Carbon dioxide emission from Katanuma volcanic lake, Japan
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2011
Received: 21 October 2010
Accepted: 22 June 2011
Published: 14 February 2012
We report herein the first results of a CO2 efflux survey carried out at Katanuma volcanic lake, Japan. A total of 110 CO2 efflux measurements were undertaken at the lake by means of the floating accumulation chamber method during August 2010 to estimate the total CO2 output from the studied area. Two different mechanisms of degassing were observed during the survey; (1) diffusion through the water-air interface and (2) bubbling. CO2 efflux values ranged from 0.5 up to 322 g m−2 d−1. In addition, the probability graph was used to distinguish the existence of different geochemical populations in the measured values. Sequential Gaussian Simulation was used to construct a map of CO2 efflux from 200 simulations and to compute the total CO2 diffuse emission at the studied area, i.e., 17 ± 0.6td−1.
Key wordsDiffuse CO2 degassing volcanic lake Katanuma Naruko
During the last two decades, studies of the spatial distribution of soil CO2 efflux has become an ideal geochemical tool for monitoring volcanic activity (Hernandez et al., 2001a, b, 2006; Granieri et al., 2006; Perez et al., 2011). Several authors have demonstrated that continuous monitoring of CO2 efflux provides important information for volcanic surveillance and seismotectonic monitoring (Salazar et al., 2002; Carapezza et al., 2004; Pérez et al., 2006). Other studies have shown that diffuse CO2 emissions from active volcanoes are of the same order of magnitude as the CO2 released by visible emanations (plumes, fumaroles, etc), pointing out the importance of estimating the total diffuse CO2 output from volcanic areas (Baubron et al., 1990; Allard et al., 1991; Hernandez et al., 1998, 2001a; Salazar et al., 2001). Since the rate of diffuse CO2 emission can increase greatly before the occurrence of a volcanic eruption (Hernandez et al., 2001a; Carapezza et al., 2004), it is very important to map surface CO2 efflux anomalies and to estimate the total output of this gas regularly in order to have a better understanding of on-going volcanic processes (Salazar et al., 2001).
During the last years, several studies have focused on CO2 emission from volcanic lakes. Volcanic lakes are generally formed by one of three mechanisms: 1) explosive excavation (crater lakes), 2) collapse of volcanic edifices (caldera lakes), and 3) blockage of common waterways (rivers, streams) by mudflows, lava flows or ash (http://www.wesleyan.edu/ees/JCV/vloverview.html). After the gas disasters at lakes Monoun (1984) and Nyos (1986), both in Cameroon (Sigurdsson et al., 1987; Sigvaldason, 1989), accumulation of CO2 in these lakes has been well known by the scientific community. This led to the recognition that volcanic lakes are hazardous (Le Guern and Sigvaldason, 1989, 1990; Evans et al., 1994; Kling et al., 2005; Kusakabe et al., 2008). Since a large amount of magmatic gases is dissolved in water, CO2 degassing from volcanic lakes should be a process to be taken into account (Pérez et al., 2011). Degassing through the lake surface occurs by bubbles (convective/advective degassing) or by diffusion through the water/air interface (Mazot and Taran, 2009). In order to measure the gas flux from crater lakes, it may be the only way to measure fluxes at the lake surface.
This work presents the first results of a CO2 efflux measurement carried out in August 2010 at Katanuma lake, Japan. The main goals of this work are: 1) to study the spatial distribution of diffuse CO2 degassing from this volcanic lake; 2) to discriminate diffusive degassing from degassing by bubbling); 3) to estimate the total output of CO2 emitted to the atmosphere from the study area.
2. Geological Setting
Lake Katanuma is dimictic and covered by ice from January to mid-March. Inverse stratification occurs under the ice cover. After turnover in March, weak stratification develops with a thermocline at a depth of 3–5 m. Stratification is generally observed from April to late August. The circulation period is from late August to December (Takagi et al., 2005).
3. Procedures and Methods
Surface CO2 efflux, water temperature and water pH maps for Katanuma lake were constructed using Conditional sequential Gaussian simulations (sGs) provided by the sgsim program (Deutsch and Journel, 1998; Cardellini et al., 2003). In order to characterize the chemical and isotopic composition of the bubbling gas from Katanuma lake, gas samples were collected and gas composition was analyzed later in the laboratory. Gas composition was analyzed by combining a Varian CP-3800 gas chromatograph with Ar as the carrier gas and a Quadrupole Mass Spectrometer (QMS) model Pfeiffer Omnistar 422. The 13C/12C ratio of CO2 (expressed as δ13C-CO2 ‰ vs. V-PDB) was determined with a Thermo-Finnigan MAT 253 mass spectrometer at the ITER laboratory. The analytical error for δ13C values is ±0.1‰. Elemental abundances of He and Ne, and He isotope composition of the gas samples collected in a 50 cm3 lead glass bottle with high vacuum stopcocks were analyzed in the laboratory of the Geochemical Research Center, The University of Tokyo. A magnetic-sector mass spectrometer VG 5400 was used for the analysis following the methodology described by Sumino et al. (2001).
4. Results and Discussion
Inspection of the CO2 efflux contour map for Katanuma lake (Fig. 7) shows the existence of three anomalous areas of CO2 degassing through the lake surface without a clear emission trend. High CO2 efflux values were always measured nearby visible gas bubbling emanations and located above the deepest areas of the lake, south and northeast basins of the lake, where hot springs are thought to issue. Figure 8(a) shows water temperature contour map for Katanuma lake together with bathymetric contour lines. Even when there is a homogeneous distribution of temperature at the surface of the lake, some slight increase in temperature was observed at the southern most part of the lake. To estimate the total output of diffuse CO2 released from Katanuma lake, we considered the contribution of each cell obtained after SGS and the average of the 200 simulations to estimate the total output with one standard deviation as the uncertainty. The result was 17±0.6td−1 for diffuse CO2. This value is smaller than the emission rates reported for other volcanic lakes (Pérez et al., 2011). However, in order to compare individual CO2 emission of various volcanic lakes, it is important to consider the lake-type and the area. Figure 8(b) shows water pH contour map for Katanuma lake together with bathymetric contour lines. Most of the surface water showed an almost homogeneous acidic pH (∼2.0) distribution. Katanuma, as an acid lake with an area of 1.26 × 105 m2, would have a normalized CO2 emission of 136 t d−1 km−2, a value close to that from other acid volcanic lakes in the world (Pérez et al., 2011).
As reported by Takagi et al. (2005), Katanuma lake circulates from late August to December and stratifies from April to late August. Our survey was carried out at the beginning of the monomictic circulation period (August), which significantly reduces accumulation of CO2 in the deepest part of the lake, and maximizes CO2 emission to the atmosphere. During the overturn period, when the present study was carried out, the emission of CO2 is mainly diffusive, advective and convective, showing the maximum CO2 emission in the year. In order to evaluate the CO2 emission from the bubbling spots, we measured the CO2 flux from 10 spots using the same method. We visually counted approximately 100 bubbling spots and assumed an average CO2 emission rate per bubbling spot of 14 kg d−1. Under the above assumption we estimated a total CO2 emission of 1.4 t d−1 from bubbling degassing. As a whole, adding diffuse and visible bubbling degassing, the total CO2 emission from Katanuma is estimated to be 18.4 td−1.
Since water from Katanuma lake is acidic (pH ∼2.0), almost all CO2 is present as dissolved CO2 and will diffuse out of the water, allowing volcanic gas fluxes to be channeled through the acid lake. Therefore, 18.4 td−1 of CO2 can be considered as a deep-seated CO2 emission from Katanuma lake, because relatively high CO2 efflux values were measured during this survey including data from all geochemical populations (16.6–322gm−2 d−1).
Chemical and isotopic compositions of bubbling gases were analyzed to constrain the origin of the gases emitted through the water of Katanuma lake. Bubbling gases are clearly CO2-dominated (72.6%V) and contain He (10 ppmV), O2 (4.6%V), N2 (22.5%V), Ar (0.2%V) and CH4 (477 ppmV) in minor amounts. N2/Ar ratio at the Katanuma bubbling gases (112.5) is notably higher than the air ratio (83.6) and air-saturated water (ASW; ∼36.8), indicating an additional non-atmospheric N2 source, typical for arc volcanoes. Measured δ13C-CO2 value for Katanuma bubbling gases (−1.59±0.03‰) is heavier than MORB values of −6.5±2.5‰ (Pineau and Javoy, 1983; Taylor, 1986). The measured value indicates a typical isotopic composition for gases from volcanic arcs (e.g. Taylor, 1986; Marty et al., 1989; Sano and Marty, 1995; Sano and Williams, 1996; Pedroni et al.1999; Shaw et al.2003).
The 3He/4He ratio was also measured at 3.46±0.06 Ra, where Ra denotes the atmospheric 3He/4He ratio (1.4 × 10−6, Mamyrin et al.1970). The relatively low 4He/20Ne ratio of the sample (3.73) is higher than that of the atmosphere (0.318), but still suggests atmospheric contamination of the sample. The measured 3He/4He ratio is similar to the value of 4.86±0.17 Ra reported by Asamori et al (2010) from the hot spring nearest to Naruko volcano. The value supports the existence of a hydrothermal system which supplies materials from underlying magma. In general, He in natural gases is composed of three components: atmospheric He, crustal or radiogenic He, and primordial He derived from the upper mantle. In order to estimate the mixing ratio of these components using the observed 3He/4He and 20Ne/4He ratios, we followed the methodology proposed by Sano et al. (1982). The calculated contribution for each component was 35.9%, 55.6% and 8.5% for MOR-type (upper mantle), crustal and air, respectively. The large contribution of the upper mantle He in Katanuma gas sample confirms active magmatic activity beneath the Naruko-Katanuma volcanic system.
Bubbling springs with lower gas/water ratios generally show higher 3He/4He ratios and consequently lower CO2/3He ratios (Rouwet et al, 2009). As He is less soluble in water than CO2 (Stephen and Stephen, 1963), and 3He is lighter than 4He, gases liberated from a weakly bubbling spring tend to be enriched in 3He during near-surface degassing processes and vapour separation in an aqueous hydrothermal system. This has been observed in the other volcanic areas, e.g. Tacaná volcano in Guatelama (Rouwet et al, 2009).
In order to detail deep magmatic and near-surface physical degassing processes at Katanuma lake, we have calculated the CO2/3 He ratio of the bubbling gas. The CO2/3He ratio is 1.54 × 1010, a value that fits well with the average value established for worldwide arcs (1.5 ± 1.1 × 1010; Sano and Williams, 1996). The three-component mixing model reported by Sano and Marty (1995) to calculate relative proportions of carbon sources contributing to arc magmas; MORB (M), marine limestones (L) and organic sediments (S) was used to estimate the fraction of each C source for Katanuma gas sample. L source contributes 53.6%, S source 3.6% and the M source 42.8%. These values are in the same order than the reported by Sano and Marty (1995) for bubbling gas and fumarolic gas samples from Japanese volcanic areas, with limestones as the main C component followed by the MORB-type C. Organic sedimentary C fraction is relatively low (3.6%), suggesting that the fumarolic feeding system beneath Katanuma lake corresponds to high temperature fumaroles.
CO2 efflux measurements were performed at the surface of Katanuma, a volcanic lake in Japan, by using the floating accumulation chamber method. This study allowed an estimation of 17±0.6td−1 as total diffuse CO2 emission and ∼1.4 t d−1 as CO2 emitted from bubbling spots. Chemical and isotopic analyses of bubbling gas samples from the Katanuma lake indicate a strong magmatic contribution to the gases with CO2 as the dominating gas species. To perform regular diffuse CO2 emission surveys at Katanuma lake would be important for detecting possible changes in the activity of the volcano.
This research was supported by the Japan Society for the Promotion of Science (Ref.: L10522) and the Cabildo Insular de Tenerife (Canary Islands, Spain). We are grateful to Katanuma boat rental office for their help during the field work and logistic support. The authors also want to thank M. Kusakabe and an anonymous reviewer for the constructive reviews of this manuscript as well as T. Hernan for the English reviewing.
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