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vol.48 número1Major and trace element geochemistry of El Chichón volcano-hydrothermal system (Chiapas, México) in 2006-2007: implications for future geochemical monitoringNon-methane Volatile Organic Compounds (VOCs) at El Chichón volcano (Chiapas, México): Geochemical features, origin and behavior índice de autoresíndice de materiabúsqueda de artículos
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Geofísica internacional

versión impresa ISSN 0016-7169

Geofís. Intl vol.48 no.1 Ciudad de México ene./mar. 2009




CO2 flux from the volcanic lake of El Chichón (Mexico)


A. Mazot* and Y. Taran


Instituto de Geofísica, Universidad Nacional Autónoma de México, Del. Coyoacán, 04510 México City, México E–mail: * Corresponding author:


Received: July 1, 2008
Accepted: September 19, 2008



El flujo de dióxido de carbono fue medido en marzo de 2007 en la superficie del lago del Volcán El Chichón, México, usando el método de la cámara de acumulación flotante. Los resultados de 162 medidas y la aplicación del método estadístico estándar, desarrollado para estos estudios, demuestran que la tasa de emisión total de CO2 del lago cratérico es relativamente alta. La tasa de emisión total calculada con simulación secuencial Gaussiana fue de 164 ± 9.5 t.d–1 para el área de superficie del lago de 138, 000 m2.

Se proponen dos mecanismos diferentes de desgasificación (por difusión a través de la interfase agua–aire y por burbujas) después de usar el método estadístico gráfico (GSA). Los flujos más altos fueron observados a lo largo de trazas de fallas deducidas. Una desgasificación alta también fue observada a lo largo de lineamentos que concuerdan con fallas que afectan el basamento de la región. Si se considera que el flujo promedio de CO2 comprendiera todo el fondo del cráter (308,000 m2) se tendría una emisión total del cráter del Volcán El Chichón de por lo menos 370 t.d–1. Este flujo sería cinco veces más alto que el del lago volcánico de Kelud, Indonesia y similar al flujo de CO2 de otros volcanes activos con desgasificación pasiva en el mundo.

Palabras clave: Flujo de CO2, cámara de acumulación, lagos cratéricos, El Chichón.



Carbon dioxide flux was measured in March 2007 at the surface of the volcanic lake of El Chichón volcano, Mexico using the floating accumulation chamber method. The results of 162 measurements and the application of a standard statistical approach developed for these studies showed that the total CO2 flux from the crater lake is relatively high. The total emission rate calculated by sequential Gaussian simulation was 164 ± 9.5 t.d–1from the 138,000 m2 area of the lake. Two different mechanisms of degassing (diffusion through the water–air interface and bubbling) are well resolved by a graphical statistical approach (GSA). The highest fluxes were observed along inferred fault traces. Elevated degassing was also observed along main basement faults in the area. The average flux of CO2 over the entire crater floor of El Chichón (~ 308,000 m2) is inferred to exceed 370 t.d–1. Thus the total emission rate of CO2 from El Chichón crater is five times higher than at Kelud volcanic lake, Indonesia, but is similar to emission rates from other passively degassing active volcanoes worldwide.

Key words: CO2 flux, accumulation chamber, crater lakes, El Chichón.



Geochemical monitoring of active volcanoes generally includes a periodical or continuous study of the chemistry and/or fluxes of fluids released from the volcano crater or from the volcano edifice where active hydrothermal manifestations are present. In addition to spectroscopic remote sensing of volcanic plumes and direct sampling of fumaroles and hot springs, measurements of the soil diffuse CO2 degassing by using the method of "accumulation chamber" has become a standard monitoring tool in volcanic and geothermal environments over the last 20 years (e.g. Chiodini et al., 1998). Temporal variations in CO2 fluxes can be related to changes in the volcanic activity and may be important for the mitigation of the volcanic risk (Hernández et al., 2001a, Notsu et al., 2005). Fluxes of volcanic CO2 by diffuse degassing through crater floors (Koepenick et al., 1996) or volcanic flanks can be comparable with plume degassing (Wardell et al., 2001). Volcanic craters occupied by a lake include Ruapehu in New Zealand, Poas in Costa Rica, Santa Ana in El Salvador, Kelud in Indonesia and El Chichón in Mexico. In order to measure the gas flux from crater lakes it is necessary to measure fluxes at the water lake surface. Degassing through the lake surface occurs by bubbles (convective/advective degassing) or by diffusion through the water/air interface. Early measurements of diffuse degassing from lakes by using the "floating accumulation chamber" method were made by Kling et al. (1991) for studying biogenic CO2 production from an Arctic lake. Bernard et al. (2004) and Mazot (2005) were the first to use this method in a volcanic lake (Santa Ana in El Salvador and Kelud in Indonesia).

In this work, we report the first data on CO2 flux from the surface of the crater lake of El Chichón volcano, Mexico, obtained in March 2007. The aims of this work were (1) to quantify the total CO2 output from the volcanic lake and the whole crater, (2) to discriminate between mechanisms of degassing (diffusive or by bubbling); (3) to build a CO2 flux map of degassing patterns from the lake bottom and relate them to local tectonics.

Finally, the total emission rate of CO2 from El Chichón volcano is compared with those from other volcanic sites.


General setting

The El Chichón dome complex (17.36N, 93.23W; 1,100 m.a.s.l.) is located in the northwestern part of the State of Chiapas in southeastern Mexico and halfway between the southeastern end of the Trans–Mexican Volcanic Belt (TMVB) and the northwestern end of the Central American Volcanic Arc (CAVA) (Fig. 1A). Prior to the 1982 eruption, the volcanic structure consisted of two nested andesitic lava domes (maximum elevation of 1260 m a.s.l.) inside a somma crater (Macías et al, 2003; Layer et al., this issue). The 1982 eruption of El Chichón volcano ejected 1.1 km3 of anhydrite–bearing trachyandesite pyroclastic material to form a new 1–km–wide and 200–m–deep crater (Rose et al., 1984). Currently, intense hydrothermal activity, consisting of fumaroles (mainly at the boiling point), steaming grounds, a soap–pool and an acidic (pH≈2.3) and warm lake (~30 °C) occur in the summit crater (Fig. 1B; Taran et al., 1998). With the low pH of the lake, CO2 is mainly present as a gaseous phase and dissolved in water. So, at this range of pH, the other carbonate species HCO3– and CO32– are not present in the water for which we were sure to measure the whole CO2 emitted from the lake.

El Chichón lies within an area of folded Jurassic evaporates, Cretaceous limestones, and Tertiary terrigenous rocks (Canul and Rocha, 1981; Duffield et al., 1984). The region is affected by two faults systems oriented approximately N–S and E–W. The most significant fault of the latter system is the San Juan Fault (Fig. 2). Furthermore, the area is characterized by a series of N45° E faults (Chapultenango Fault System) on top of which El Chichón has been emplaced (García–Palomo et al., 2004).


Procedure and method

In March 2007, a total of 162 randomly distributed CO2 flux measurements, covering an area of 138,000 m2 of the lake surface, were carried out (Fig. 1B). The GPS position of each measurement point represents the average of two readings (resolution ± 6 m) taken before and after each CO2 flux measurement (duration 40–60 sec). The drift between these two readings depended greatly on the wind and could attain 40 m. The accumulation chamber method (Chiodini et al., 1998) was modified in order to work on a lake by using a floating chamber (Fig. 3). Gas flux was measured by using a chamber equipped with a LICOR LI–8100–103 infrared CO2 analyzer (IRGA). The measurement accuracy of the CO2 flux measurements method is assumed to be ~12.5% (Evans et al., 2001). As the original method from Chiodini et al. (1998), the CO2 gas coming from the water lake passes through the chamber and the infra–red sensor, it returns to the chamber where it accumulates with the new CO2 entering the chamber. The flux is derived by obtaining the increase of the CO2 concentration with time (ppmvol.s–1). Each measurement takes about 40 to 60 seconds. In order to convert volumetric concentrations to mass concentrations (g.m–2.d–1), atmospheric pressure, temperature and total volume (sum of the chamber, IRGA connection tube, and the floating device) were taken in account. The fieldwork was undertaken under dry and stable meteorological conditions.

Computation of total CO2 flux was based on the graphical statistical approach (GSA) procedure (Chiodini et al., 1998, 2001; Cardellini et al., 2003). This procedure also permits to differentiate the degassing mechanisms of CO2. GSA consists in the partition of CO2 flux data into different lognormal populations (using the so–called "inflection" points) and in the estimation of the proportion, the mean and the standard deviation of each population following the graphical procedure of Sinclair (1974). The CO2 output associated to each population is obtained by multiplying the area of the lake by the proportion and the mean CO2 flux. The total CO2 release from the entire studied area can be obtained by summing the contribution of each population. The 90% confidence interval of the mean is used to calculate the uncertainty of the total CO2 output estimation of each population.

The mapping of degassing areas and estimation of the total CO2 discharge from the lake and the uncertainty of this estimation, were performed by using the sequential Gaussian simulation (sGs) that is an interpolation algorithm (Deutsch and Journel, 1998). The basic idea of the sGs is to generate a set of equiprobable representations of the spatial distribution of the simulated values, reproducing the statistical (histogram) and spatial (variogram) characteristics of the original data. According to Goovaerts (2001), the differences among all simulated maps (from 100 to 500 realizations) are used to compute the uncertainty of the flux estimation. The sGs approach has already successfully been used for soil CO2 degassing at other volcanic systems e.g. Chiodini et al., 2007 and details about the method in Cardellini et al., 2003.


Results and discussion

Probability distribution of the CO2flux data

Fig. 4a shows the histogram of log FCO2 (where FCO2 is CO2 flux in g.m–2.d–1) versus its frequency. The distribution of CO2 flux differs from a log–normal distribution indicating that there are at least two different mechanisms of degassing through the lake surface. According to the GSA approach (Sinclair, 1974), the histogram must be transferred to a log probability plot (Fig. 4b). This plot indicates that the CO2 flux data are separated into two different populations recognizable by the inflection point on the curve corresponding to the 83 cumulative percentile. On the plot we can individuate a high CO2 population (A in fig. 4b) corresponding to the 17 % of the data and a low CO2 population (B in fig. 4b) corresponding to the 83 % of FCO2. The two–population percentages must be checked and validated by combining both populations in the proportion of 17% A and 83 % B at various levels of log FCO2. The checking procedure uses the following relationship: PM = fAPA + fBPB, where PM is the probability of the "mixture", PA and PB are cumulative probabilities of population A and B from the plot of Fig. 4b at a specified x value; fA and fB are the proportions of populations A and B. In fig. 4b, the points of the "mixture" are represented by gray triangles. Afterwards, parameters of the individual partitioned populations can be estimated. To estimate the arithmetic mean value of CO2 flux and the central 90% confidence interval of the mean in the original data units (in g.m–2.d–1) for each population, we used, according to Chiodini et al. (1998), the Sichel's t estimator (David, 1977).

A summary of the estimated parameters of partitioned distributions (populations A and B) is reported in Table 1. Population Ais characterized by a mean of 6,702 g.m–2.d–1 with a 90% confidence interval of 5,154–10,429 g.m–2.d–1. Population B is characterized by a mean of 464 g.m–2.d–1 with a 90% confidence interval of 442–490 g.m–2.d–1. We suggest that population A corresponds to the flux resulting from bubbles rising through the lake and population B represents the CO2 degassing by diffusion through the water–air interface (see paragraph 4.3 for details).

The total flow rate of CO2 released by the lake, calculated by the GSA method, is (6,702 g.m–2.d–1 x 0.17% + 464 g.m–2.d–1 x 0.83%) x 138,000 m2 = 210 t.d–1with a 90% confidence interval of 172–301 t.d–1.

Mapping and sgs estimation of the CO2 flux from the lake

Another statistical method for the estimation of the CO2 fluxes and the total flow rate is the sequential Gaussian simulation (sGs) (Deutsch and Journel, 1998) method. The 162 measured CO2 fluxes in randomly distributed points on the lake surface were interpolated by a distribution over a grid of 5,523 square cells (5x5 m2) covering an area of 138,075 m2 using the so–called exponential variogram model. Then, 100 simulations of the CO2 fluxes with the obtained distribution were performed. For each simulation, the CO2 flux estimated at each cell is multiplied by 25 m2 and added to the other CO2 fluxes estimated at the neighborhood cells of the grid to obtain a total lake CO2 output. The mean of the 100 total simulated CO2 outputs, 164 t.d–1, represents the estimation of the total CO2 output from the lake area with a standard deviation of 9.5 t.d–1. The total CO2 output determined using GSA method is higher (210 t.d–1) than the mean simulated by the sGs method (164 t.d–1). In the calculation of the mean of FCO2, GSA approach does not take into account the spatial correlation between the data, resulting generally in an overestimation of the uncertainty.

The obtained map (Fig. 5) shows that the highest CO2 flux "spots" are located close to the eastern shore of the lake near the active fumarolic area. Two linear zones of high flux can be clearly recognized on the map, together with several intensively bubbling "funnels" observed during the campaign. These arrangements along NNW–SSE and W–E alignments may be correlated to the regional faults and the E–W San Juan Fault, respectively (García–Palomo et al., 2004).

Estimation of the CO2 diffusion through the lake–air interface

Our suggestion that the population of data with lower CO2 fluxes is provided by the diffusion of CO2 through water–air interface can be checked using the thin boundary layer model (Liss and Slater, 1974). The flux F between water and air may be calculated by the empirical equation (e.g. McGillis and Wanninkhof, 2006):

where kCO2 is the gas exchange coefficient (in cm.h–1) for CO2, Cw and Cw/a , refers to the concentration of CO2 in water, and in water film at the water–air interface, respectively.

The value of kCO2 was calculated by using the relationship between windspeed and kCO2 derived from tracer techniques studies on a small lake (Crusius and Wanninkhof, 2003):

where u1 is the windspeed measured at 1 m height and Sc is defined as the kinematic viscosity of water at measured temperature divided by the diffusivity of the gas at that temperature. Transfer velocity was adjusted to a Schmidt number of 600 that corresponds to the value for the dissolved atmospheric CO2 in fresh water at 20°C. The value of ScCO2 at 30°C was calculated according to Wanninkhof (1992):

At a mean windspeed u1 of 2 m.s–1, ScCO2 = 360 and k =1.39.

At saturation conditions of 30 °C and 1 atmosphere, Cw of the CO2 gas is 1.32–3 (Eq. 1). The concentration of CO2 in the air–water (Cw/a) interface can be approximated to the concentration of CO2 in the air–saturated water and corresponds to C≈w/a10–5–3 and Cw>>Cw/a. From the equation (1) and with values for kCO2 of 1.39 and Cw of 1.32–3 we estimated a CO2 flux by diffusion of 442 g.m–2.d–1 that is very close to the mean value of FCO2 (464 gm–2d–1) for the low flux of data points (population B).

Estimation of the heat power and comparison with other volcanoes in the world

The area of the whole crater floor corresponding to the isohypse 900 m (Fig. 1b) was estimated to be as 308,000 m2. Hypothesizing that mains NNW–SSE and W–E alignments are recognized on the lake and that there are not so important variations in FCO2 in soil and water due to the low depth of the lake (average depth 3 meters see Taran and Rouwet, 2008), a rough estimate of the total CO2 output for the whole crater floor yields ~370 t.d–1.

The high CO2 fluxes plotted on figure 6, show that high CO2 degassing is not necessarily related to active volcanoes. Three different sources of CO2 degassing are likely: (1) CO2, directly coming from a magma chamber, escapes to the surface with other magmatic gases such as SO2, H2S, HCl and HF, as this is the case for volcanoes Masaya, Nicaragua (Pérez et al., 2000), Miyakejima and Usu, Japan (Hernández et al., 2001a,b), Stromboli, Italy (Carapezza and Federico, 2000), San Salvador, El Salvador (Pérez et al., 2004), Santa Ana, El Salvador (Bernard et al., 2004) and Galeras, Colombia (Williams–Jones et al., 2000). (2) CO2 coming from a magma chamber but with a possible contamination due to the crustal carbonate decomposition and subsequent CO2 release. This type of the CO2 release could be the case for Solfatara and Vesuvio, Italy (Cardellini et al., 2003; Frondini et al., 2004), Santorini and Nisyros, Greece (Chiodini et al., 1998; Cardellini et al., 2003), Yellowstone, USA (Werner et al., 2000) and Kelud, Indonesia (Mazot, 2005). (3) CO2 degassing at low temperature and coming from carbonate metamorphism, not related to magmatism. Sites that released this kind of CO2 are for example Dixie Valley, USA (Bergfeld et al., 2001) and central Italy (Rogie et al., 2000).

The total CO2 output from El Chichon crater is 1.5 times higher than the effusion rates reported for the summit area at Stromboli (mean flux: 246 t.d–1; area: 357,500 m2; Carapezza and Federico, 2000) and little lower than those reported for the soil CO2 flux at Mammoth Mountain in Long Valley Caldera, USA (mean flux: 411 t.d1; area: 420,000 m2; Sorey et al., 1998).

The CO2 degassing from the volcanic lake of El Chichón was compared (Fig. 6) with that of Kelud crater lake (Indonesia) and Santa Ana crater lake (El Salvador). In the Kelud crater lake, where CO2 flux measurements has been carried out since 2001 (Mazot, 2005), the total CO2 output ranges from 100 t.d–1 with a mean of 1020 g.m–2.d–1 (2001) to 35 t.d–1 with a mean of 335 g.m–2.d–1 (2006) and a constant area of 103,600 m2. In Santa Ana, where measurement was performed in 2002, CO2 output corresponds to 7 t.d–1 in 2002 with a mean of CO2 flux of 220 g.m–2.d–1 and an area of 30,000 m2 (Bernard et al, 2004). Among these three volcanic lakes, the total CO2 output at El Chichón in 2007 was up to 5 times higher (164 t.d–1) than Kelud volcano and 23 times higher than Santa Ana (Fig.4).

Fumarolic gas of El Chichón volcano contains about 90 wt% of H2O (steam) and 10 wt% of CO2 (Taran et al., 1998; Tassi et al., 2003). Assuming that all the CO2 released from the crater floor is the result of separation of these gases caused by shallow condensation of hydrothermal steam at ~ 100 °C, beneath the crater floor of the volcano we have ~ 3,700 t/day or ~ 43 kg/s of steam flux and beneath the lake we have ~ 1,640 t/day or ~ 19 kg/s. Using a value for steam enthalpy at 100 °C due to steam condensation (~ 2.257 MJ/kg) we can estimate the heat power due to fumarolic output from the crater floor as 100 and from the lake 43 MW. This heat output is up to 3.5 times higher than the output estimated by Taran and Rouwet (2008) using the heat and chemical balance approach at El Chichón lake. Our estimation based on the direct measurements of fluxes seems to be more realistic.

The heat output corresponding to El Chichón lake (43 MW) is comparable with the heat power of other crater lakes of active volcanoes. In Kelud lake, Mazot (2005) calculated values of heat power ranging from 45 to 180 MW in the period 2004–2007 (Table 2) by using the heat and chemical balance model of Stevenson (1992). The heat power was estimated on other crater lakes as Kawah Ijen (Indonesia; Delmelle, 1995), Taal (Philippines; Poussielgue, 1998), Poas (Costa Rica; Stevenson, 1992), Yugama (Japan; Ohba et al., 1994), Ruapehu (New Zealand; Stevenson, 1992) and Copahue (Argentina; Varekamp et al., 2001). The heat output of 100 MW from El Chichón crater is relatively small in comparison with the heat power observed at hot (>40 °C) crater lakes, where values as high as several hundred MW were estimated (Table 2).



CO2 flux measurements made by using the floating accumulation chamber method allowed to estimate the total CO2 emission from the crater lake of El Chichón (138,000 m2) to be close to 164 t.d–1. For the total area of the crater floor of 308,000 m2 the total CO2 emission was estimated at 370 t.d–1. This level of the total CO2 emission and the estimated heat output are comparable with other volcanic and geothermal areas worldwide.

Continuous monitoring of CO2 flux from the crater lake of El Chichón could improve our understanding of the hydrothermal system. This would be complementary to other geochemical investigations and it would be particularly important for detecting possible changes in the activity of the volcano.



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