# Heat and Helium-3 Fluxes from Teide Volcano, Canary Islands, Spain

Authors: Mar Alonso; Eleazar Padrón; Hirochika Sumino; Pedro A. Hernández; Gladys V. Melián; María Asensio-Ramos; Fátima Rodríguez; Germán Padilla; Marta García-Merino; Cecilia Amonte; Nemesio M. Pérez
Journal: Geofluids
 (2019)

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## Abstract

During July 2016, the first integrated heat flow, CO2, and 3He emission survey was conducted across 0.5 km2 of the summit cone and crater of Teide volcano, Tenerife, Canary Islands, Spain. The thermal energy released from Teide summit cone by diffuse degassing was 2.2 MW, and the heat flux calculated through Dawson’s method was 8.1 MW, difference due to the comparison of purely convective areas as the crater with diffusive areas as the flanks of the volcano. Diffuse CO2 output was 211±20 t d-1, and 3He emission was estimated to be within a range between 0.35 and 0.89 mol y-1. The obtained values of diffuse degassing and heat fluxes are close to others obtained for similar volcanic areas. The calculation of 3He/heat ratio for the first time in this volcanic system supports the presence of an important mantle source for the degassing of Teide volcano.


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## Body

## 1. Introduction

The Earth’s mantle is an important reservoir for compounds pertinent to surface and atmospheric processes such as water, carbon dioxide, sulphur, and noble gases. Advection of heat to the atmosphere via transportation of these gases remains an understudied phenomenon despite its potential importance [1, 2]. Volcanic activity represents focussed conduits for these fluxes and, as such, represents a key connection between the mantle and the atmosphere. Accurate measurements of both heat and gas flux from active volcanoes, and appraisal of their various sources, has contributed to a better understanding of the mantle-atmosphere link. In this study, we present the first data about the relationship between 3He and heat flux in the Teide volcanic system. This work is a new contribution to 3He global emission estimates.Volcanoes emit large amounts of gases and volatiles to the atmosphere. These take the form of visible emanations through volcanic plumes, fumaroles, and solfataras and through diffuse degassing (nonvisible emanations). Both types of gas emissions are controlled by local volcano-tectonic structures as a result of transport via diffusion and advection [3].Among volcanic gases, helium has been considered as a useful tool in the geochemists’ toolbox [4]. Helium is chemically inert, physically stable, nonbiogenic, sparingly soluble in water under ambient conditions, almost nonadsorbable, and, consequently, highly mobile. Due to these properties and its deep origin, helium is considered a tracer of magmatic activity and its speed of traversing the crust makes it an excellent precursor of volcanic eruptions [5–7].There are two naturally occurring isotopes of helium:4He and 3He, with an atmospheric 3He/4He ratio (RA) of 1.384·10-6 [8]. 4He is produced mainly in the crust as α-particles from the radioactive decay of 238U, 235U, and 232Th, while nearly all of the 3He is primordial in origin and, by far, its most important source is the Earth’s interior. The 3He/4He ratio varies from high values (>10-5) in mantle-derived lavas and fluids to low values (~10-8) in continental regions [9]. Helium production and the degree of tortuosity are the main parameters that control the uprising mantle-derived helium from the source to the atmosphere, showing a decreasing trend of the 3He/4He ratio with the distance in and around stratovolcanoes [6, 10]. However, in the case of Tenerife Island, Pérez et al. [11] demonstrated that the 3He/4He ratio remained constant regardless of the distance to Teide volcano.In the case of the Canary Islands, the geographical distribution of the3He/4He ratios shows the highest values on the westernmost islands (La Palma and El Hierro), which implies the existence of a helium source derived from the deep mantle [12–14]. Mass transfer of mantle helium to a fluid is accompanied by transfer of heat [15]. The presence of magmatic helium in a hydrothermal fluid therefore implies direct transport of heat from that magma to the fluid [15]. Previous studies have demonstrated a positive relation between helium isotopic composition and heat flux [16–18].The calculated3He/heat production ratio in the upper mantle of the Earth is ∼0.5×10−12cm3 STP/J [19] (where STP is P=1atm and T=25°C) and is spatially heterogeneous. For instance, the 3He/heat production ratio associated with hot-spot volcanism is typically ∼24×10−12cm3 STP/J [19, 20]. These values are much higher than that estimated for crustal regimes, ∼1×10−15cm3 STP/J, which are also dominated by radiogenic 4He production [20]. Therefore, 3He emission and heat flux studies at volcano-geothermal systems improve understanding not only of those systems but also the connection between mantle and atmosphere.The measurement of the total thermal energy flux through the surface in volcanic areas is used to determinate changes in the magmatic activity and detecting changes in the energy balance of the volcanic system as a result of magmatic and tectonic processes [3, 21, 22].The main objectives of this work are to compare3He emission estimated through different approaches, describe those estimates’ relationship with heat flux, and calculate an indicative 3He/heat production ratio at Teide volcano. It is important to highlight that it is the first study about the relationship between 3He and heat flux in the Teide volcanic system. As such, this work is a new contributing value to 3He global emission estimates.


## 2. Geological Setting

The Canarian archipelago is located in the Atlantic ocean about 100 km west of the African coast between 27°37′ and 29°25′N and between 13°20′ and 18°10′W (offshore Morocco). It consists of 7 main islands, decreasing ages from east to west, with the western islands still in the shield stage and the eastern-most in the erosional phase [23]. Their genesis continues to attract debate discussed below.The most widely accepted “working” model is the one that combines three different hypotheses: hot spot, propagating fracture, and uplifted block hypothesis. It means that the islands originate from a thermal anomaly in the mantle helped by regional fractures for the beginning of magmatism; meanwhile, the islands are in their present freeboard attitude due to the action of tectonic forces [24].Tenerife (2,034 km2) (Figure 1), the central and largest island of the archipelago, is currently at the zenith of its volcanic development [23, 25]. The structure of Tenerife is controlled by a volcano-tectonic rift system with NW, NE, and NS directions. The oldest visible geological unit on Tenerife is called the “old basaltic series,” from central Miocene, and its forms by three strongly eroded edifices distributed in the corners of the island: Anaga (north-east), Teno (north-west), and Roque del Conde (south). This unit is formed by basaltic lavas and pyroclastics with some trachytes and phonolites [26]. A period of 2-3 M.y. of volcanic quiescence and erosion took place between “old basaltic series” and the eruptions which formed the younger volcanic series. Las Cañadas volcano grew on the eroded remains of the “old basaltic series” reaching about 40 km in diameter and 2,700-3,000 m of a complex succession of basalts, trachybasalts, trachytes, and phonolites that then collapsed 200 ky ago to form Las Cañadas caldera depression [23]. The caldera is located in the intersection of the three rifts, and the vertical collapse was associated with emptying of shallow magma chambers [27–29]. Other authors suggest the combination of vertical and lateral collapse for the formation of Las Cañadas caldera [30]. The youngest activity of the island is represented by basalts, trachytes, and phonolites of Teide-Pico Viejo volcanic complex and some individual basaltic cones scattered around the island, mainly located on the structural rift systems (NW, NE, and NS directions), characterized by the alignment of cinder cones and fissure systems, where historical eruptions occurred. Those monogenetic cones represent the most common eruptive activity during the last 1 M.y., and it is possible to easily recognize 297 of these cones in the island [31].Figure 1
Tenerife Island marked with the location of the volcanic system studied, locations of historical eruptions and the three rifts. Inset: map of the Canarian archipelago highlighting Tenerife Island in grey.The 17 km long and 10 km wide caldera is the salient geomorphological feature of Tenerife partly because it hosts the highest stratovolcano in the Atlantic Ocean: Teide volcano (3,718 m.a.s.l.), a portion of Teide-Pico Viejo volcanic complex. Teide and Pico Viejo volcanoes overlap to form an elongate double cone. This volcanic complex was formed through different eruptive styles, ranging from strombolian to phreatomagmatic eruptions to cryptodome formation and dome extrusions [28, 32] forming basaltic, trachytic, and phonolitic products. The last eruption in this complex, Chahorra, occurred in 1798 through an adventive cone of Pico Viejo volcano.Teide summit cone has been constructed during several phases. Its eruptive products are mainly phonolitic and basaltic-trachybasaltic lavas [32]. Persistent degassing activity has taken place at the summit of the volcano since the last eruption [33, 34].Visible degassing in the summit cone of Teide volcano consists in low temperature fumaroles (around 83°C). Water is the major component of these fumaroles, followed by CO2, N2, H2, H2S, Ar, CH4, and CO, a composition typical of hydrothermal fluids [34, 35]. Diffuse degassing is the principle degassing mechanism of Teide volcano, with the highest rates emanated from the summit cone and crater of Teide volcano [36, 37].


## 3. Sampling Procedures, Analytical Methods, and Data Reduction

During July 2016, a soil gas survey comprised of 170 measurement sites was conducted at the summit cone of Teide volcano covering an area of 0.5 km2 (Figure 2). The field work was carried out in the summer in order to minimize meteorological influences. The average distance between points of the summit cone was 45 meters on the slopes and 10 meters inside the crater, designed to tightly constrain the areal extent of visible degassing anomalies and arrive at more accurate overall estimates, while also achieving an evenly spaced distribution per domain.Figure 2
Geological map of Teide volcano summit cone and crater marked with the 170 measurement sites performed in the survey.


### 3.1. Soil CO2 Efflux and Temperature Measurements

Measurements of diffuse CO2 were conducted at the soil surface using the accumulation chamber method [38] by means of West Systems portable CO2 efflux meters equipped with a nondispersive infrared CO2 analyzer LICOR-820. This system is composed of a double beam infrared carbon dioxide sensor compensated for temperature and atmospheric pressure and an optical bench of 20,000 ppm of resolution. The gas flux meter was interfaced to a handheld computer running data acquisition software.Soil temperature was determined by inserting a Type K thermocouple at each sampling site at 15 and 40 cm depth.


### 3.2. Soil Gas Sampling

At each measurement site, soil gas was collected in 20 cc glass vials. This was achieved by inserting a 50 cm stainless probe 40 cm depth into the ground connected to a hypodermic syringe. Residual gas inside the probe was purged before sampling.Gaseous species as Ne, H2, O2, N2, CH4, CO2, and H2O were analyzed by microchromatrography with a VARIAN model 4900 (Agilent Technologies, USA), using a thermal conductivity detector and a 20 m PoraPLOT Q column using argon (Ar) as carrier gas. The temperature of the column and injector was 40°C and 80°C, respectively, and the injection time was 20 ms. The detection limit for CO2 was estimated to be about 10 ppmV, and the accuracy of the measurements was about 2.5% on the basis of standard sample measurements.Helium was analyzed by a quadrupole mass spectrometer Pfeiffer Omnistar 422. The instrument accuracy of helium concentration was estimated to be±300ppb, and the detection limit for helium is 1 ppm. Atmospheric gas was used periodically to calibrate the instrument.The isotopic ratio expressed asδ13C-CO2‰ vs. VPDB was measured by means of a Thermo Finnigan MAT 253 mass spectrometer. The analytical error for δ13C values is of ±0.1‰.


### 3.3. Fumarole Sampling

Fumarolic gas samples were also collected in July 2016. Teide fumarolic activity consists of fluids discharged at approximately 83.5°C, close to the boiling point of water at 3,718 m.a.s.l. (87.5°C). A vent located inside the rim of the summit crater in the NE sector was the focus of the sampling effort.A glass funnel was inserted into the vent and buried to prevent atmospheric air entering into the sampling system. The funnel was connected to a preevacuated glass flask filled with 50 ml of an alkaline solution (4 N KOH). H2O vapour condenses and acidic gases as CO2, SO2, and HCl dissolve into the alkaline solution, while noncondensable gases (N2, O2, He, H2, CH4, etc.) are concentrated in the gas phase of the sampling flask [35]. CO2 concentration and CO2/H2O molar ratio were analyzed by titration following the method described by Giggenbach and Goguel [39].For the analysis of helium isotopes, lead-glass containers were filled with the fumarolic gas discharge. Helium concentration and3He/4He isotopic ratios are expressed as RA=R/Rair, where R is the measured 3He/4He ratio and Rair is that of the air; 1.384×10−6 [8] were analyzed using a high-precision noble gas mass spectrometer (modified-VG5400), following the procedure of Sumino et al. [40]. The correction factor for the helium isotope ratio was determined by measurements of interlaboratory helium standard named HESJ, with an established 3He/4He value of 20.63±0.10RA [41]. The analytical error for RA was <2%. The measured 3He/4He ratios were corrected for air contamination based on the 4He/20Ne ratios measured with the mass spectrometer, assuming that all the neon has an atmospheric origin [16, 42].


### 3.4. Data Reduction and Spatial Interpolation

#### 3.4.1.4He Flux Determination

The circulation of gases at superficial levels of volcanoes is governed by a combination of diffusive and advective mechanisms. Flows and velocities of gas moving by advective mechanisms, however, are much higher than those produced by diffusion. Diffusive and advective emission values were estimated at each sampling site as follows.Diffusion is described by Fick’s law:(1)Fi=−DmdCdz,where Dm is the molecular diffusion coefficient (m2 s-1) and dC is the variation of gas concentration (kg m-3) along dz (m).The apparent diffusion coefficient (D) includes the effect of porosity (n) and tortuosity (τ) of the environment. For soils, Etiope and Martinelli [43] define this coefficient as
(2)D=Dmn2=Dmnτ.Advection is described by Darcy’s law:(3)Fi=−Cik∇PμZ,where Ci is the soil gas concentration (kg m-3), k the permeability (m2), μ the dynamic viscosity of the gas (kg m-1 s-1), and ∇P the pressure difference (kg m-1 s-2) between two points spaced at distance Z (m) [43].Soil intrinsic permeability (k) is a key factor to estimate the theoretical emission of gases via Darcy’s law. It depends on the hydraulic permeability (Ks) following Schaap and Lebron [44]:
(4)k=μρgKs,where μ is the gas viscosity (kg m-1 s-1), ρ the gas density (kg m-3), and g the gravitational constant (m s-2).In case of Teide volcano, pressure gradients are mostly generated by the geothermal gradient, which manifests by convection. We assume in this study, therefore, that the advective component of gas flux from the deep interior to the atmosphere is mainly governed by the efficiency of convection at the soil scale. Under this assumption, the pressure gradient is obtained from:(5)∇P=Pamb−Psoil=Pamb1−TsoilTamb,where Psoil and Pamb are soil and ambient pressure and Tsoil and Tamb are soil and ambient temperatures, respectively.By combining equations (3), (4), and (5), we obtain the following expression for the convective flux:
(6)Fi=−CiKsPambρgZ1−TsoilTamb.Direct measurements of diffuse CO2 emission FCO2, soil CO2 concentration CCO2, air temperature (Tamb), and soil temperature at 40 cm depth (Tsoil) were used to estimate the hydraulic permeability Ks from equation (6) at each sampling site. These values were used later to estimate the convective flux of 4He. To calculate the diffusive emission component for 4He, we used a 7×10−5 as diffusion coefficient [43] and a value of 0.35 for porosity, as have been used in similar volcanic areas [45].


#### 3.4.2.3He Flux Determinations

3He generally has low abundance, which leads to high analytical uncertainty for most gas samples. To arrive at an accurate estimate of flux across the study area, we must interpolate from 3He measurements with high certainty using robust relationships with other gas fluxes. The 3He output released to the atmosphere from the summit cone of Teide volcano can be estimated to be within the limits calculated by two end-member assumptions:
(1)
The3He/4He ratio in the fumarolic gases (9.34×10−6) is the same across the whole hydrothermal system, which is to assume the source of all helium is the same. In this case, 3He emission (mol d-1) is simply calculated using the 3He/4He ratio and the 4He emission (mol d-1) using the relationship:
(7)Φ3He=3He/H4e×Φ4He
(2)
The3He flux is wholly derived from deep-seated source and therefore can be tied to the nonbiogenic component of the CO2 flux. The estimated diffuse CO2 emission, the CO2/4He molar ratio, and the 3He/4He isotopic ratio measured in the fumarolic discharges of Teide can be used to estimate 3He output using the relationships:
(8)CO2/H4e/3He/H4e=CO2/H3e;Φ3He=ΦCO2/CO2/H3e


#### 3.4.3. Heat Flow

CO2 was used as a tracer of hydrothermal fluids to calculate the heat flow involved in the diffuse degassing process. Chiodini et al. [46] first demonstrated this method that rests on the assumption that the H2O/CO2 ratio is recorded, before steam condensation, by fumarolic effluents. These authors computed the heat flux adding the following contributions: (1) the heat released by H2O gas moving from the hydrothermal reservoir to the steam condensation zone, (2) the heat given off by CO2 passing from the hydrothermal reservoir to atmospheric conditions, (3) the enthalpy of steam condensation at 100°C, and (4) the heat loss by liquid water on cooling from 100°C to the average seasonal value.In the July 2016 survey, the measured H2O/CO2 ratio was 2.24. On the basis of this ratio, we computed that 473 t d-1 of steam are condensed to produce the hydrothermal CO2 output of 211 t d-1 following the procedure described by Frondini et al. [47]. The released thermal energy associated with the condensation of 473 t d-1 of steam was estimated on 1.26×1012J d-1.This value was obtained following two contributions. The enthalpy of steam condensation at 100°C (1.07×1012J d-1) is given by the product of the total amount of steam condensed in one day (4.73×108g) times the enthalpy of evaporation at 100°C (2,257 J g-1) [48]. The heat loss by liquid water on cooling from 100°C to the average seasonal value of 3.2°C (1.89×1011J d-1) is given by the product of the enthalpy lost by 1 g of water (ΔH=398.7J g-1) times the mass of water (4.73×108g).The heat flux was also calculated following the method described by Dawson [49]. The method is based on correlation between soil temperature at 15 cm depth (t15) and surface heat flux (q) by the following equation:
(9)q=5.2×10−6t154,where t15 was measured by a portable calorimeter at each point.Sequential Gaussian simulation (sGs) using the sGsim program [50] was used to construct spatial distribution maps of CO2, 4He, and heat fluxes. The sGs procedure allowed us to interpolate the different parameters at a nonsampled area between the sampling points and obtain the uncertainty of emissions. Emission of the entire area of study was estimated using these maps.


## 3.1. Soil CO2 Efflux and Temperature Measurements

Measurements of diffuse CO2 were conducted at the soil surface using the accumulation chamber method [38] by means of West Systems portable CO2 efflux meters equipped with a nondispersive infrared CO2 analyzer LICOR-820. This system is composed of a double beam infrared carbon dioxide sensor compensated for temperature and atmospheric pressure and an optical bench of 20,000 ppm of resolution. The gas flux meter was interfaced to a handheld computer running data acquisition software.Soil temperature was determined by inserting a Type K thermocouple at each sampling site at 15 and 40 cm depth.


## 3.2. Soil Gas Sampling

At each measurement site, soil gas was collected in 20 cc glass vials. This was achieved by inserting a 50 cm stainless probe 40 cm depth into the ground connected to a hypodermic syringe. Residual gas inside the probe was purged before sampling.Gaseous species as Ne, H2, O2, N2, CH4, CO2, and H2O were analyzed by microchromatrography with a VARIAN model 4900 (Agilent Technologies, USA), using a thermal conductivity detector and a 20 m PoraPLOT Q column using argon (Ar) as carrier gas. The temperature of the column and injector was 40°C and 80°C, respectively, and the injection time was 20 ms. The detection limit for CO2 was estimated to be about 10 ppmV, and the accuracy of the measurements was about 2.5% on the basis of standard sample measurements.Helium was analyzed by a quadrupole mass spectrometer Pfeiffer Omnistar 422. The instrument accuracy of helium concentration was estimated to be±300ppb, and the detection limit for helium is 1 ppm. Atmospheric gas was used periodically to calibrate the instrument.The isotopic ratio expressed asδ13C-CO2‰ vs. VPDB was measured by means of a Thermo Finnigan MAT 253 mass spectrometer. The analytical error for δ13C values is of ±0.1‰.


## 3.3. Fumarole Sampling

Fumarolic gas samples were also collected in July 2016. Teide fumarolic activity consists of fluids discharged at approximately 83.5°C, close to the boiling point of water at 3,718 m.a.s.l. (87.5°C). A vent located inside the rim of the summit crater in the NE sector was the focus of the sampling effort.A glass funnel was inserted into the vent and buried to prevent atmospheric air entering into the sampling system. The funnel was connected to a preevacuated glass flask filled with 50 ml of an alkaline solution (4 N KOH). H2O vapour condenses and acidic gases as CO2, SO2, and HCl dissolve into the alkaline solution, while noncondensable gases (N2, O2, He, H2, CH4, etc.) are concentrated in the gas phase of the sampling flask [35]. CO2 concentration and CO2/H2O molar ratio were analyzed by titration following the method described by Giggenbach and Goguel [39].For the analysis of helium isotopes, lead-glass containers were filled with the fumarolic gas discharge. Helium concentration and3He/4He isotopic ratios are expressed as RA=R/Rair, where R is the measured 3He/4He ratio and Rair is that of the air; 1.384×10−6 [8] were analyzed using a high-precision noble gas mass spectrometer (modified-VG5400), following the procedure of Sumino et al. [40]. The correction factor for the helium isotope ratio was determined by measurements of interlaboratory helium standard named HESJ, with an established 3He/4He value of 20.63±0.10RA [41]. The analytical error for RA was <2%. The measured 3He/4He ratios were corrected for air contamination based on the 4He/20Ne ratios measured with the mass spectrometer, assuming that all the neon has an atmospheric origin [16, 42].


## 3.4. Data Reduction and Spatial Interpolation

### 3.4.1.4He Flux Determination

The circulation of gases at superficial levels of volcanoes is governed by a combination of diffusive and advective mechanisms. Flows and velocities of gas moving by advective mechanisms, however, are much higher than those produced by diffusion. Diffusive and advective emission values were estimated at each sampling site as follows.Diffusion is described by Fick’s law:(1)Fi=−DmdCdz,where Dm is the molecular diffusion coefficient (m2 s-1) and dC is the variation of gas concentration (kg m-3) along dz (m).The apparent diffusion coefficient (D) includes the effect of porosity (n) and tortuosity (τ) of the environment. For soils, Etiope and Martinelli [43] define this coefficient as
(2)D=Dmn2=Dmnτ.Advection is described by Darcy’s law:(3)Fi=−Cik∇PμZ,where Ci is the soil gas concentration (kg m-3), k the permeability (m2), μ the dynamic viscosity of the gas (kg m-1 s-1), and ∇P the pressure difference (kg m-1 s-2) between two points spaced at distance Z (m) [43].Soil intrinsic permeability (k) is a key factor to estimate the theoretical emission of gases via Darcy’s law. It depends on the hydraulic permeability (Ks) following Schaap and Lebron [44]:
(4)k=μρgKs,where μ is the gas viscosity (kg m-1 s-1), ρ the gas density (kg m-3), and g the gravitational constant (m s-2).In case of Teide volcano, pressure gradients are mostly generated by the geothermal gradient, which manifests by convection. We assume in this study, therefore, that the advective component of gas flux from the deep interior to the atmosphere is mainly governed by the efficiency of convection at the soil scale. Under this assumption, the pressure gradient is obtained from:(5)∇P=Pamb−Psoil=Pamb1−TsoilTamb,where Psoil and Pamb are soil and ambient pressure and Tsoil and Tamb are soil and ambient temperatures, respectively.By combining equations (3), (4), and (5), we obtain the following expression for the convective flux:
(6)Fi=−CiKsPambρgZ1−TsoilTamb.Direct measurements of diffuse CO2 emission FCO2, soil CO2 concentration CCO2, air temperature (Tamb), and soil temperature at 40 cm depth (Tsoil) were used to estimate the hydraulic permeability Ks from equation (6) at each sampling site. These values were used later to estimate the convective flux of 4He. To calculate the diffusive emission component for 4He, we used a 7×10−5 as diffusion coefficient [43] and a value of 0.35 for porosity, as have been used in similar volcanic areas [45].


### 3.4.2.3He Flux Determinations

3He generally has low abundance, which leads to high analytical uncertainty for most gas samples. To arrive at an accurate estimate of flux across the study area, we must interpolate from 3He measurements with high certainty using robust relationships with other gas fluxes. The 3He output released to the atmosphere from the summit cone of Teide volcano can be estimated to be within the limits calculated by two end-member assumptions:
(1)
The3He/4He ratio in the fumarolic gases (9.34×10−6) is the same across the whole hydrothermal system, which is to assume the source of all helium is the same. In this case, 3He emission (mol d-1) is simply calculated using the 3He/4He ratio and the 4He emission (mol d-1) using the relationship:
(7)Φ3He=3He/H4e×Φ4He
(2)
The3He flux is wholly derived from deep-seated source and therefore can be tied to the nonbiogenic component of the CO2 flux. The estimated diffuse CO2 emission, the CO2/4He molar ratio, and the 3He/4He isotopic ratio measured in the fumarolic discharges of Teide can be used to estimate 3He output using the relationships:
(8)CO2/H4e/3He/H4e=CO2/H3e;Φ3He=ΦCO2/CO2/H3e


### 3.4.3. Heat Flow

CO2 was used as a tracer of hydrothermal fluids to calculate the heat flow involved in the diffuse degassing process. Chiodini et al. [46] first demonstrated this method that rests on the assumption that the H2O/CO2 ratio is recorded, before steam condensation, by fumarolic effluents. These authors computed the heat flux adding the following contributions: (1) the heat released by H2O gas moving from the hydrothermal reservoir to the steam condensation zone, (2) the heat given off by CO2 passing from the hydrothermal reservoir to atmospheric conditions, (3) the enthalpy of steam condensation at 100°C, and (4) the heat loss by liquid water on cooling from 100°C to the average seasonal value.In the July 2016 survey, the measured H2O/CO2 ratio was 2.24. On the basis of this ratio, we computed that 473 t d-1 of steam are condensed to produce the hydrothermal CO2 output of 211 t d-1 following the procedure described by Frondini et al. [47]. The released thermal energy associated with the condensation of 473 t d-1 of steam was estimated on 1.26×1012J d-1.This value was obtained following two contributions. The enthalpy of steam condensation at 100°C (1.07×1012J d-1) is given by the product of the total amount of steam condensed in one day (4.73×108g) times the enthalpy of evaporation at 100°C (2,257 J g-1) [48]. The heat loss by liquid water on cooling from 100°C to the average seasonal value of 3.2°C (1.89×1011J d-1) is given by the product of the enthalpy lost by 1 g of water (ΔH=398.7J g-1) times the mass of water (4.73×108g).The heat flux was also calculated following the method described by Dawson [49]. The method is based on correlation between soil temperature at 15 cm depth (t15) and surface heat flux (q) by the following equation:
(9)q=5.2×10−6t154,where t15 was measured by a portable calorimeter at each point.Sequential Gaussian simulation (sGs) using the sGsim program [50] was used to construct spatial distribution maps of CO2, 4He, and heat fluxes. The sGs procedure allowed us to interpolate the different parameters at a nonsampled area between the sampling points and obtain the uncertainty of emissions. Emission of the entire area of study was estimated using these maps.


## 3.4.1.4He Flux Determination

The circulation of gases at superficial levels of volcanoes is governed by a combination of diffusive and advective mechanisms. Flows and velocities of gas moving by advective mechanisms, however, are much higher than those produced by diffusion. Diffusive and advective emission values were estimated at each sampling site as follows.Diffusion is described by Fick’s law:(1)Fi=−DmdCdz,where Dm is the molecular diffusion coefficient (m2 s-1) and dC is the variation of gas concentration (kg m-3) along dz (m).The apparent diffusion coefficient (D) includes the effect of porosity (n) and tortuosity (τ) of the environment. For soils, Etiope and Martinelli [43] define this coefficient as
(2)D=Dmn2=Dmnτ.Advection is described by Darcy’s law:(3)Fi=−Cik∇PμZ,where Ci is the soil gas concentration (kg m-3), k the permeability (m2), μ the dynamic viscosity of the gas (kg m-1 s-1), and ∇P the pressure difference (kg m-1 s-2) between two points spaced at distance Z (m) [43].Soil intrinsic permeability (k) is a key factor to estimate the theoretical emission of gases via Darcy’s law. It depends on the hydraulic permeability (Ks) following Schaap and Lebron [44]:
(4)k=μρgKs,where μ is the gas viscosity (kg m-1 s-1), ρ the gas density (kg m-3), and g the gravitational constant (m s-2).In case of Teide volcano, pressure gradients are mostly generated by the geothermal gradient, which manifests by convection. We assume in this study, therefore, that the advective component of gas flux from the deep interior to the atmosphere is mainly governed by the efficiency of convection at the soil scale. Under this assumption, the pressure gradient is obtained from:(5)∇P=Pamb−Psoil=Pamb1−TsoilTamb,where Psoil and Pamb are soil and ambient pressure and Tsoil and Tamb are soil and ambient temperatures, respectively.By combining equations (3), (4), and (5), we obtain the following expression for the convective flux:
(6)Fi=−CiKsPambρgZ1−TsoilTamb.Direct measurements of diffuse CO2 emission FCO2, soil CO2 concentration CCO2, air temperature (Tamb), and soil temperature at 40 cm depth (Tsoil) were used to estimate the hydraulic permeability Ks from equation (6) at each sampling site. These values were used later to estimate the convective flux of 4He. To calculate the diffusive emission component for 4He, we used a 7×10−5 as diffusion coefficient [43] and a value of 0.35 for porosity, as have been used in similar volcanic areas [45].


## 3.4.2.3He Flux Determinations

3He generally has low abundance, which leads to high analytical uncertainty for most gas samples. To arrive at an accurate estimate of flux across the study area, we must interpolate from 3He measurements with high certainty using robust relationships with other gas fluxes. The 3He output released to the atmosphere from the summit cone of Teide volcano can be estimated to be within the limits calculated by two end-member assumptions:
(1)
The3He/4He ratio in the fumarolic gases (9.34×10−6) is the same across the whole hydrothermal system, which is to assume the source of all helium is the same. In this case, 3He emission (mol d-1) is simply calculated using the 3He/4He ratio and the 4He emission (mol d-1) using the relationship:
(7)Φ3He=3He/H4e×Φ4He
(2)
The3He flux is wholly derived from deep-seated source and therefore can be tied to the nonbiogenic component of the CO2 flux. The estimated diffuse CO2 emission, the CO2/4He molar ratio, and the 3He/4He isotopic ratio measured in the fumarolic discharges of Teide can be used to estimate 3He output using the relationships:
(8)CO2/H4e/3He/H4e=CO2/H3e;Φ3He=ΦCO2/CO2/H3e


## 3.4.3. Heat Flow

CO2 was used as a tracer of hydrothermal fluids to calculate the heat flow involved in the diffuse degassing process. Chiodini et al. [46] first demonstrated this method that rests on the assumption that the H2O/CO2 ratio is recorded, before steam condensation, by fumarolic effluents. These authors computed the heat flux adding the following contributions: (1) the heat released by H2O gas moving from the hydrothermal reservoir to the steam condensation zone, (2) the heat given off by CO2 passing from the hydrothermal reservoir to atmospheric conditions, (3) the enthalpy of steam condensation at 100°C, and (4) the heat loss by liquid water on cooling from 100°C to the average seasonal value.In the July 2016 survey, the measured H2O/CO2 ratio was 2.24. On the basis of this ratio, we computed that 473 t d-1 of steam are condensed to produce the hydrothermal CO2 output of 211 t d-1 following the procedure described by Frondini et al. [47]. The released thermal energy associated with the condensation of 473 t d-1 of steam was estimated on 1.26×1012J d-1.This value was obtained following two contributions. The enthalpy of steam condensation at 100°C (1.07×1012J d-1) is given by the product of the total amount of steam condensed in one day (4.73×108g) times the enthalpy of evaporation at 100°C (2,257 J g-1) [48]. The heat loss by liquid water on cooling from 100°C to the average seasonal value of 3.2°C (1.89×1011J d-1) is given by the product of the enthalpy lost by 1 g of water (ΔH=398.7J g-1) times the mass of water (4.73×108g).The heat flux was also calculated following the method described by Dawson [49]. The method is based on correlation between soil temperature at 15 cm depth (t15) and surface heat flux (q) by the following equation:
(9)q=5.2×10−6t154,where t15 was measured by a portable calorimeter at each point.Sequential Gaussian simulation (sGs) using the sGsim program [50] was used to construct spatial distribution maps of CO2, 4He, and heat fluxes. The sGs procedure allowed us to interpolate the different parameters at a nonsampled area between the sampling points and obtain the uncertainty of emissions. Emission of the entire area of study was estimated using these maps.


## 4. Results and Discussion

### 4.1. CO2 Fluxes and Isotopic Signatures

Diffuse CO2 efflux values ranged from below detection to 10,650 g m-2d-1 with an average value of 879 g m-2d-1. The spatially interpolated total diffuse CO2 output released from the summit cone of Teide volcano was calculated as 211±20t d-1. Similar results were obtained by Pérez et al. [37]; an emission value of 180±21 was calculated for the 2009 survey for an area of 0.11 km2.The diffuse CO2 emission map (Figure 3) shows higher values located inside the crater, along the crater rim mainly close to the fumarolic area and towards the north and north-east flanks. The areas with higher CO2 efflux values also show relatively high temperatures and appear correlated to hydrothermal alteration at the surface, suggesting a mainly advective degasification mechanism governing the gas emission regime at the study area. The north and north-east anomalies are probably related to radial fissures propagated from the volcanic axis [37]. Lower values are observed at other sectors of the flanks of the cone.Figure 3
Diffuse CO2 emission map of the summit cone and crater of Teide volcano.The total diffuse CO2 output is comparable with the 219±36t d-1 released by Pico do Fogo volcano, Cape Verde, a similar volcanic system in a similar volcano-tectonic environment, measured during a survey in February 2010 [21].Figure4 summarizes the CO2 isotopic composition and indicates that most of the analyzed samples correspond to a deep-seated source of CO2, with different degrees of atmospheric contributions. The heaviest δ13C(CO2) values, indicatives of deep-seated CO2, were measured in soil gases in and around the summit crater, where fumarolic activity and thermal anomalies occur. The contribution of biogenic CO2 can be considered negligible, which is consistent with the very limited vegetation and its related biological activity in the summit cone of Teide volcano.Figure 4
A plot of13δC(CO2) versus 1/[CO2] (ppmV−1) data from the Teide summit cone and crater. This figure depicts three possible geochemical reservoirs: air, characterized by a δ13CCO2=−8‰ and CO2=0.04%, deep-seated CO2 with δ13CCO2=−3.1‰ and CO2=100%, and biogenic CO2 with δ13CCO2=−27.5‰ and CO2=100%. Mixing trend between biogenic, air-derived, and deep-seated CO2 is represented by straight lines.


### 4.2.4He Emission

The total output of4He from the studied area was estimated in 1.06±0.2kg d-1 (265.15 mol d-1) with the highest values observed where fumarolic activity is present, along the crater rim, and towards the north and north-east flanks, coinciding with the highest temperature and CO2 efflux values measured (Figure 5). The average value of the convective component exceeded the average value of the diffusive component by almost an order of magnitude (4.2 vs. 0.44 mg m-2 d-1, respectively). For this reason, we can assume that most of the diffuse gas emission from the summit cone of Teide volcano is governed by convection.Figure 5
Diffuse4He emission map for the summit cone and crater of Teide volcano.Similar studies carried out in other volcanic systems of the Canary Islands have taken into account only the diffusive component due to the lack of geothermal anomalies in the surface environment of the study areas. Padrón et al. [51] estimate a 4He emission between 15 and 38 kg d-1 from Cumbre Vieja volcano (La Palma) for an area of 220 km2. Padrón et al. [7] observed an increase in the diffusive component of 4He emission from 9 to 38 kg d-1 of the whole El Hierro island (278 km2) prior to and during the 2011-2012 submarine eruption that took place 2 km off the southern coast of the island. In the case of the summit cone of Teide, with an area of 0.5 km2, the normalized 4He emission rate is 2.12 kg km-2 d-1, which represents a much higher value than that calculated for Cumbre Vieja and El Hierro (0.17 and 0.14 kg km-2 d-1, respectively).The summit cone of Teide value for4He is comparable to Pico do Fogo volcano in Cape Verde. Dionis et al. [21] estimated a helium emission of 4.1 kg d-1 from the crater that has an area of 0.142 km2 by considering a pure convective emission and a normalized emission rate of 28 kg km-2 d-1. It is worth noting that Pico do Fogo volcano has experienced a higher eruptive activity in the historical times (last 500 years) than Teide. This observation might suggest a more general relationship between 4He emission and volcanic activity than that demonstrated at the scale of the Cape Verde archipelago by Dionis et al. [21] using CO2 and 3He emission.


### 4.3.3He Emission

Chemical and isotopic composition of fumarolic gases from the summit crater of Teide volcano are summarized in Table1.Table 1
Outlet temperature, chemical, and isotopic composition of fumarolic gases from the summit crater of Teide volcano.
T (°C)
4He/20Ne
3He/4He (R/RA)
δ13C-CO2 (‰)
CO2 (%)
Gas steam
Teide fumarole
83.3
33.613
6.723±0.056
−3.13±0.01
98.15
0.251Assuming that the3He/4He ratio analyzed from the fumaroles is the same for the whole hydrothermal system, the calculated diffuse 3He emission for the first assumption is 2.48×10−3mol d-1 (0.89 mol y-1). Nevertheless, because we have used the 4He flux calculated before for our estimation, the 3He emission could be overestimated because there must be some radiogenic 4He from the crust. Anyway, that amount of 4He from the crust is almost negligible for polygenetic volcanoes at oceanic islands as Tenerife [11]. For the second assumption, we use the CO2 flux calculated before because we assume that the 3He flux is wholly derived from deep-seated source. The calculated 3He emission is 9.69×10−4mol d-1 (0.35 mol y-1). In this case, some amount of CO2 derived from magma would be trapped by water in soil or groundwater during its ascent, so the true 3He flux is underestimated and should be higher than the estimate. Marrero et al. [52] estimates through a CO2 mass balance that 17.5×108mol y-1 (211 t d-1) of CO2 is discharged by the groundwaters of Las Cañadas aquifer (144 km2) (Figure 6). That means that there is a large amount of magmatic CO2 that is trapped in the aquifer during its ascent to the atmosphere, suggesting that 3He emission calculated using the second assumption is clearly subestimated.Figure 6
Hydrogeological model of Las Cañadas aquifer in the island of Tenerife. Fluid transport from the volcanic-hydrothermal system to the atmosphere is shown. Modified from Marrero-Díaz et al. [55].These summit-cone wide values are consistent with the crater-only value which was reported by Hernández et al. [53] to be 0.51 mol y-1 (after correction of an error observed in the original calculation).This work provides one more of the few values reported to date related to3He global emission, of which volcanic systems are highly significant. Other hot spot-type volcanic systems have shown similar (Piton de la Fournaise, La Réunion island, 1.1 mol y-1) or higher emission values (Kilauea, Hawaii, 9-14 mol y-1) [54], using fumarolic data. Other studies of soil 3He emission in volcanic areas are rare. Padrón et al. [51] estimated a total output of 3He in Cumbre Vieja volcano (La Palma, Canary Islands) of 0.6-0.7 mol y-1 considering a pure diffusive transport mechanism for an area of 220 km2.


### 4.4. Heat Flow

The computed thermal energy released by degassing of1.26×1012J d-1 corresponds to a total heat flow of 2.21 MW. We obtained a value of 8.1±0.97MW using the Dawson method. In the interpolation map, the areas with the highest heat flow occurred at the fumarolic areas inside the crater, the crater rim, and the NE flank (Figure 7). The fumarolic area in the crater of Teide volcano has an average temperature of 83.5°C that it is constant since it began to register in 1993. The major component of these fumaroles is the water vapour, which originates from the vaporization of the rainfall water [33] followed by CO2, N2, H2, H2S, Ar, CH4, and CO, a composition typical of hydrothermal fluids [34, 35]. These data suggest that the fumarolic effluents are made by endogenous gases which cross the aquifer located somewhere in the postcaldera structure close to the surface [33]. At the same time, the heat flux in the crater of Teide volcano has been registered since 2009 and no significant changes have been detected. Most of the heat flow measured in Teide volcano is the result of the emitted heat by the phase change of water from gas to liquid in the condensation zone.Figure 7
Heat flux emission map for the summit cone and crater of Teide volcano.The difference between the heat emission calculations among two different methods is because the method proposed by Chiodini et al. [46] assumes that the H2O/CO2 molar ratio measured in the fumarolic discharges is the same for the whole hydrothermal system. In this study, we are comparing areas with higher convective component at the crater with areas typified mainly by diffusive component at the flanks of the volcano, where there are no surface evidences of hydrothermal alteration.To compare our data with other volcanic systems, Hernández et al. [3] estimated a total heat flow of 1.24 MW for the Hengill volcanic system; Chiodini et al. [2] reported the energy released by other volcanic areas as Campi Flegrei 100.8 MW, Ischia 40.1 MW, Vesuvio cone 16.6 MW, Vulcano crater 21 MW, and Comalito cinder cone 0.9 MW, and Dionis et al. [21] estimated a value of 10.3 MW released from the summit crater of Pico do Fogo volcano.


### 4.5.3He/Heat Ratio

Following from the end-member assumptions used to calculate the3He and heat flux, we calculated a plausible 3He/heat ratio range from 0.117×10−12 to 0.764×10−12cm3 STP J-1, with an average value of 0.370×10−12cm3 STP J-1. This value is close to the 0.5 × 10-12 cm3 STP J-1 calculated for the 3He/heat ratio for hydrothermal activity from the upper mantle [19, 20]. Figure 8 shows the relationship between heat and helium emissions, following the model of Kennedy et al. [17], which demonstrate that Teide volcano is a useful window to take measurements of volatiles and heat from the upper mantle of the Earth to the atmosphere. By extension, future studies that focus upon the temporal evolution of heat and volatile emission from Teide and similar windows to the mantle will improve understanding of mantle dynamics and the link between lithosphere and atmosphere.Figure 8
Schematic representation of the coherence between heat and helium.


## 4.1. CO2 Fluxes and Isotopic Signatures

Diffuse CO2 efflux values ranged from below detection to 10,650 g m-2d-1 with an average value of 879 g m-2d-1. The spatially interpolated total diffuse CO2 output released from the summit cone of Teide volcano was calculated as 211±20t d-1. Similar results were obtained by Pérez et al. [37]; an emission value of 180±21 was calculated for the 2009 survey for an area of 0.11 km2.The diffuse CO2 emission map (Figure 3) shows higher values located inside the crater, along the crater rim mainly close to the fumarolic area and towards the north and north-east flanks. The areas with higher CO2 efflux values also show relatively high temperatures and appear correlated to hydrothermal alteration at the surface, suggesting a mainly advective degasification mechanism governing the gas emission regime at the study area. The north and north-east anomalies are probably related to radial fissures propagated from the volcanic axis [37]. Lower values are observed at other sectors of the flanks of the cone.Figure 3
Diffuse CO2 emission map of the summit cone and crater of Teide volcano.The total diffuse CO2 output is comparable with the 219±36t d-1 released by Pico do Fogo volcano, Cape Verde, a similar volcanic system in a similar volcano-tectonic environment, measured during a survey in February 2010 [21].Figure4 summarizes the CO2 isotopic composition and indicates that most of the analyzed samples correspond to a deep-seated source of CO2, with different degrees of atmospheric contributions. The heaviest δ13C(CO2) values, indicatives of deep-seated CO2, were measured in soil gases in and around the summit crater, where fumarolic activity and thermal anomalies occur. The contribution of biogenic CO2 can be considered negligible, which is consistent with the very limited vegetation and its related biological activity in the summit cone of Teide volcano.Figure 4
A plot of13δC(CO2) versus 1/[CO2] (ppmV−1) data from the Teide summit cone and crater. This figure depicts three possible geochemical reservoirs: air, characterized by a δ13CCO2=−8‰ and CO2=0.04%, deep-seated CO2 with δ13CCO2=−3.1‰ and CO2=100%, and biogenic CO2 with δ13CCO2=−27.5‰ and CO2=100%. Mixing trend between biogenic, air-derived, and deep-seated CO2 is represented by straight lines.


## 4.2.4He Emission

The total output of4He from the studied area was estimated in 1.06±0.2kg d-1 (265.15 mol d-1) with the highest values observed where fumarolic activity is present, along the crater rim, and towards the north and north-east flanks, coinciding with the highest temperature and CO2 efflux values measured (Figure 5). The average value of the convective component exceeded the average value of the diffusive component by almost an order of magnitude (4.2 vs. 0.44 mg m-2 d-1, respectively). For this reason, we can assume that most of the diffuse gas emission from the summit cone of Teide volcano is governed by convection.Figure 5
Diffuse4He emission map for the summit cone and crater of Teide volcano.Similar studies carried out in other volcanic systems of the Canary Islands have taken into account only the diffusive component due to the lack of geothermal anomalies in the surface environment of the study areas. Padrón et al. [51] estimate a 4He emission between 15 and 38 kg d-1 from Cumbre Vieja volcano (La Palma) for an area of 220 km2. Padrón et al. [7] observed an increase in the diffusive component of 4He emission from 9 to 38 kg d-1 of the whole El Hierro island (278 km2) prior to and during the 2011-2012 submarine eruption that took place 2 km off the southern coast of the island. In the case of the summit cone of Teide, with an area of 0.5 km2, the normalized 4He emission rate is 2.12 kg km-2 d-1, which represents a much higher value than that calculated for Cumbre Vieja and El Hierro (0.17 and 0.14 kg km-2 d-1, respectively).The summit cone of Teide value for4He is comparable to Pico do Fogo volcano in Cape Verde. Dionis et al. [21] estimated a helium emission of 4.1 kg d-1 from the crater that has an area of 0.142 km2 by considering a pure convective emission and a normalized emission rate of 28 kg km-2 d-1. It is worth noting that Pico do Fogo volcano has experienced a higher eruptive activity in the historical times (last 500 years) than Teide. This observation might suggest a more general relationship between 4He emission and volcanic activity than that demonstrated at the scale of the Cape Verde archipelago by Dionis et al. [21] using CO2 and 3He emission.


## 4.3.3He Emission

Chemical and isotopic composition of fumarolic gases from the summit crater of Teide volcano are summarized in Table1.Table 1
Outlet temperature, chemical, and isotopic composition of fumarolic gases from the summit crater of Teide volcano.
T (°C)
4He/20Ne
3He/4He (R/RA)
δ13C-CO2 (‰)
CO2 (%)
Gas steam
Teide fumarole
83.3
33.613
6.723±0.056
−3.13±0.01
98.15
0.251Assuming that the3He/4He ratio analyzed from the fumaroles is the same for the whole hydrothermal system, the calculated diffuse 3He emission for the first assumption is 2.48×10−3mol d-1 (0.89 mol y-1). Nevertheless, because we have used the 4He flux calculated before for our estimation, the 3He emission could be overestimated because there must be some radiogenic 4He from the crust. Anyway, that amount of 4He from the crust is almost negligible for polygenetic volcanoes at oceanic islands as Tenerife [11]. For the second assumption, we use the CO2 flux calculated before because we assume that the 3He flux is wholly derived from deep-seated source. The calculated 3He emission is 9.69×10−4mol d-1 (0.35 mol y-1). In this case, some amount of CO2 derived from magma would be trapped by water in soil or groundwater during its ascent, so the true 3He flux is underestimated and should be higher than the estimate. Marrero et al. [52] estimates through a CO2 mass balance that 17.5×108mol y-1 (211 t d-1) of CO2 is discharged by the groundwaters of Las Cañadas aquifer (144 km2) (Figure 6). That means that there is a large amount of magmatic CO2 that is trapped in the aquifer during its ascent to the atmosphere, suggesting that 3He emission calculated using the second assumption is clearly subestimated.Figure 6
Hydrogeological model of Las Cañadas aquifer in the island of Tenerife. Fluid transport from the volcanic-hydrothermal system to the atmosphere is shown. Modified from Marrero-Díaz et al. [55].These summit-cone wide values are consistent with the crater-only value which was reported by Hernández et al. [53] to be 0.51 mol y-1 (after correction of an error observed in the original calculation).This work provides one more of the few values reported to date related to3He global emission, of which volcanic systems are highly significant. Other hot spot-type volcanic systems have shown similar (Piton de la Fournaise, La Réunion island, 1.1 mol y-1) or higher emission values (Kilauea, Hawaii, 9-14 mol y-1) [54], using fumarolic data. Other studies of soil 3He emission in volcanic areas are rare. Padrón et al. [51] estimated a total output of 3He in Cumbre Vieja volcano (La Palma, Canary Islands) of 0.6-0.7 mol y-1 considering a pure diffusive transport mechanism for an area of 220 km2.


## 4.4. Heat Flow

The computed thermal energy released by degassing of1.26×1012J d-1 corresponds to a total heat flow of 2.21 MW. We obtained a value of 8.1±0.97MW using the Dawson method. In the interpolation map, the areas with the highest heat flow occurred at the fumarolic areas inside the crater, the crater rim, and the NE flank (Figure 7). The fumarolic area in the crater of Teide volcano has an average temperature of 83.5°C that it is constant since it began to register in 1993. The major component of these fumaroles is the water vapour, which originates from the vaporization of the rainfall water [33] followed by CO2, N2, H2, H2S, Ar, CH4, and CO, a composition typical of hydrothermal fluids [34, 35]. These data suggest that the fumarolic effluents are made by endogenous gases which cross the aquifer located somewhere in the postcaldera structure close to the surface [33]. At the same time, the heat flux in the crater of Teide volcano has been registered since 2009 and no significant changes have been detected. Most of the heat flow measured in Teide volcano is the result of the emitted heat by the phase change of water from gas to liquid in the condensation zone.Figure 7
Heat flux emission map for the summit cone and crater of Teide volcano.The difference between the heat emission calculations among two different methods is because the method proposed by Chiodini et al. [46] assumes that the H2O/CO2 molar ratio measured in the fumarolic discharges is the same for the whole hydrothermal system. In this study, we are comparing areas with higher convective component at the crater with areas typified mainly by diffusive component at the flanks of the volcano, where there are no surface evidences of hydrothermal alteration.To compare our data with other volcanic systems, Hernández et al. [3] estimated a total heat flow of 1.24 MW for the Hengill volcanic system; Chiodini et al. [2] reported the energy released by other volcanic areas as Campi Flegrei 100.8 MW, Ischia 40.1 MW, Vesuvio cone 16.6 MW, Vulcano crater 21 MW, and Comalito cinder cone 0.9 MW, and Dionis et al. [21] estimated a value of 10.3 MW released from the summit crater of Pico do Fogo volcano.


## 4.5.3He/Heat Ratio

Following from the end-member assumptions used to calculate the3He and heat flux, we calculated a plausible 3He/heat ratio range from 0.117×10−12 to 0.764×10−12cm3 STP J-1, with an average value of 0.370×10−12cm3 STP J-1. This value is close to the 0.5 × 10-12 cm3 STP J-1 calculated for the 3He/heat ratio for hydrothermal activity from the upper mantle [19, 20]. Figure 8 shows the relationship between heat and helium emissions, following the model of Kennedy et al. [17], which demonstrate that Teide volcano is a useful window to take measurements of volatiles and heat from the upper mantle of the Earth to the atmosphere. By extension, future studies that focus upon the temporal evolution of heat and volatile emission from Teide and similar windows to the mantle will improve understanding of mantle dynamics and the link between lithosphere and atmosphere.Figure 8
Schematic representation of the coherence between heat and helium.


## 5. Conclusions

Most of the volcano-hydrothermal fluid discharges occurring at the summit cone of Teide volcano occur in the crater area; yet, other important emission rates were measured along the north and north-east flanks. These extracrater emissions are suggestive of a strong structural control in the degassing process of Teide volcano. Given the prevalence of structural controls on the expression of volcanic systems worldwide, we can suggest that other important, yet not as obvious, emissions are likely to be encountered at other volcanic systems.The estimated global volcanic emission of3He is 1250±250mol y-1 [54]. The contribution to this estimate emission obtained by Teide volcano in this work is about 0.62 mol y-1, for an area of 0.5 km2, 0.05% of the total global emission. This study provides the first estimation of 3He/heat from the Teide volcanic system and supports theoretical estimates at a global scale. The calculation of flux supports the presence of an important mantle source of volatiles and heat to the atmosphere.



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*Source: 3983864-2019-06-23.xml*