2). Experimental variograms show spherical and Gaussian structures, respectively, for Furnas Lake and Furnas Village datasets (Fig. 6). The high nugget effect associated to Furnas Village (Fig. 6b) detailed survey is probably explained by the soil heterogeneities in this fumarolic ground, where the soil alteration causes large differences in the permeability at small scales. This behavior was previously observed by Viveiros et al. (2010) for data acquired in the same sampling sites. Figure 7 shows the soil CO2 flux distribution maps for Furnas Lake and Furnas Village fumarolic ground.
Multi-GAS in-plume measurements
The Multi-GAS detected strong volcanic CO2 and H2S signals in both areas. SO2 was undetected (<0.05 ppmv) at both sites, and the relative humidity in the plumes ranged 30–50 % and 40–60 % at Furnas Lake and Village, respectively. The relative humidity variations in the plumes did not systematically correlate with changes in either CO2 or H2S, precluding the volcanic H2O signal to be clearly resolved.
An example of Multi-GAS acquisition is shown in Fig. 8, in which the CO2 and H2S signals detected in 215 measurements close to “WJ” degassing vent were plotted. At Furnas Lake, the Multi-GAS derived compositions of the plumes of the main jet-water degassing vent (WJ; Figs. 2 and 4) are consistent with literature data based on direct fumarole sampling. We obtain a mean Multi-GAS-based CO2/H2S plume (molar) ratio of 353, which fits well with the mean ratio of 348 observed in an earlier chemical survey of the fumarole (Ferreira and Oskarsson 1999). At Furnas Village, the mean CO2/H2S plume ratio of 150 measured by the Multi-GAS at the CG fumarole (Figs. 3 and 5) is not far from the mean fumarolic ratio of 120 of Ferreira and Oskarsson (1999). The CO2/St ratios of Furnas fumaroles (this study) are similar to those seen in other hydrothermal fluids of similar outlet temperatures. For example, the CO2/St ratio detected at Furnas Lake is close to that quoted by Aiuppa et al. (2013) for Pisciarelli fumaroles of Campi Flegrei (CO2/St ratio of 300, range 210–410) and by Chiodini et al. (2001b) for Vesuvius fumaroles (CO2/St ratio of 342). The CO2/St ratio detected at Furnas Village is comparable with compositions of fumaroles at Solfatara crater, Campi Flegrei (CO2/St ratio of 130, range 120–152; Aiuppa et al. 2013) and Ischia (CO2/St ratio of 119; Chiodini et al. 2004).
CO2 and H2S output
We estimated the fumarolic CO2 output from Furnas volcano by 2D integration of the TDL-based CO2 concentration values. This integration was restricted to the shaded box areas of Figs. 4 and 5, downwind the main fumaroles. These integrated CO2 amounts within the defined areas were finally multiplied by the vertical gas transport speeds to calculate the fluxes (Table 1). The so-estimated fumarolic CO2 fluxes were ~29 t day−1 at Furnas Lake (17.6 ± 5.3 t day−1 emitted from WJ and 11.4 ± 4.7 t day−1 from ST) and ~21 t day−1 at Furnas Village (17.8 ± 4.1 t day−1 emitted from CdA and 3 ± 0.8 t day−1 from CG) (Table 1). The cumulative fumarolic output from the two areas is therefore ~50 t day−1.
We additionally infer, using this fumarolic CO2 flux (Table 1) and the Multi-GAS-derived CO2/H2S ratios, fumarolic H2S fluxes of 0.08 t day−1 (Furnas Lake) to 0.17 t day−1 (Furnas Village), respectively. Our results indicate that Furnas fumaroles are weak, but yet not negligible, sources of S. The present-day H2S flux of 0.25 t day−1 (0.08 + 0.17 t day−1) at Furnas is nearly 1 order of magnitude lower than typical emissions from Campi Flegrei volcano (1.5–2.2 t day−1; Aiuppa et al. 2013), which similarly display a H2S-dominated flux and more than 1 order of magnitude lower than emissions from Vulcano Island (6–9 t day−1; Tamburello et al. 2011), whose fumarolic field hosts hot (>400 °C) magmatic fumaroles. For comparison, the H2S flux sustained by Etna, the largest source of volcanic gases worldwide, is 200 to 400 times larger (50 to 113 t day−1; Aiuppa et al. 2005) (note Etna additionally emits thousands of tons of SO2 every day; Caltabiano et al. 2004).
On the basis of the integration of the average of 100 sequential Gaussian simulations (Deutsch and Journel 1998; Cardellini et al. 2003), over the sampled area, mean soil diffuse CO2 emissions of ~6 ± 0.2 t day−1 and 3.2 ± 0.2 t day−1 were estimated for Furnas Lake and Furnas Village degassing areas, respectively. We then obtain a cumulative soil CO2 release of ~9.2 t day−1. Detailed soil CO2 surveys in the Furnas Lake and Furnas Village fumarolic fields (same as Fig. 7 in this study) have previously been performed by Viveiros et al. (2012). For the sake of comparison, we extracted from these earlier surveys (made between 2008 and 2009) the results obtained in the same areas as those investigated in the present study (2014) (Fig. 7). This comparison shows that the Furnas Lake area emitted in 2008 about 3 t day−1 of CO2, or about half of what was measured in 2014. Similarly, the Furnas Village area was found in 2009 to emit nearly half (1.7 t day−1) of the amount of CO2 released in 2014 (3.2 ± 0.2 t day−1). Increased CO2 emissivity in 2014 is consistent with the different average CO2 flux values observed in the two different surveys (Table 2) but is not supported by records of the permanent soil CO2 flux station GFUR2 (where lower soil CO2 flux values—about 250 g m−2 day−1—were recorded during 2014 compared to 2008 and 2009 surveys—values higher than 350 g m−2 day−1). We caution that differences in sampling grid/density (that was significantly higher in the present surveys, as can be also observed in the number of points of Table 2) can partially explain the CO2 flux diversity between the two campaigns (Viveiros et al. 2010).
Our results here suggest that, in the actively degassing fumarolic areas of Furnas, fumarolic vents, with their cumulative fumarolic output of ~50 t day−1, dominate the total CO2 degassing budget (~59 t day−1) and overwhelm the relatively marginal contribution (~15 %) of soil diffuse degassing. While the fumarolic output can be locally important, however, its contribution to the total CO2 degassing output becomes marginal at the scale of the entire volcano. Earlier soil CO2 flux measurements, in fact, have demonstrated a total diffusive hydrothermal CO2 release at Furnas, from an area (6.2 km2) far larger than that studied here, as high as 968 t day−1 (Viveiros et al. 2010). From this comparison, we conclude that—at Furnas—the most actively degassing areas, although featuring the most visible (e.g., fumaroles, hot pools) and spectacular manifestations of thermal activity, in no way correspond to the areas of largest CO2 output: in total, the actively degassing areas contribute only about 5 % to the total CO2 output.
To what extent this conclusion can be generalized to other hydrothermal-volcanic systems remains unknown, given the paucity of information we have in hand. A small contribution of fumarolic gas vents to the total CO2 budget was also suggested by Fridriksson et al. (2006) for the Reykjanes geothermal area, SW Iceland, where the contribution of steam vents/mud pools is only about 3 % of the soil CO2 degassing output. In other systems, in contrast, the contribution of fumaroles is manifestly more significant. At Mud volcano (Yellowstone, USA), for example, Werner et al. (2000) estimated that fumarolic vent emissions contribute to more than 32 % of the total degassing; based on statistical approach, the authors even suggested that the hydrothermal-focused emissions can be responsible for up to 63 % of the total degassing in that thermal area. At Campi Flegrei, the CO2 fumarolic output of ~500 t day−1 (range, 460–507 t day−1, Aiuppa et al. 2013; Pedone et al. 2014a) makes a substantial contribution to the total CO2 output, which is still dominated by soil diffuse degassing (~1100 ± 120 t day−1; Chiodini et al. 2010). From these examples, we argue that much remains to be done to fully understand the fumarolic vs. diffusive gas contribution at volcano-hydrothermal systems. The relative significance of the fumarolic output can differ significantly from one volcano to another. A general conclusion is that the relative significance of the above two forms of gas dissipation will likely be dependent upon the scale at which the comparison is made. At the local scale of an active hydrothermal manifestation, the fumarolic output will likely overwhelm the soil diffuse flux, while the latter will most likely dominate at a larger scale (at the scale of an entire volcanic complex). For example, based on results from 20 analyzed hydrothermal areas, Harvey et al. (2015) concluded that the contribution of focused venting to the total CO2 emission is typically less than 10 %. The TDL, with the ability to characterize the fumarolic CO2 output, promises to contribute a substantial advancement in this field in the following years.
We estimated the total CO2 emissions from the main thermal manifestations of Furnas volcano by jointly using two different techniques: the GasFinder 2.0 tunable diode laser and the accumulation chamber method. We find that, in the most vigorously degassing areas, the soil CO2 flux contribution (approximately 9.2 t day−1) represents a minor (~18 %) contribution to the total CO2 output, which is dominated by the fumaroles (about ~50 t day−1). The CO2 output contributed by the fumaroles is larger than that contributed by Furnas springs (~12 t day−1, Cruz et al. 1999), but far lower than the total hydrothermal diffuse degassing flux (~968 t day−1) at the scale of the entire volcano. This observation supports the conclusions that although fumaroles are the most visible surface manifestations of thermal activity, they are not necessarily the biggest contributors to the total CO2 output from quiescent, Solfatara-stage volcanoes, where CO2 is mainly released in silent, invisible form through soil emissions.
Summing up the CO2 flux contributions for the fumarolic emissions, the degassing soils and the springs (12 t day−1, Cruz et al. 1999), the total volcanic/hydrothermal CO2 output for Furnas volcano is estimated to be ~1030 t day−1. These results show once more the importance of taking into consideration both soil degassing and gas vent emissions to estimate the CO2 emission in hydrothermal areas, since their relative contribution seems to be quite different depending on the study sites. Using a portable Multi-GAS, we also obtained the CO2/H2S ratio signature for the investigated fumaroles, and concluded that the Furnas fumaroles are, in their present state of activity, weak, but yet not negligible, sources of H2S (~0.25 t day−1).
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The research leading to these results has received funding from the European Research Council under the European Union’s Seventh Framework Programme (FP7/2007/2013)/ERC grant agreement n 305377, and from the FP7 grant “Futurevolc.” F. Viveiros is supported by a post-doctoral grant from Fundação para a Ciência e a Tecnologia (FCT). The authors would like to acknowledge the technical assistance from the staff of Centro de Vulcanologia e Avaliação de Riscos Geológicos, University of the Azores, and the staff of INGV (Istituto Nazionale di Geofisica e Vulcanologia) of Palermo, Italy. The authors would also like to thank the two reviewers, Dr. C. Werner and Dr. H. Shinohara, for the valuable contribution to improve the early version of the manuscript.
The authors declare that they have no competing interests.
MP and FV carried out the field campaigns and drafted the manuscript. AA allowed the work realization and actively contributed to drafting the manuscript. GG, FG, and TF provided important suggestions during data processing. FV and ALG provided useful suggestions/help in the maps elaboration. VF provided technical assistance in laboratory. All authors have read and approved the final manuscript.
MP is a Dr. in geochemistry at DiSTeM (Dipartimento di Scienze della Terra e del Mare) of Palermo University and has a study grant at INGV (Istituto Nazionale di Geofisica e Vulcanologia) of Palermo. FV has a post-doc grant from Fundação para a Ciência e Tecnologia (FCT) and is a researcher at Centro de Vulcanologia e Avaliação de Riscos Geológicos (CVARG) of the University of the Azores. AA is Associate Professor of Volcanology and Geochemistry at DiSTeM (Dipartimento di Scienze della Terra e del Mare) of Palermo University and Associate Researcher at Istituto Nazionale di Geofisica e Vulcanologia (Sezione di Palermo). GG is first engineer at Istituto Nazionale di Geofisica e Vulcanologia (Sezione di Palermo). FG is a researcher at Istituto Nazionale di Geofisica e Vulcanologia (Sezione di Palermo). ALG is a Dr. in geochemistry at DiSTeM (Dipartimento di Scienze della Terra e del Mare) of Palermo University and has a study grant at INGV of Palermo. VF is a technician at Istituto Nazionale di Geofisica e Vulcanologia (Sezione di Palermo). TF is Associate Professor in the Department of Geosciences (University of the Azores) and Researcher at Centro de Vulcanologia e Avaliação de Riscos Geológicos (CVARG).
The supplementary file is a more detailed documentation about the TDL acquisitions and data elaboration. A1. CO2 TDL-datasets. A2. Parameters used to perform sGs with CO2 concentrations TDL data and Zonal Statistic on E-Type maps. A3. Parameters used to perform sGs with soil CO2 flux data (accumulation chamber). In A1 section, each path laser-retroreflector acquisition during the campaigns carried out at Furnas Lake (Additional file 1: Table S1) and Furnas Village (Additional file 1: Table S2) is shown. In A2 section, more details about statistical approach and elaboration of data to create the distribution CO2 concentration maps are shown (Additional file 1: Tables S3, S4, and S5). Finally, parameters used to perform sGs with soil CO2 flux data are shown in A3 section (Tables S6 and S7).
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Pedone, M., Viveiros, F., Aiuppa, A. et al. Total (fumarolic + diffuse soil) CO2 output from Furnas volcano. Earth Planet Sp 67, 174 (2015). https://doi.org/10.1186/s40623-015-0345-5