# Organic, Gas, and Element Geochemistry of Hydrothermal Fluids of the Newly Discovered Extensive Hydrothermal Area in the Wallis and Futuna Region (SW Pacific)

Authors: C. Konn; J. P. Donval; V. Guyader; E. Roussel; E. Fourré; P. Jean-Baptiste; E. Pelleter; J. L. Charlou; Y. Fouquet
Journal: Geofluids
 (2018)

---

## Abstract

Two newly discovered hydrothermal vent fields of the Wallis and Futuna region, Kulo Lasi and Fatu Kapa, were sampled for fluid geochemistry. A great geochemical diversity was observed and assigned to the diversity of lithologies as well as the occurrence of various processes. Kulo Lasi fluids likely formed by interaction with fresh volcanic rocks, phase separation, and mixing with magmatic fluid. Conversely, the geochemistry of the Fatu Kapa fluids would be mostly due to water/felsic lavas reactions. In terms of organic geochemistry, fluids from both fields were found to be enriched in formate, acetate, and semivolatile organic compounds (SVOCs): n-alkanes, n-fatty acids, and polyaromatic hydrocarbons (PAHs). Concentrations of SVOCs reached a few ppb at most. The distribution patterns of SVOCs indicated that several processes and sources, at once of biogenic, thermogenic, and abiogenic types, likely controlled organic geochemistry. Although the contribution of each process remains unknown, the mere presence of organics at theμM level has strong implications for metal dispersion (cycles), deposition (ore-forming), and bioavailability (ecosystems), especially as our fluxes estimations suggest that back-arc hosted vent fields could contribute as much as MOR to the global ocean heat and mass budget.


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## Body

## 1. Introduction

Although back-arc settings are favourable environments for the formation of hydrothermal convection cells, hydrothermal exploration has long been conducted to a greater extent on Mid-Oceanic Ridges (MOR). Today, more than 600 active hydrothermal vent fields have been discovered and about half of them are located at MOR against a fifth in back-arc basins (BAB) [1]. Yet back-arc environments are likely to generate more diversity than their MOR homologs in terms of fluid chemistry because of the variety of lithologies the fluids can react with (e.g., basaltic to rhyolitic volcanic rocks with or without arc-like geochemical signature, various alteration mineralogical assemblages) as well as the possible contribution of magmatic-related aqueous fluids [2–5]. The Wallis and Futuna area was surveyed for hydrothermal activity because of its very peculiar geological settings within a back-arc system and its potential relevance for mineral resources [6, 7]. It is located about 200 km west of the northern tip of the Tonga-Kermadec trench where the fastest subduction rates have been recorded (18 to 24 cm per year) and occur at the junction of 2 BAB: the Lau and the North-Fiji BAB [8]. Here we report on the geochemistry of the fluids of the very first two vent fields discovered in the area and in this type of environment. We chose to bring a special focus on organic geochemistry because it has been hardly studied in modern hydrothermal systems despite the recent growing interest for organic matter (OM) in the ocean. The discussion focuses on processes controlling the geochemistry as well as implications of the presence of organic molecules at the local and regional scales.Organic geochemistry of hydrothermal fluids has generally been far less studied than the mineral and gas geochemistry. In most cases works focused on small molecules (hydrocarbon gases, volatile fatty acids, and amino acids) and very few data are available on semivolatile organic compounds (SVOCs). Despite the growing interest for OM in the ocean and hydrothermal systems there is still a major lack in identification and quantification of organic compounds [10–15]. Notably numbers of studies agree on the major ligand role of organics in metal stabilisation, transportation, bioavailability, and ore-forming but there are hardly any clues on the nature of these ligands in hydrothermal environments [16–25]. Organic compounds in hydrothermal fluids may come from marine dissolved organic matter (DOM) recycling [12, 13], subsurface biomass degradation [26], entrainment of organic detritus from local recharge zones, and subsequent degradation, or abiotic formation in the deep subsurface [27–30]. The latter is supported by many theoretical [31–33] and experimental work summarised in two reviews [34, 35]. Conversely, some other studies reported the absence of organic compounds in hydrothermal fluids except at the Lost City alkaline vent field which is theoretically more favourable for abiotic synthesis [36]. Nevertheless, we report here the presence of semivolatile organic compounds in hydrothermal fluids from the Wallis and Futuna area and provide concentrations of a selection of extractable compounds that have been identified elsewhere as hydrothermally derived [27, 37]: n-alkanes, n-fatty acids (n-FAs), mono-, and polyaromatic hydrocarbons (BTEXs and PAHs). These very first quantitative field data might feed thermodynamic models of abiotic synthesis, guide the design of experiments to better understand hydrothermal organic geochemistry, and help assessing the importance of hydrothermally derived organic compounds in metal complexation and, as a nutrient for microorganisms, complete fluxes calculation and enter in the carbon cycle budget calculations.


## 2. Geological Settings

Wallis and Futuna Islands are located at the transition between the North Fiji and the Lau back-arc basins. This geodynamical setting accounts for complex volcanic and tectonic activity in the area. Pelletier et al. [38] and Fouquet et al. [6] observed multiple active extensional zones including widespread areas composed of numerous individual volcanoes (e.g., Southeast Futuna volcanic zone (SEVZ)) and well organised spreading centers such as the Futuna and Alofi oceanic ridge. West of Futuna Island, the 20–30° trending Futuna spreading center (FSC), is composed of a series of en echelon spreading segments. The opening rate of this oceanic ridge has been estimated at 4 cm/yr from the interpretation of magnetic anomalies [38]. East and southeast of Futuna Island, bathymetric maps, and reflectivity data clearly reveal that active extension and recent volcanism occur in the SEVZ as well as along the Alofi spreading center [6]. The SEVZ is a broad zone of diffuse volcanism bordered by the ENE-WSW trending volcanic graben (named Tasi Tulo graben) to the north and the NNE-SSW trending Alofi spreading center to the south. The SEVZ includes Kulo Lasi active volcano, the Fatu Kapa, and Tasi Tulo volcanic zones ([7], Figure 1).Figure 1
Bathymetric map of the study area. Close-ups of Fatu Kapa and Kulo Lasi are shown in boxes where sample positions are marked with red disks. Copyrights from Ifremer, FUTUNA 1, 2, and 3 cruises.Fluids were sampled at the Kulo Lasi and Fatu Kapa sites. Kulo Lasi has been described in detail by Fouquet and collaborators [39]. In summary, it is a shield volcano located about 100 km southeast of Futuna Island (Figure 1). It represents the most recent volcano in the SEVZ and is composed of basaltic to trachy-andesitic lava with no direct geochemical affinity with subduction [39]. The volcanic edifice is ca. 20 km in diameter and appears relatively flat with the top located at a depth of 1200 m and the base only 300 m deeper (ca. 1500 m below sea level). It exhibits a central caldera (5 km in diameter and 200–300 m deep) with a flat bottom covered by recent lavas and a central mound composed of older and tectonised lava flow. By contrast, the Fatu Kapa volcanic area is in a 20 km wide transition zone between the Tasi Tulo graben and the Kulo Lasi volcano. Here only small (<1 km) volcanic edifices are seen to be consisting of young mafic to felsic lavas (Figure 1).


## 3. Sampling and Analytical Procedures

Sampling was achieved at Kulo Lasi and Fatu Kapa by the HOV Nautile during the FUTUNA 1 and FUTUNA 3 cruises conducted by Ifremer in 2010 and 2012. Fluid samples were taken at the nose of smokers to minimise seawater contamination. Samples of volumes up to 750 mL of hydrothermal fluids were collected in titanium syringes that were modified after the model described in Von Damm et al. [40]. The gas-tightness was greatly improved and ensured the majority of the gas to be recovered. Those same syringes have been used in several studies by Charlou et al. and have shown good results notably for gas-Mg correlations (e.g., Charlou et al., 2002). Autonomous temperature sensors (S2T 6000-DH, NKE Instrumentation) were mounted on the sampler nozzle. As soon as the fluids were recovered, pH, H2S, and Cl- concentrations were measured to evaluate the quality of the sample. Total gases were immediately extracted and analysed; then aliquots of gas were conditioned for further stable isotopes measurements. Finally, the gas-free fluid was conditioned for major and minor elements analyses, on the one hand, and for organic compounds analyses, on the other hand.


### 3.1. Gas Extraction and Analyses

Total gas was extracted as described in Charlou and Donval [41]. Preliminary major gases (CO2, H2, CH4, and N2) concentrations were obtained on board by using a portable chromatograph(Microsensor Technology Instruments Inc.) that was mounted on line with the gas extractor. Extracted gases were conditioned on board in stainless steel pressure-tight flasks and stored until analyses. Gases were separated by Gas-Chromatography (Agilent GC 7890A,Agilent Technologies) and quantitatively analysed by triple detection using mass (MS 5975C,Agilent technologies), flame ionisation, and thermal conductivity detectors. Aliquots of gas were stored both in vacuum tight tubes(Labco, Ltd.) and in copper tubes to be sent for further carbon isotope analyses(Isolab b.v., Netherlands) and He isotopes analyses(CEA, Saclay, France), respectively.


### 3.2. Inorganic Geochemistry: Sample Preparation and Analyses

pH was measured using a combined glass electrode(Ecotrode Plus, Metrohm). Cl− and H2S were measured by potentiometry using AgNO3 (0.05 M) and HgCl2 (0.01 M) as titrating solutions, respectively. NaOH (2 M) was added to the aliquot before H2S measurement. SO4, Br, Na, K, Mg, Ca, Li, and Cl were measured by ionic chromatography(Dionex Ion Chromatograph System 2000) after appropriate dilutions. Fe, Mn, Cu, Zn, Sr, Li, and Rb were measured by flame atomic absorption spectrometry using standard additions(AAnalyst, Perkin Elmer Inc.). Aliquots for silica determination were immediately diluted 100- to 200-fold and analysed by the silicomolybdate automatic colorimetric method [42, 43].


### 3.3. Organic Geochemistry

Total Organic Carbon (TOC) was measured using a multi N/C 3100(Analytik Jena AG, Germany). Samples were acidified online with HCl and then purged with O
2 to remove inorganic carbon (IC). A TIC control analysis was performed and followed by three TOC measurements on each sample.Acetate and formate concentrations were determined using a Dionex ICS-2000 Reagent-Free Ion Chromatography System equipped with an AS50 autosampler(Dionex Camberley, UK). Chromatographic separation was conducted using two Ionpac AS15 columns in series at 30°C and the determination of species was carried out using an Anion Self-Regenerating Suppressor(ASRS 300 4 mm) unit in combination with a DS6 heated conductivity cell (35°C). The gradient program was as follows: 6 mmol L−1 KOH (43 min); increase from 27 mmol L−1 KOH min−1 to 60 mmol L−1 (39 min); decrease from 54 mmol L−1 KOH min−1 to 6 mmol L−1 (5 min).SVOCs were extracted using Stir Bar Sorptive Extraction (SBSE). Basically any compound with a log Ko/w > 2.5 is recovered with a rate > 50% [44]. The method was improved after Konn et al. [37]. The entire content of the titanium syringe was transferred into a precombusted glass bottle and six 90 mL aliquots of the sample were poured into 100 mL precombusted glass vials. 10 mL of MeOH was added to avoid adsorption of the compounds onto the wall of the vials. Internal standards were added to the solutions in 2012 so that quantification could only be achieved in Fatu Kapa fluids. Extraction was performed in sealed vials with ultrainert septum crimps, at 300 rpm and using 48 μL PDMS Twisters® (Gerstel GmbH). We focused on a selection of chemical groups that had previously been described as hydrothermally derived [27]. To that respect, pairs of aliquots were dedicated to analysis of n-alkanes, n-FAs, and both BTEXs and PAHs, respectively. Extraction kinetics experiments showed that chemical equilibrium was reached after 5 h of extraction for n-alkanes, 4 h for PAHs and 14 h for n-FAs (Konn, unpublished results). Twisters were then removed, rinsed with MQ water, dried, and stored at +4°C until analyses by Thermal Desorption-Gas Chromatography-Mass Spectrometry (TD-GC-MS) [37]. Analytical parameters were adjusted for each group of compounds (Table 1).Table 1
Main GC analytical parameters used for calibration and analyses of hydrothermal fluid samples. Each group of compounds (n-alkanes, BTEXs, PAHs, and n-fatty acids) was analysed using separate twisters.
n-Alkanes
BTEX & PAHs
n-Fatty acids
Oven
InitialT (°C)
40
40
40
Initialt (min)
1
1
1
ramp
40 to 320°C at 12°C/min
40 to 320°C at 12°C/min
40 to 320°C at 20°C/min
FinalT (°C)
320
320
320
Finalt (min)
2
2
2
Injector
T (°C)
250
250
325For each batch of conditioned Twisters, one was spared, stored at +4°C, and analysed in the same run as the other Twisters. This dry blank aimed at showing any contamination that could have occurred during conditioning, storage, and transport. MQ water samples were prepared and extracted on board as regular hydrothermal samples to check if any contaminations could have occurred during the sample preparation step. Deep-sea water was also collected, processed, and analysed, using the same titanium syringes and according to the same protocols as for hydrothermal fluid samples, and thus constitute the reference blank experiment.Calibration was achieved using a commercial standard solution of BTEXs and 3 custom standard solutions of C9–C20  n-alkanes, C6–C18  n-FAs, and PAHs containing naphthalene (N), Acenaphtene (A), Fluorene (F), Phenanthrene (Ph), Anthracene (An), Fluoranthene (Fl), and pyrene (Py)(LGC Standards, LGC Ltd.). Deuterated n-alkanes (C10D22 and C14D34), methyl esters (C9H18O2 and C15H30O2), and deuterated PAHs (naphthalene-D8, Biphenyl-D8, and Phenanthrene-D10) were used as internal standards (IS). Calibration curves (Concentration (analyte)/Concentration (IS) versus Area (analyte)/Area (IS)) were obtained using at least five concentration levels that were replicated 3 times (Table 2). Although the correlation coefficient of the linear regressions was satisfactory for all compounds, the significance and lack of fit of the model were checked by statistical tests before validation. A series of Student, Barlett, Chi-square, and Fisher tests was run for each individual compound using the Lumière software. The best fitting model was then chosen for each case and confidence intervals were calculated.Table 2
Experimental conditions used for calibration curves. Linear regressions were performed on one order of magnitude concentration domain depending on the concentration range of the samples.
n-Alkanes
BTEX & PAHs
n-Fatty acids
Concentration levels (µg·L−1)
0.5, 1, 2, 5, 10
0.05, 0.1, 0.25, 0.5, 1, 2, 5, 10
0.25, 0.5, 1, 2, 5, 10
IS concentration (µg·L−1)
5
5
10


## 3.1. Gas Extraction and Analyses

Total gas was extracted as described in Charlou and Donval [41]. Preliminary major gases (CO2, H2, CH4, and N2) concentrations were obtained on board by using a portable chromatograph(Microsensor Technology Instruments Inc.) that was mounted on line with the gas extractor. Extracted gases were conditioned on board in stainless steel pressure-tight flasks and stored until analyses. Gases were separated by Gas-Chromatography (Agilent GC 7890A,Agilent Technologies) and quantitatively analysed by triple detection using mass (MS 5975C,Agilent technologies), flame ionisation, and thermal conductivity detectors. Aliquots of gas were stored both in vacuum tight tubes(Labco, Ltd.) and in copper tubes to be sent for further carbon isotope analyses(Isolab b.v., Netherlands) and He isotopes analyses(CEA, Saclay, France), respectively.


## 3.2. Inorganic Geochemistry: Sample Preparation and Analyses

pH was measured using a combined glass electrode(Ecotrode Plus, Metrohm). Cl− and H2S were measured by potentiometry using AgNO3 (0.05 M) and HgCl2 (0.01 M) as titrating solutions, respectively. NaOH (2 M) was added to the aliquot before H2S measurement. SO4, Br, Na, K, Mg, Ca, Li, and Cl were measured by ionic chromatography(Dionex Ion Chromatograph System 2000) after appropriate dilutions. Fe, Mn, Cu, Zn, Sr, Li, and Rb were measured by flame atomic absorption spectrometry using standard additions(AAnalyst, Perkin Elmer Inc.). Aliquots for silica determination were immediately diluted 100- to 200-fold and analysed by the silicomolybdate automatic colorimetric method [42, 43].


## 3.3. Organic Geochemistry

Total Organic Carbon (TOC) was measured using a multi N/C 3100(Analytik Jena AG, Germany). Samples were acidified online with HCl and then purged with O
2 to remove inorganic carbon (IC). A TIC control analysis was performed and followed by three TOC measurements on each sample.Acetate and formate concentrations were determined using a Dionex ICS-2000 Reagent-Free Ion Chromatography System equipped with an AS50 autosampler(Dionex Camberley, UK). Chromatographic separation was conducted using two Ionpac AS15 columns in series at 30°C and the determination of species was carried out using an Anion Self-Regenerating Suppressor(ASRS 300 4 mm) unit in combination with a DS6 heated conductivity cell (35°C). The gradient program was as follows: 6 mmol L−1 KOH (43 min); increase from 27 mmol L−1 KOH min−1 to 60 mmol L−1 (39 min); decrease from 54 mmol L−1 KOH min−1 to 6 mmol L−1 (5 min).SVOCs were extracted using Stir Bar Sorptive Extraction (SBSE). Basically any compound with a log Ko/w > 2.5 is recovered with a rate > 50% [44]. The method was improved after Konn et al. [37]. The entire content of the titanium syringe was transferred into a precombusted glass bottle and six 90 mL aliquots of the sample were poured into 100 mL precombusted glass vials. 10 mL of MeOH was added to avoid adsorption of the compounds onto the wall of the vials. Internal standards were added to the solutions in 2012 so that quantification could only be achieved in Fatu Kapa fluids. Extraction was performed in sealed vials with ultrainert septum crimps, at 300 rpm and using 48 μL PDMS Twisters® (Gerstel GmbH). We focused on a selection of chemical groups that had previously been described as hydrothermally derived [27]. To that respect, pairs of aliquots were dedicated to analysis of n-alkanes, n-FAs, and both BTEXs and PAHs, respectively. Extraction kinetics experiments showed that chemical equilibrium was reached after 5 h of extraction for n-alkanes, 4 h for PAHs and 14 h for n-FAs (Konn, unpublished results). Twisters were then removed, rinsed with MQ water, dried, and stored at +4°C until analyses by Thermal Desorption-Gas Chromatography-Mass Spectrometry (TD-GC-MS) [37]. Analytical parameters were adjusted for each group of compounds (Table 1).Table 1
Main GC analytical parameters used for calibration and analyses of hydrothermal fluid samples. Each group of compounds (n-alkanes, BTEXs, PAHs, and n-fatty acids) was analysed using separate twisters.
n-Alkanes
BTEX & PAHs
n-Fatty acids
Oven
InitialT (°C)
40
40
40
Initialt (min)
1
1
1
ramp
40 to 320°C at 12°C/min
40 to 320°C at 12°C/min
40 to 320°C at 20°C/min
FinalT (°C)
320
320
320
Finalt (min)
2
2
2
Injector
T (°C)
250
250
325For each batch of conditioned Twisters, one was spared, stored at +4°C, and analysed in the same run as the other Twisters. This dry blank aimed at showing any contamination that could have occurred during conditioning, storage, and transport. MQ water samples were prepared and extracted on board as regular hydrothermal samples to check if any contaminations could have occurred during the sample preparation step. Deep-sea water was also collected, processed, and analysed, using the same titanium syringes and according to the same protocols as for hydrothermal fluid samples, and thus constitute the reference blank experiment.Calibration was achieved using a commercial standard solution of BTEXs and 3 custom standard solutions of C9–C20  n-alkanes, C6–C18  n-FAs, and PAHs containing naphthalene (N), Acenaphtene (A), Fluorene (F), Phenanthrene (Ph), Anthracene (An), Fluoranthene (Fl), and pyrene (Py)(LGC Standards, LGC Ltd.). Deuterated n-alkanes (C10D22 and C14D34), methyl esters (C9H18O2 and C15H30O2), and deuterated PAHs (naphthalene-D8, Biphenyl-D8, and Phenanthrene-D10) were used as internal standards (IS). Calibration curves (Concentration (analyte)/Concentration (IS) versus Area (analyte)/Area (IS)) were obtained using at least five concentration levels that were replicated 3 times (Table 2). Although the correlation coefficient of the linear regressions was satisfactory for all compounds, the significance and lack of fit of the model were checked by statistical tests before validation. A series of Student, Barlett, Chi-square, and Fisher tests was run for each individual compound using the Lumière software. The best fitting model was then chosen for each case and confidence intervals were calculated.Table 2
Experimental conditions used for calibration curves. Linear regressions were performed on one order of magnitude concentration domain depending on the concentration range of the samples.
n-Alkanes
BTEX & PAHs
n-Fatty acids
Concentration levels (µg·L−1)
0.5, 1, 2, 5, 10
0.05, 0.1, 0.25, 0.5, 1, 2, 5, 10
0.25, 0.5, 1, 2, 5, 10
IS concentration (µg·L−1)
5
5
10


## 4. Results

Altogether 35 hot fluid samples were collected in the study area from 8 different sites: Kulo Lasi caldera(
6
), on the one hand, and Stéphanie (
7
), Carla (
4
), I
d
e
f
X  (
4
), O
b
e
l
X  (
3
), A
s
t
e
r
X  (
1
), Fati Ufu (
6
), and Tutafi (
4
), on the other hand, all located in the Fatu Kapa area (Figure 1). The Kulo Lasi smokers occurred at ~1500 m depth on recent lava flows and consisted in a multitude of short (~25 cm) and narrow (~3–5 cm) diameter anhydrite chimneys containing a small percentage of sphalerite (ZnS), chalcopyrite (CuFeS2), isocubanite (CuFe2S3), pyrrhotite (F
e
1
-
x
S), and pyrite (FeS2) (Figure 2). The temperature was consistently about 343°C and the pH approached 2.2–2.3 (Table 3). In the Fatu Kapa area we could distinguish two types of hydrothermal environments at 1550–1650 m depth. Translucent 270–290°C fluids associated with anhydrite chimneys (up to 25 m tall and 2.5 m in diameter) characterised Stéphanie, Carla, I
d
e
f
X, O
b
e
l
X, and A
s
t
e
r
X sites, while >300°C milky to grey fluids associated with sulphide chimneys were characteristic of the southwest region including Fati Ufu and Tutafi sites (Figure 3, Table 3).Table 3
Measured concentration of major and minor elements in hydrothermal fluids from the Kulo Lasi and Fatu Kapa vent fields. FUX-PLYY-TiDZ and FUX-PLYY-TiGZ are replicate samples taken in the same orifice, one after the other, but using 2 individual Ti syringes.Tmax (chimney) is the maximum T of the discharged fluid for the given chimney which was recorded by the T probe of the submarine before sampling. Tmax (sample) is the maximum T of the fluid entering the sampler recorded during sampling by the autonomous sensor that was coupled at the nozzle of the sampler.
Sample name
Zone
Site
Description
Depth
Tmax (sample) °C
Tmax (chimney) °C
pH
d
20 Kg m−3
S
‰
NaCl(wt%)
ClmM
SimM
S
O
4 mM
Br
µM
NamM
KmM
MgmM
CamM
Li
µM
Li
µM
Rb
µM
Sr
µM
Fe
µM
Mn
µM
Cu
µM
Zn
µM
Na/Cl
Br/Cl×103
Na/K
C
H
4/Mn
IAPSO
-
-
Standard water
-
-
-
-
-
35
3.2
546
0.0
28.2
839
468
10.2
53.2
10.3
27
27
1.3
90
<LOD
<LOD
<LOD
<LOD
0.9
1.5
46
-
FU-PL-05-TiG2
Kulo Lasi
South (out)
Reference water
1150
-
-
-
1.023
35
3.2
551
0.1
29.0
833
457
9.8
53.2
10.6
25
28
4.4
93
<LOD
<LOD
<LOD
<LOD
0.83
1.5
47
-
FU-PL-05-TiG1
Kulo Lasi
South (in)
Diffuse fluid above worms
1414
32.8
-
5.96
1.023
35
3.2
549
0.2
29.3
833
457
9.9
53.2
10.6
28
52
4.6
92
<LOD
<LOD
1.4
1.5
0.83
1.5
46
-
FU-PL-06-TiG4
Kulo Lasi
North (in)
Beehive type black smoker
1475
134.1
332
6.07
1.022
33
3.0
516
1.0
27.0
822
448
10.6
49.8
10.5
33
54
5.3
84
123
32
1.7
3.1
0.87
1.6
42
-
FU-PL-06-TiD4
Kulo Lasi
North (in)
Beehive type black smoker
1475
136
332
5.58
1.021
31
2.8
485
2.1
23.9
994
406
9.5
45.7
10.2
32
55
6.1
74
78
76
1.3
1.5
0.84
2.0
43
0.010
FU-PL-06-TiG3
Kulo Lasi
North (in)
Translucent smoker
1475
342.3
330.7
2.24
1.017
32
2.9
497
8.2
8.8
738
388
18.5
24.6
11.6
149
156
26
7.3
4796
862
14
45
0.78
1.5
21
0.007
FU-PL-06-TiD3
Kulo Lasi
North (in)
Translucent smoker
1475
337.7
330.7
2.37
1.018
33
3.0
517
8.4
10.7
770
405
16.6
28.6
10.8
115
149
24
9.4
4283
788
4.2
41
0.78
1.5
24
-
FU-PL-06-TiD1
Kulo Lasi
North (in)
Black smoker
1475
343.2
345.1
2.36
1.02
47
4.3
735
14.6
6.2
1135
612
29.5
26.5
10.9
238
249
46
3.4
9884
1416
2.5
175
0.83
1.5
21
-
FU-PL-06-TiG1
Kulo Lasi
North (in)
Black smoker
1475
343.2
345.1
3.32
1.028
44
4.0
689
10.8
12.0
1051
565
23.7
34.9
10.8
176
197
36
9.1
6845
1064
20
77
0.82
1.5
24
0.001
FU3-PL-03-TiD3
Fatu Kapa
20 masf
Reference water
1488
-
-
-
-
-
3.3
565
0.0
28.8
841
483
10.4
54.5
10.7
22
51
6
<LOD
<LOD
<LOD
<LOD
<LOD
0.85
1.5
46
-
FU3-PL-14-TiG2
Fatu Kapa
23 masf
Reference water
1572
2
-
-
-
36
3.3
557
0.0
28.7
841
477
10.4
54.2
10.8
23
nm
nm
nm
nm
nm
nm
nm
0.86
1.5
46
-
FU3-PL-04-TiD3
Fatu Kapa
Stéphanie
Translucent smoker
1554
213
279
4.65
1.03
45
4.1
704
0.7
10.9
1300
519
39.8
18.7
69.6
472
568
80
<LOD
169
166
nm
<LOD
0.74
1.8
13
-
FU3-PL-04-TiG3
Fatu Kapa
Stéphanie
Translucent smoker
1554
213
279
4.64
1.03
44
4.0
686
1.0
12.9
1240
513
36.5
22.5
62.8
420
504
71
169
nm
141
8.2
<LOD
0.75
1.8
14
0.805
FU3-PL-08-TiD1
Fatu Kapa
Stéphanie
Translucent smoker
1555
289
280
4
1.031
49
4.5
770
3.8
1.3
1574
535
54.2
0.8
98.9
705
804
121
268
655
265
6.6
<LOD
0.69
2.0
10
0.886
FU3-PL-08-TiG1
Fatu Kapa
Stéphanie
Translucent smoker
1555
289
280
3.41
1.031
49
4.5
772
4.7
0.7
1592
537
54.7
0.5
98.7
708
807
122
283
167
269
nm
<LOD
0.70
2.1
10
0.762
FU3-PL-08-TiD2
Fatu Kapa
Stéphanie
Translucent smoker
1555
291
280
3.83
1.031
48
4.4
748
4.3
0.5
1537
520
52.9
0.6
95.3
684
806
116
<LOD
148
259
nm
<LOD
0.70
2.1
10
-
FU3-PL-09-TiD2
Fatu Kapa
Stéphanie
Beehive type black smoker + bacterial mat
1650
197
236
5.19
1.026
40
3.7
629
1.7
19.8
1052
500
24.4
37.4
37.8
230
293
36
149
nm
65
nm
1.0
0.79
1.7
21
0.902
FU3-PL-09-TiG2
Fatu Kapa
Stéphanie
Beehive type black smoker + bacterial mat
1559
197
236
5.42
1.025
38
3.5
600
1.0
23.8
959
489
18.5
44.3
26.4
143
193
23
<LOD
nm
23
nm
<LOD
0.81
1.6
26
-
FU3-PL-06-TiD1
Fatu Kapa
Carla
Translucent smoker
1663
278
270
5.03
1.024
37
3.4
576
1.7
18.5
927
482
28.5
35.2
17.9
260
310
42
101
nm
nm
nm
<LOD
0.84
1.6
17
-
FU3-PL-06-TiG1
Fatu Kapa
Carla
Translucent smoker
1663
278
270
4.91
1.024
37
3.4
579
0.7
12.7
984
476
37.8
23.6
22.2
391
455
63
<LOD
18
32
nm
<LOD
0.82
1.7
13
-
FU3-PL-08-TiD3
Fatu Kapa
Carla
Translucent smoker
1664
281
281
2.78
1.024
38
3.5
594
4.5
1.1
1139
479
59.6
0.4
31.5
690
746
104
115
nm
48
nm
4.4
0.80
1.9
8
1.365
FU3-PL-08-TiG3
Fatu Kapa
Carla
Translucent smoker
1664
281
281
4.17
1.024
38
3.5
592
4.0
1.9
1120
477
57.7
2.7
30.3
655
720
96
<LOD
288
39
nm
<LOD
0.81
1.9
8
-
FU3-PL-11-TiD3
Fatu Kapa
I
d
e
f
X
Translucent smoker
1573
259
258
4.9
1.025
41
3.7
637
1.4
8.3
1142
509
49.8
15.5
35.0
541
612
78
<LOD
38
26
nm
<LOD
0.80
1.8
10
-
FU3-PL-11-TiG3
Fatu Kapa
I
d
e
f
X
Translucent smoker
1573
259
258
4.43
1.025
43
3.9
664
4.1
1.9
1268
518
63.5
2.0
44.7
733
802
110
160
nm
46
nm
2.5
0.78
1.9
8
1.848
FU3-PL-14-TiD1
Fatu Kapa
I
d
e
f
X
Translucent smoker
1572
271
271
3.73
1.025
43
3.9
665
4.2
1.1
1282
519
66.2
0.8
43.4
764
823
120
144
28
64
nm
3.4
0.78
1.9
8
1.078
FU3-PL-14-TiG1
Fatu Kapa
I
d
e
f
X
Translucent smoker
1572
271
271
3.97
1.025
42
3.9
661
4.1
0.8
1279
515
65.7
0.8
42.9
757
825
119
<LOD
nm
62
nm
<LOD
0.78
1.9
8
-
FU3-PL-14-TiD2
Fatu Kapa
O
b
e
l
X
Translucent smoker
1669
272
-
4.59
1.03
49
4.5
769
4.5
0.7
1506
577
69.4
1.3
65.5
757
nm
nm
nm
nm
nm
nm
nm
0.75
2.0
8
-
FU3-PL-14-TiD3
Fatu Kapa
O
b
e
l
X
Translucent smoker
1636
287
-
4.28
1.03
47
4.3
729
3.7
15.0
1283
557
58.8
11.1
65.0
621
nm
nm
nm
nm
nm
nm
nm
0.76
1.8
9
-
FU3-PL-14-TiG3
Fatu Kapa
O
b
e
l
X
Translucent smoker
1636
287
-
5.37
1.028
43
3.9
672
2.5
27.0
1103
528
42.5
25.3
54.6
415
nm
nm
nm
nm
nm
nm
nm
0.79
1.6
12
-
FU3-PL-18-TiD1
Fatu Kapa
A
s
t
e
r
X
Translucent smoker
1540
265
260
4.35
1.027
44
4.1
693
3.7
1.0
1344
533
64.9
1.2
51.1
755
nm
nm
nm
nm
nm
nm
nm
0.77
1.9
8
-
FU3-PL-17-TiD2
Fatu Kapa
Fati Ufu
Grey smoker
1522
299
303
4.26
1.031
47
4.3
739
3.3
9.3
1378
555
38.4
17.6
66.6
543
nm
nm
nm
nm
nm
nm
nm
0.75
1.9
14
-
FU3-PL-17-TiG2
Fatu Kapa
Fati Ufu
Grey smoker
1522
299
303
4.22
1.031
48
4.4
748
3.5
8.7
1402
562
39.8
15.9
69.7
569
nm
nm
nm
nm
nm
nm
nm
0.75
1.9
14
-
FU3-PL-21-TiD1
Fatu Kapa
Fati Ufu
Grey smoker
1523
302
301
3.81
1.032
50
4.6
784
4.7
1.4
1554
577
47.3
1.4
86.2
717
nm
nm
nm
nm
nm
nm
nm
0.74
2.0
12
-
FU3-PL-21-TiG1
Fatu Kapa
Fati Ufu
Grey smoker
1523
302
301
4.69
1.03
45
4.1
708
2.7
10.5
1292
544
34.7
19.3
60.3
474
nm
nm
nm
nm
nm
nm
nm
0.77
1.8
16
-
FU3-PL-21-TiD2
Fatu Kapa
Fati Ufu
White smoker
1503
-
284
3.27
1.028
44
4.1
694
4.9
0.4
1359
534
39.3
1.0
63.3
573
nm
nm
nm
nm
nm
nm
nm
0.77
2.0
14
-
FU3-PL-21-TiG2
Fatu Kapa
Fati Ufu
White smoker
1503
-
284
4.22
1.026
42
3.9
661
3.9
7.0
1217
520
32.0
13.3
50.6
435
nm
nm
nm
nm
nm
nm
nm
0.79
1.8
16
-
FU3-PL-20-TiD1
Fatu Kapa
Tutafi
Grey smoker
1580
316
317
4.1
1.029
46
4.2
720
2.6
0.6
1409
543
54.6
0.9
65.4
628
nm
nm
nm
nm
nm
nm
nm
0.75
2.0
10
-
FU3-PL-20-TiG1
Fatu Kapa
Tutafi
Grey smoker
1580
316
317
4.14
1.029
46
4.2
723
2.3
1.0
1409
543
54.7
0.7
66.4
630
nm
nm
nm
nm
nm
nm
nm
0.75
1.9
10
-
FU3-PL-21-TiD3
Fatu Kapa
Tutafi
White smoker
1626
293
294
2.92
1.028
45
4.1
701
5.1
0.9
1367
528
51.3
0.3
63.9
640
nm
nm
nm
nm
nm
nm
nm
0.75
1.9
10
-
FU3-PL-21-TiG3
Fatu Kapa
Tutafi
White smoker
1626
293
294
3.65
1.027
45
4.1
700
5.0
0.8
1371
528
51.0
0.8
63.3
633
nm
nm
nm
nm
nm
nm
nm
0.75
2.0
10
-Figure 2
Photographs of sulphide chimneys and young lava flows observed on the floor of the Kulo Lasi caldera. Copyrights from Ifremer, FUTUNA 1 cruise.Figure 3
(a) and (b) Photographs of anhydrite structures observed at Stéphanie, Carla,I
d
e
f
X, A
s
t
e
r
X, and O
b
e
l
X site. (c) Photographs of grey smokers associated with sulphides structures observed at Fati Ufu and Tutafi. Copyrights from Ifremer, FUTUNA 3 cruise.
(a)
(b)
(c)


### 4.1. Gas

Concentrations of gases in all fluids as well as stable isotopes data are compiled in Table4. Samples recovered from Kulo Lasi were extremely poor in CH4 (<0.01 mM) but contained the series of C2–C5 hydrocarbons. Samples from Fatu Kapa had higher concentration of CH4 (0.05–0.235 mM) but only n-pentane (0.5–3.2 μM) could be detected and quantified in terms of longer hydrocarbons. One sample from Kulo Lasi was found to be extremely rich in H2 with nearly 20 mM while the others ranged from 1 to 6 mM and were below 0.05 mM at Fatu Kapa. H2S was highly variable between the 3 sampled chimneys at Kulo Lasi (0.39, 1.66, and 5.05 mM) while it was found rather homogeneous at Fatu Kapa with values around 1 mM. CO2 concentrations were more elevated at Fatu Kapa (4.5–29 mM) compared to Kulo Lasi (1–5 mM).Table 4
Measured gas concentration and associated stable isotopic ratios hydrothermal fluids from the Kulo Lasi and Fatu Kapa vent fields. Values of logfH2 were calculated using SUPCRT92 with the slop98 data base.
Sample name
Site
H2S
N2
3He
R/Ra
H2
logfH2
CH4
CO2
C2H6
C2H4
C3H8
C3H6
n-C4H10
n-C5H12
δD (H2)
δD (CH4)
δ
13C (CO2)
δ
13C (CH4)
δ
13C (C2H6)
δ
13C (C3H8)
δ
13C (C4H10)
mM
mM
mM
mM
mM
mM
µM
µM
µM
µM
µM
µM
‰
‰
‰
‰
‰
‰
‰
Seawater
0.59
nm
nm
<LOD
-
<LOD
2.3
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
FU-PL-05-TiG1
Kulo Lasi
0.12
nm
nm
<LOQ
-
0.001
2.6
<LOD
nm
<LOD
nm
<LOD
<LOD
nm
nm
nm
nm
nm
nm
nm
FU-PL-06-TiD4
Kulo Lasi
1.66
0.10
nm
nm
1.14
-
0.001
1.3
0.02
0.005
0.006
0.004
0.005
0.005
−323
n.m.
−3.2
−29
−27
−26
nm
FU-PL-06-TiG3
Kulo Lasi
5.05
1.43
nm
nm
19.8
−3.11
0.006
5.1
0.11
0.042
0.028
0.030
0.024
0.006
−306
n.m.
−4.1
−23
−26
−26
−24
FU-PL-06-TiD1
Kulo Lasi
0.39
2.48
nm
nm
6.18
−3.62
0.004
3.0
0.1
0.017
0.017
0.020
0.012
0.004
−300
n.m.
−1.9
−28
−24
−26
−24
FU-PL-06-TiG1
Kulo Lasi
0.79
nm
nm
1.04
−4.40
0.001
1.0
0.02
0.009
0.005
0.007
0.005
0.001
−316
n.m.
−0.2
−27.2
−22
−26
−24
FU3-PL-04-TiG3
Stéphanie
0.91
0.93
1.1
E
-
08
8.6
0.03
−1.87
0.114
15.5
<LOD
<LOD
<LOD
<LOD
<LOD
1.7
nm
nm
nm
nm
nm
nm
nm
FU3-PL-08-TiD1
Stéphanie
1.23
1.98
nm
0.06
−1.57
0.235
29.0
<LOD
<LOD
<LOD
<LOD
<LOD
3.2
−676
−108
−5
−21.7
nm
nm
nm
FU3-PL-08-TiG1
Stéphanie
0.98
2.47
4.4
E
-
09
7.6
0.05
−1.65
0.205
25.7
<LOD
<LOD
<LOD
<LOD
<LOD
2.9
nm
nm
nm
nm
nm
nm
nm
FU3-PL-09-TiD2
Stéphanie
0.23
0.48
1.9
E
-
09
7.0
0.04
−1.75
0.059
6.0
<LOD
<LOD
<LOD
<LOD
<LOD
0.7
−436
−111
−5.3
−22.2
nm
nm
nm
FU3-PL-06-TiD1
Carla
1.34
0.50
7.1
E
-
09
9.6
0.01
−2.35
0.021
4.5
<LOD
<LOD
<LOD
<LOD
<LOD
0.5
nm
nm
nm
nm
nm
nm
nm
FU3-PL-08-TiD3
Carla
0.19
3.33
1.7
E
-
08
9.8
0.05
−1.65
0.066
11.9
<LOD
<LOD
<LOD
<LOD
<LOD
1.5
−410
−109
−4.7
−21.5
nm
nm
nm
FU3-PL-11-TiG3
I
d
e
f
X
1.13
0.78
1.8
E
-
08
9.8
0.03
−1.87
0.085
10.0
<LOD
<LOD
<LOD
<LOD
<LOD
1.1
nm
nm
nm
nm
nm
nm
nm
FU3-PL-14-TiD1
I
d
e
f
X
1.00
1.20
5.5
E
-
09
8.7
0.02
−2.05
0.069
10.1
<LOD
<LOD
<LOD
<LOD
<LOD
1.1
−417
−110
−4.9
−23.8
nm
nm
nm
FU3-PL-14-TiD2
O
b
e
l
X
0.85
1.05
3.8
E
-
08
9.8
0.03
−1.87
0.110
8.7
<LOD
<LOD
<LOD
<LOD
<LOD
1.0
−407
−113
−5
−24
nm
nm
nm
FU3-PL-14-TiD3
O
b
e
l
X
0.54
0.93
5.2
E
-
09
8.4
0.02
−2.05
0.165
9.2
<LOD
<LOD
<LOD
<LOD
<LOD
1.0
nm
nm
nm
nm
nm
nm
nm
FU3-PL-18-TiD1
A
s
t
e
r
X
0.98
0.89
nm
nm
0.01
−2.35
0.067
9.2
<LOD
<LOD
<LOD
<LOD
<LOD
1.0
−412
−111
−4.9
−23.6
nm
nm
nm
FU3-PL-17-TiG2
Fati Ufu
1.76
0.84
2.7
E
-
08
9.9
0.01
−2.59
0.070
21.5
<LOD
<LOD
<LOD
<LOD
<LOD
2.3
-
−93
−2.3
−6.1
nm
nm
nm
FU3-PL-21-TiD2
Fati Ufu
0.71
2.07
3.1
E
-
09
9.9
0.03
−2.11
0.111
12.6
<LOD
<LOD
<LOD
<LOD
<LOD
1.5
−410
−109
−4.4
−23.3
nm
nm
nm
FU3-PL-20-TiD1
Tutafi
2.36
1.18
1.4
E
-
08
9.2
0.05
−1.89
0.156
22.2
<LOD
<LOD
<LOD
<LOD
<LOD
2.4
−396
−111
−4.5
−23.6
nm
nm
nm
FU3-PL-21-TiD3
Tutafi
0.84
1.67
nm
nm
0.03
−2.11
0.053
11.7
<LOD
<LOD
<LOD
<LOD
<LOD
1.4
−415
−109
−4.7
−24.2
nm
nm
nmHelium isotope ratios were in the range 7.0–9.9 Ra over the Fatu Kapa area, in agreement with plume data [7]. They could not be measured at Kulo Lasi unfortunately. Carbon isotopes ratios were around −5‰ for CO2 at Fatu Kapa whereas at Kulo Lasi the ratio showed very different results ranging from −0.2 to −4.1‰. As for methane, δ
13C were slightly lower at Kulo Lasi (~−28‰) versus Fatu Kapa (~−23‰) and δD was about −110‰ in all samples from Fatu Kapa. δD (CH4) could not be measured in the Kulo Lasi fluids because of the too low concentrations of CH4. Carbon isotope ratios of longer hydrocarbons were in the −27 to −22‰ at both vent fields. To be noted one sample from Fati Ufu in the Fatu Kapa area showed remarkably lower isotopic ratios with δ
13C (CO2) = −2.3‰, δ
13C (CH4) = −6.1‰ and δD (CH4) = −93‰. We do not have any explanation for this but do not have any reasons either to consider it as an outlier.


### 4.2. Major and Minor Elements

Major and minor elements measurements data are compiled in Table3. Fluids from Fatu Kapa all exhibited a higher salinity than seawater up to 4.6 wt% NaCl whereas at Kulo Lasi fluids with both lower (2.8 wt% NaCl) and higher (4.3 wt% NaCl) salinity were sampled. Mg and SO4 concentrations tend to be zero in the purest samples at Fatu Kapa. But, the purest fluids from Kulo Lasi showed significant levels of Mg and SO4, associated with an extremely acidic pH (<2.5) and a high T (343°C). Although we cannot totally discard that some mixing with seawater occurred, endmember concentrations of the Kulo Lasi fluids were then estimated to be close to the purest fluids sampled whereas they were obtained from mixing lines at Fatu Kapa assuming Mg zero (Table 5).Table 5
Endmember compositions in fluids from the Kulo Lasi and Fatu Kapa vent fields. Kulo Lasi endmembers cannot be extrapolated at Mg = 0. Values presented here for both brine and condensed vapour phases correspond to concentrations in the fluid with the lowest Mg. Elemental compositions in endmember fluids from the various sites of the Fatu Kapa vent field were calculated using the mixing lines (FigureS1) and assuming Mg = 0. Values of the purest fluid were used when linear regression was not possible (∗). Note that only one sample was available for the A
s
t
e
r
X site (
1
).
Zone
Site
Depth
T
pH
NaCl
Cl
Si
SO4
Br
Na
K
Mg
Ca
Li
Rb
Sr
Fe
Mn
Cu
Zn
Na/Cl
Br/Cl
Na/K
CH4/Mn
°C
(wt%)
mM
mM
mM
µM
mM
mM
mM
mM
µM
µM
µM
µM
µM
µM
µM
×103
Kulo Lasi
NaCl poor
1475
345
2.24
2.9
497
8.2
8.8
738
388
18.5
24.6
11.6
149
26
7.3
4796
862
14
45
0.78
1.48
21
0.007∗
Kulo Lasi
NaCl rich
1475
345
2.36
4.3
735
14.6
6.2
1135
612
29.5
26.5
10.9
238
46
3.4
9884
1416
2.5
175
0.83
1.54
21
0.001∗
Fatu Kapa
Stéphanie
1555
280
3.4
4.5
767
4.7∗
0.0
1569
532
54.5
0.0
98.9
708
114
282∗
655∗
268
6.6∗
<LOD
0.69
2.05
10
0.76∗
Fatu Kapa
Carla
1664
280
2.8
3.5
594
4.3
0.0
1132
477
59.9
0.0
31.4
691
105
114∗
287∗
53
nm
4.4∗
0.80
1.90
8
1.37∗
Fatu Kapa
I
d
e
f
X
1572
270
3.7
3.9
665
4.2∗
0.0
1282
518
66.4
0.0
44.3
751
113
160∗
28∗
60
nm
3.4∗
0.78
1.93
8
1.08∗
Fatu Kapa
O
b
e
l
X
1669
270
4.6
4.5
771
4.6
0.0
1458
580
71.0
0.0
85.9
777
nm
nm
nm
nm
nm
nm
0.75
1.89
8
-
Fatu Kapa
A
s
t
e
r
X
(
1
)
1540
265
4.4
4.1
693
3.7
1.0
1344
533
64.9
1.2
51.1
755
nm
nm
nm
nm
nm
nm
0.77
1.94
8
-
Fatu Kapa
Fati Ufu
1523
300
3.8
4.6
790
4.9
0.0
1589
580
48.2
0.0
85.4
722
nm
nm
nm
nm
nm
nm
0.73
2.01
12
-
Fatu Kapa
Fati Ufu
1503
280
3.3
4.1
700
4.9
0.0
1380
538
40.0
0.0
65.0
583
nm
nm
nm
nm
nm
nm
0.77
1.97
13
-
Fatu Kapa
Tutafi
1580
315
4.1
4.2
713
5.1
0.0
1405
535
52.9
0.0
65.1
635
nm
nm
nm
nm
nm
nm
0.75
1.97
10
-
IAPSO
Standard sw
-
-
-
3.2
546
0.0
28.2
839
468
10.2
53.2
10.3
27
1.3
90
<LOD
<LOD
<LOD
<LOD
0.9
1.5
46
-
Kulo Lasi
Reference sw
1150
-
-
3.2
551
0.1
29.0
833
457
9.8
53.2
10.6
25
4.4
93
<LOD
<LOD
<LOD
<LOD
0.83
1.5
47
-
Fatu Kapa
Reference sw
1488
-
-
3.3
565
0.0
28.8
841
483
10.4
54.5
10.7
22
5.8
<LOD
<LOD
<LOD
<LOD
<LOD
0.85
1.5
46
-
Fatu Kapa
Reference sw
1572
2
-
3.3
557
0.0
28.7
841
477
10.4
54.2
10.8
23
nm
nm
nm
nm
nm
nm
0.86
1.5
46
-
∗Maximum value when linear regression was not possible; (
1
) only one sample.Fluids from Fatu Kapa were enriched compared to seawater in alkali, alkaline Earth, and transition metals as well as in strontium, bromide, and silica. Conversely, the fluids from Kulo Lasi exhibited a much more complex pattern. They were all highly enriched in transition metals and silica compared to seawater and fluids from Fatu Kapa (e.g., Fe up to ~10 mM). The enrichment versus seawater in alkali metals was not as striking as for Fatu Kapa fluids. As for the alkaline Earth metals, the amount of Ca was identical to seawater and fluids were depleted in Sr compared to seawater. Finally, both depletion and enrichment in Br were observed in the fluids from Kulo Lasi.


### 4.3. Organic Geochemistry

First of all, we would like to mention that because solubility of organic compounds decreases withT and because samples were processed at room temperature, the measured concentrations are probably lower than in situ concentrations. Moreover, it is very likely that a portion of the OM was adsorbed on small particles in the fluids which are not taken into account using our extraction and analytical techniques. As a result, the concentrations we report here probably represent lower estimates of in situ concentrations. However, since in situ measurement techniques are not available yet, these values are the best estimates we can obtain. Note that they also are the first to be published for SVOCs.Formate and acetate reached 16.3 and 15.5μM, respectively, and covaried with Mg in the Kulo Lasi fluids (Figure 4). Concentrations of formate and acetate were significantly higher in the Fatu Kapa area but no correlation with Mg could be observed. Nevertheless, the purest fluids usually showed the highest concentrations. Formate reached 68 ppb at Stéphanie and 722 ppb at Fati Ufu whereas it could not be detected at I
d
e
f
X and Tutafi and was not measured at Carla. Acetate was detected in all analysed samples and concentrations were an order of magnitude higher than the ones of formate (543–2309 ppb) (Table 6).Table 6
Measured concentration of Total Organic Carbon (TOC), formate, acetate, and a selection of individual semi-volatile organic compounds extracted from hydrothermal fluids of the Kulo Lasi and Fatu Kapa vent fields.
Compound
Rtmin
Units
BlankDry
BlankMQ
FU3-PL-14-TiG2deepsea water
FU3-PL-08-TiD2Stéphanie
FU3-PL-04-TiD3Stéphanie
FU3-PL-09-TiG2Stéphanie
FU3-PL-08-TiG3Carla
FU3-PL-06-TiG1Carla
FU3-PL-14-TiG1Idefix
FU3-PL-11-TiD3Idefix
FU3-PL-21-TiG2Fati Ufu
FU3-PL-17-TiD2Fati Ufu
FU3-PL-21-TiG1Fati Ufu
FU3-PL-21-TiG3Tutafi
FU3-PL-20-TiG1Tutafi
pH
-
-
-
-
3.83
4.65
5.42
4.17
4.91
3.97
4.9
4.22
4.26
4.69
3.65
4.14
Mg
-
mM
-
-
54.2
0.6
18.7
44.3
2.7
23.6
0.8
15.5
13.3
17.6
19.3
0.8
0.7
TOC
-
ppm
na
<0.005
na
0.165
na
na
na
na
0.498
na
na
6.514
na
0.304
na
Formate
-
ppb
na
nd
na
65.8
<LOQ
na
na
na
<LOQ
<LOQ
111.7
721.6
na
<LOQ
na
Acetate
-
ppb
na
nd
na
1155.1
543.2
na
na
na
1033.6
995.1
1740.9
2308.8
na
1067.3
na
Nonane
4.68
ppb
nd
nd
0.85 ± 0.51
1.59 ± 0.52
1.17 ± 0.51
1.08 ± 0.51
0.72 ± 0.51
0.58 ± 0.51
0.84 ± 0.51
0.52 ± 0.50
0.64 ± 0.50
0.50 ± 0.51
0.28 ± 0.51
1.52 ± 0.52
2.29 ± 0.54
Decane
5.911
ppb
nd
<0.03
2.21 ± 0.44
2.03 ± 0.44
2.02 ± 0.44
2.10 ± 0.44
3.05 ± 0.45
1.63 ± 0.44
6.92 ± 0.51
2.20 ± 0.44
6.47 ± 0.50
5.58 ± 0.48
2.88 ± 0.45
9.18 ± 0.56
22.16 ± 0.95
Undecane
7.183
ppb
nd
<0.2
11.35 ± 0.97
6.79 ± 0.76
9.52 ± 0.87
11.48 ± 0.98
13.81 ± 1.14
9.61 ± 0.87
23.13 ± 1.88
10.89 ± 0.94
19.13 ± 1.55
26.06 ± 2.14
12.26 ± 1.03
20.48 ± 1.66
26.93 ± 2.21
Dodecane
8.394
ppb
nd
nd
3.36 ± 0.65
1.33 ± 0.57
2.30 ± 0.60
2.98 ± 0.63
3.35 ± 0.65
2.64 ± 0.61
5.12 ± 0.76
3.35 ± 0.65
4.76 ± 0.73
6.52 ± 0.86
3.30 ± 0.65
4.00 ± 0.69
5.14 ± 0.76
Tridecane
9.549
ppb
nd
nd
1.39 ± 0.54
0.35 ± 0.53
0.73 ± 0.53
0.86 ± 0.53
1.37 ± 0.54
1.39 ± 0.54
1.63 ± 0.55
2.21 ± 0.57
1.75 ± 0.55
3.89 ± 0.65
2.27 ± 0.57
1.06 ± 0.54
1.42 ± 0.54
Tetradecane
10.641
ppb
nd
nd
0.53 ± 0.47
0.56 ± 0.47
0.57 ± 0.47
0.59 ± 0.47
0.67 ± 0.46
0.66 ± 0.46
0.59 ± 0.47
0.72 ± 0.46
0.69 ± 0.46
0.64 ± 0.46
0.72 ± 0.46
0.72 ± 0.46
0.70 ± 0.46
Pentadecane
11.675
ppb
nd
nd
0.44 ± 0.28
0.40 ± 0.28
0.48 ± 0.27
0.44 ± 0.28
0.52 ± 0.27
0.59 ± 0.27
0.43 ± 0.28
0.60 ± 0.27
0.57 ± 0.27
0.47 ± 0.28
0.49 ± 0.27
0.62 ± 0.27
0.58 ± 0.27
Hexadecane
12.65
ppb
nd
nd
0.25 ± 0.73
0.40 ± 0.74
0.42 ± 0.73
0.49 ± 0.73
0.64 ± 0.73
0.59 ± 0.74
0.26 ± 0.73
0.84 ± 0.74
0.53 ± 0.73
0.39 ± 0.73
0.37 ± 0.73
0.65 ± 0.74
0.48 ± 0.73
Heptadecane
13.576
ppb
nd
nd
0.57 ± 0.32
1.08 ± 0.32
0.61 ± 0.32
0.87 ± 0.32
1.13 ± 0.33
0.85 ± 0.32
1.20 ± 0.33
1.48 ± 0.33
0.85 ± 0.32
0.67 ± 0.32
0.78 ± 0.32
1.10 ± 0.33
0.98 ± 0.32
Octadecane
14.452
ppb
nd
nd
0.17 ± 0.17
0.30 ± 0.18
0.28 ± 0.18
0.30 ± 0.18
0.35 ± 0.18
0.33 ± 0.18
0.39 ± 0.18
0.42 ± 0.18
0.49 ± 0.19
0.29 ± 0.18
0.25 ± 0.18
0.47 ± 0.18
0.50 ± 0.19
Nonadecane
15.295
ppb
nd
nd
1.08 ± 1.34
1.36 ± 1.35
1.24 ± 1.35
1.38 ± 1.34
1.64 ± 1.36
1.40 ± 1.36
1.33 ± 1.35
1.83 ± 1.38
1.26 ± 1.33
0.86 ± 1.33
1.02 ± 1.34
1.10 ± 1.33
1.36 ± 1.35
Eicosane
16.104
ppb
nd
nd
1.09 ± 1.23
1.75 ± 1.27
1.05 ± 1.25
0.94 ± 1.23
1.13 ± 1.24
1.69 ± 1.27
1.03 ± 1.24
1.46 ± 1.26
1.00 ± 1.23
0.71 ± 1.24
1.19 ± 1.24
1.25 ± 1.24
1.50 ± 1.26
Nonanoic acid
6.914
ppb
nd
nd
3.72 ± 2.53
8.07 ± 2.96
<0.37
5.71 ± 2.67
4.49 ± 2.56
3.49 ± 2.50
4.91 ± 2.60
7.12 ± 2.87
8.94 ± 3.09
9.23 ± 3.10
na
2.86 ± 2.45
9.90 ± 3.21
Decanoic acid
7.542
ppb
nd
nd
1.17 ± 1.65
0.86 ± 1.59
nd
0.53 ± 1.60
0.41 ± 1.65
nd
0.61 ± 1.62
nd
0.84 ± 1.67
0.56 ± 1.68
na
1.09 ± 1.64
0.83 ± 1.66
Undecanoic acid
8.178
ppb
nd
nd
0.18 ± 0.19
0.29 ± 0.20
nd
0.23 ± 0.19
0.25 ± 0.20
0.28 ± 0.19
0.22 ± 0.20
nd
0.26 ± 0.19
0.34 ± 0.19
na
0.35 ± 0.20
0.33 ± 0.19
Dodecanoic acid
8.773
ppb
nd
nd
0.42 ± 0.48
2.10 ± 0.51
0.55 ± 0.48
0.55 ± 0.48
0.78 ± 0.48
0.49 ± 0.47
2.01 ± 0.51
0.69 ± 0.48
1.29 ± 0.49
1.08 ± 0.49
na
1.45 ± 0.49
0.61 ± 0.48
Tridecanoic acid
9.31
ppb
nd
nd
0.28 ± 0.20
0.35 ± 0.19
0.23 ± 0.21
0.24 ± 0.21
0.24 ± 0.20
0.33 ± 0.20
0.27 ± 0.20
0.25 ± 0.21
0.26 ± 0.21
0.32 ± 0.20
na
0.31 ± 0.19
0.27 ± 0.20
Tetradecanoic acid
9.859
ppb
nd
<0.06
0.94 ± 0.32
1.86 ± 0.31
1.44 ± 0.31
0.87 ± 0.33
0.92 ± 0.32
4.28 ± 0.35
1.41 ± 0.31
2.74 ± 0.31
0.90 ± 0.32
1.15 ± 0.32
na
1.42 ± 0.31
1.07 ± 0.32
Pentadecanoic acid
10.355
ppb
nd
nd
0.54 ± 0.30
1.44 ± 0.30
0.82 ± 0.28
0.46 ± 0.30
0.76 ± 0.29
0.57 ± 0.29
1.06 ± 0.29
0.58 ± 0.30
0.52 ± 0.30
0.78 ± 0.29
na
1.02 ± 0.29
0.77 ± 0.29
Hexadecanoic acid
10.902
ppb
nd
nd
1.46 ± 1.20
6.66 ± 1.37
4.47 ± 1.27
1.78 ± 1.20
3.90 ± 1.25
2.91 ± 1.23
7.30 ± 1.41
3.61 ± 1.24
3.24 ± 1.23
4.92 ± 1.29
na
6.09 ± 1.34
5.59 ± 1.32
Heptadecanoic acid
11.317
ppb
nd
nd
0.54 ± 0.61
3.23 ± 0.58
nd
0.89 ± 0.53
2.04 ± 0.54
1.82 ± 0.54
1.04 ± 0.62
1.62 ± 0.55
<0.03
2.89 ± 0.59
na
2.87 ± 0.59
2.79 ± 0.57
Octadecanoic acid
11.78
ppb
nd
nd
0.94 ± 2.16
8.70 ± 2.82
6.32 ± 2.55
1.67 ± 2.32
6.36 ± 2.48
3.49 ± 2.30
11.83 ± 3.29
5.15 ± 2.35
2.64 ± 2.09
5.26 ± 2.40
na
9.19 ± 2.86
9.66 ± 2.96
Ethyl, Benzene
4.344
ppb
nd
<0.1
nd
<0.1
<0.1
nd
nd
<0.1
<0.1
na
0.10 ± 0.35
<0.1
<0.1
nd
0.44 ± 0.23
p-,m-Xylene
4.443
ppb
nd
nd
0.03 ± 0.05
0.10 ± 0.05
0.11 ± 0.05
0.08 ± 0.05
0.10 ± 0.05
0.11 ± 0.05
0.18 ± 0.05
na
0.33 ± 0.05
0.21 ± 0.05
0.15 ± 0.05
0.11 ± 0.05
0.71 ± 0.08
o-Xylene
4.708
ppb
nd
<0.02
0.02 ± 0.05
0.07 ± 0.06
0.06 ± 0.05
0.02 ± 0.06
0.03 ± 0.08
0.06 ± 0.05
0.14 ± 0.06
na
0.33 ± 0.07
0.19 ± 0.06
0.13 ± 0.06
0.06 ± 0.05
0.68 ± 0.09
Styrene
4.831
ppb
nd
nd
0.59 ± 0.14
0.22 ± 0.16
nd
nd
0.46 ± 0.14
nd
0.29 ± 0.15
na
0.21 ± 0.15
0.20 ± 0.15
0.24 ± 0.14
0.37 ± 0.14
0.20 ± 0.14
isopropyl, Benzene
5.006
ppb
nd
nd
0.04 ± 0.05
0.06 ± 0.05
0.07 ± 0.05
0.07 ± 0.05
0.06 ± 0.05
0.08 ± 0.05
0.09 ± 0.05
na
0.09 ± 0.05
0.04 ± 0.06
0.05 ± 0.05
0.09 ± 0.05
0.09 ± 0.05
n-Propyl, Benzene
5.468
ppb
nd
nd
0.03 ± 0.04
0.02 ± 0.04
0.03 ± 0.04
0.02 ± 0.04
0.03 ± 0.04
0.03 ± 0.04
0.03 ± 0.04
na
0.04 ± 0.04
0.03 ± 0.04
0.03 ± 0.05
0.03 ± 0.04
0.04 ± 0.04
1,2,4-triMethyl-Benzene
5.572
ppb
nd
nd
0.03 ± 0.04
0.05 ± 0.04
0.06 ± 0.04
0.04 ± 0.04
0.06 ± 0.05
0.06 ± 0.04
0.04 ± 0.05
na
0.08 ± 0.04
0.07 ± 0.05
0.07 ± 0.04
0.08 ± 0.04
0.07 ± 0.04
1,3,5-triMethyl-Benzene
5.95
ppb
nd
nd
0.02 ± 0.06
0.11 ± 0.07
0.08 ± 0.07
0.06 ± 0.06
0.09 ± 0.06
0.09 ± 0.06
0.11 ± 0.06
na
0.30 ± 0.07
0.25 ± 0.06
0.20 ± 0.07
0.13 ± 0.06
0.19 ± 0.06
sec-Butyl-Benzene
6.106
ppb
nd
nd
0.27 ± 0.05
0.04 ± 0.04
nd
0.04 ± 0.05
0.05 ± 0.06
0.05 ± 0.05
0.06 ± 0.05
na
nd
0.05 ± 0.05
nd
nd
0.07 ± 0.05
2,isopropyl, Toluene
6.305
ppb
nd
nd
0.07 ± 0.03
0.03 ± 0.03
0.03 ± 0.03
0.03 ± 0.03
0.05 ± 0.03
0.03 ± 0.03
0.04 ± 0.03
na
0.04 ± 0.03
0.04 ± 0.03
0.03 ± 0.03
0.05 ± 0.03
0.07 ± 0.03
n-Butyl, Benzene
6.66
ppb
nd
<0.08
0.06 ± 0.03
0.01 ± 0.03
0.01 ± 0.02
0.01 ± 0.03
0.02 ± 0.03
0.01 ± 0.02
0.02 ± 0.02
na
0.02 ± 0.03
0.02 ± 0.02
nd
0.03 ± 0.03
0.03 ± 0.03
Naphthalene
8.351
ppb
nd
<0.01
1.39 ± 0.07
0.49 ± 0.05
0.32 ± 0.05
0.13 ± 0.04
1.24 ± 0.07
0.69 ± 0.05
1.08 ± 0.06
na
0.90 ± 0.06
0.64 ± 0.05
1.99 ± 0.09
1.19 ± 0.06
1.19 ± 0.06
Acenaphthene
11.796
ppb
nd
nd
<0.009
<0.009
<0.009
<0.009
<0.009
<0.009
<0.009
na
<0.009
<0.009
<0.009
<0.009
<0.009
Fluorene
12.778
ppb
nd
nd
nd
0.05 ± 0.03
<0.01
<0.01
0.14 ± 0.03
0.10 ± 0.03
0.16 ± 0.03
na
0.14 ± 0.03
0.09 ± 0.03
0.06 ± 0.03
0.09 ± 0.03
0.07 ± 0.03
Phenanthrene
14.582
ppb
nd
nd
0.02 ± 0.04
0.10 ± 0.04
0.06 ± 0.04
0.06 ± 0.04
0.29 ± 0.05
0.13 ± 0.04
0.20 ± 0.05
na
0.16 ± 0.05
0.10 ± 0.04
0.06 ± 0.04
0.23 ± 0.05
0.17 ± 0.05
Anthracene
14.788
ppb
nd
nd
nd
nd
nd
nd
nd
nd
nd
na
nd
nd
nd
nd
nd
Fluoranthene
17.117
ppb
nd
nd
<0.04
<0.04
<0.04
<0.04
0.06 ± 0.16
<0.04
<0.04
na
0.04 ± 0.16
<0.04
<0.04
0.05 ± 0.16
<0.04
Pyrene
17.52
ppb
nd
nd
<0.03
0.03 ± 0.11
0.03 ± 0.10
<0.03
0.14 ± 0.11
0.07 ± 0.10
0.10 ± 0.11
na
0.06 ± 0.10
0.05 ± 0.11
0.03 ± 0.10
0.09 ± 0.10
0.06 ± 0.10Figure 4
Mixing lines of formate and acetate versus Mg for the Kulo Lasi fluids. Note that the reference deep-sea water sample (FU-PL05-TiG2 noted as SW here) was taken at 1150 m depth above the southern wall of the caldera (see Figure1 for location and Table 3) and thus very likely within the plume [7]. This would account for the unusual concentrations of formate and acetate detected.Heavier extractable organic compounds were not detected in the dry control experiment and only a few were detectable but below limit of quantification (LOQ) in the MQ water blank experiment (Table6). This showed that sample preparation and storage could be considered as contamination-free steps. The levels of heavier extractable organic compounds appeared rather high in the reference water at Fatu Kapa certainly because of the overall spread hydrothermal discharges and diffuse venting in the region [7] (Table 6, Figure 5). This sample was indeed taken mid-way between O
b
e
l
X and A
s
t
e
r
X fields at about 20 m above the seafloor. As a consequence, it is difficult to assess possible contamination originating from sampling device or seawater contribution in the present case. However, earlier studies have shown that they generally did not represent major sources of contamination as for the studied compounds [27, 37]. Nevertheless, in comparison to deep-sea water both the qualitative (Kulo Lasi) and quantitative (Fatu Kapa) data obtained suggested enrichment of the fluids in hydrothermally derived compounds, namely, n-alkanes (C9–C12), n-FAs (C9, C12, C14–C18), and PAHs (fluorene, phenanthrene, pyrene) ([39]; Table 6, Figures 5 and 6). Such enrichment was unclear for >C12  n-alkanes; C10, C11, C13  n-FAs; BTEXs; naphthalene, acenaphthene, and fluoranthene because of their very low concentration and/or the measurement uncertainty.Figure 5
Distribution of n-alkanes, n-fatty acids, mono-, and polyaromatic hydrocarbons (BTEX and PAH) in the purest fluids of the Stéphanie, Carla,I
d
e
f
X, Fati Ufu, and Tutafi sites collected within the Fatu Kapa vent field. Because organic geochemistry does not seem to follow a simple mixing model, endmember concentrations cannot be calculated. To that respect composition of the purest fluids is presented and assumed to be close to endmembers composition. Note that quantitative results are not available for the Kulo Lasi fluids (see Figure 6 for chromatograms).Figure 6
Only qualitative results could be obtained at Kulo Lasi. This figure presents a selection of representative chromatograms obtained for the Kulo Lasi fluid samples. For the sake of clarity, close-ups of a few peaks are shown to illustrate the enrichment of fluids (FU-PL06-TiG1 in red and FU-PL06-TiD3 in green) versus the reference deep-sea water (FU-PL05-TiG2 in blue).Differences in concentrations seemed to exist among the vents over the Fatu Kapa area. Fluids from the Stéphanie vent field had concentrations in hydrocarbons equal or below the reference water sample whereas they were clearly enriched in C9, C12, C14–C18 n-FAs. The Carla fluids were slightly enriched in C9–C12  n-alkanes and showed the highest concentrations in PAHs. Fluids from I
d
e
f
X, Fati Ufu, and Tutafi shared some similarities: a strong enrichment in decane and undecane, alike concentrations in PAHs, and the presence of significant amounts of xylene. However, fluids expelled at the Tutafi vent appeared the most enriched in C9–C11  n-alkanes and xylenes. In terms of fatty acids and considering the analytical error, the 5 vents showed consistent concentrations with C9, C16, and C18 being major. Note that fluids from Fati Ufu seemed depleted in C17 and C18.Generally we did not observe strong linear correlation between the concentration of individual compounds and Mg. Nonetheless, these relations showed that both enrichment and depletion of organic compounds seemed to occur in hydrothermal fluids versus deep-sea water.


## 4.1. Gas

Concentrations of gases in all fluids as well as stable isotopes data are compiled in Table4. Samples recovered from Kulo Lasi were extremely poor in CH4 (<0.01 mM) but contained the series of C2–C5 hydrocarbons. Samples from Fatu Kapa had higher concentration of CH4 (0.05–0.235 mM) but only n-pentane (0.5–3.2 μM) could be detected and quantified in terms of longer hydrocarbons. One sample from Kulo Lasi was found to be extremely rich in H2 with nearly 20 mM while the others ranged from 1 to 6 mM and were below 0.05 mM at Fatu Kapa. H2S was highly variable between the 3 sampled chimneys at Kulo Lasi (0.39, 1.66, and 5.05 mM) while it was found rather homogeneous at Fatu Kapa with values around 1 mM. CO2 concentrations were more elevated at Fatu Kapa (4.5–29 mM) compared to Kulo Lasi (1–5 mM).Table 4
Measured gas concentration and associated stable isotopic ratios hydrothermal fluids from the Kulo Lasi and Fatu Kapa vent fields. Values of logfH2 were calculated using SUPCRT92 with the slop98 data base.
Sample name
Site
H2S
N2
3He
R/Ra
H2
logfH2
CH4
CO2
C2H6
C2H4
C3H8
C3H6
n-C4H10
n-C5H12
δD (H2)
δD (CH4)
δ
13C (CO2)
δ
13C (CH4)
δ
13C (C2H6)
δ
13C (C3H8)
δ
13C (C4H10)
mM
mM
mM
mM
mM
mM
µM
µM
µM
µM
µM
µM
‰
‰
‰
‰
‰
‰
‰
Seawater
0.59
nm
nm
<LOD
-
<LOD
2.3
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
nm
FU-PL-05-TiG1
Kulo Lasi
0.12
nm
nm
<LOQ
-
0.001
2.6
<LOD
nm
<LOD
nm
<LOD
<LOD
nm
nm
nm
nm
nm
nm
nm
FU-PL-06-TiD4
Kulo Lasi
1.66
0.10
nm
nm
1.14
-
0.001
1.3
0.02
0.005
0.006
0.004
0.005
0.005
−323
n.m.
−3.2
−29
−27
−26
nm
FU-PL-06-TiG3
Kulo Lasi
5.05
1.43
nm
nm
19.8
−3.11
0.006
5.1
0.11
0.042
0.028
0.030
0.024
0.006
−306
n.m.
−4.1
−23
−26
−26
−24
FU-PL-06-TiD1
Kulo Lasi
0.39
2.48
nm
nm
6.18
−3.62
0.004
3.0
0.1
0.017
0.017
0.020
0.012
0.004
−300
n.m.
−1.9
−28
−24
−26
−24
FU-PL-06-TiG1
Kulo Lasi
0.79
nm
nm
1.04
−4.40
0.001
1.0
0.02
0.009
0.005
0.007
0.005
0.001
−316
n.m.
−0.2
−27.2
−22
−26
−24
FU3-PL-04-TiG3
Stéphanie
0.91
0.93
1.1
E
-
08
8.6
0.03
−1.87
0.114
15.5
<LOD
<LOD
<LOD
<LOD
<LOD
1.7
nm
nm
nm
nm
nm
nm
nm
FU3-PL-08-TiD1
Stéphanie
1.23
1.98
nm
0.06
−1.57
0.235
29.0
<LOD
<LOD
<LOD
<LOD
<LOD
3.2
−676
−108
−5
−21.7
nm
nm
nm
FU3-PL-08-TiG1
Stéphanie
0.98
2.47
4.4
E
-
09
7.6
0.05
−1.65
0.205
25.7
<LOD
<LOD
<LOD
<LOD
<LOD
2.9
nm
nm
nm
nm
nm
nm
nm
FU3-PL-09-TiD2
Stéphanie
0.23
0.48
1.9
E
-
09
7.0
0.04
−1.75
0.059
6.0
<LOD
<LOD
<LOD
<LOD
<LOD
0.7
−436
−111
−5.3
−22.2
nm
nm
nm
FU3-PL-06-TiD1
Carla
1.34
0.50
7.1
E
-
09
9.6
0.01
−2.35
0.021
4.5
<LOD
<LOD
<LOD
<LOD
<LOD
0.5
nm
nm
nm
nm
nm
nm
nm
FU3-PL-08-TiD3
Carla
0.19
3.33
1.7
E
-
08
9.8
0.05
−1.65
0.066
11.9
<LOD
<LOD
<LOD
<LOD
<LOD
1.5
−410
−109
−4.7
−21.5
nm
nm
nm
FU3-PL-11-TiG3
I
d
e
f
X
1.13
0.78
1.8
E
-
08
9.8
0.03
−1.87
0.085
10.0
<LOD
<LOD
<LOD
<LOD
<LOD
1.1
nm
nm
nm
nm
nm
nm
nm
FU3-PL-14-TiD1
I
d
e
f
X
1.00
1.20
5.5
E
-
09
8.7
0.02
−2.05
0.069
10.1
<LOD
<LOD
<LOD
<LOD
<LOD
1.1
−417
−110
−4.9
−23.8
nm
nm
nm
FU3-PL-14-TiD2
O
b
e
l
X
0.85
1.05
3.8
E
-
08
9.8
0.03
−1.87
0.110
8.7
<LOD
<LOD
<LOD
<LOD
<LOD
1.0
−407
−113
−5
−24
nm
nm
nm
FU3-PL-14-TiD3
O
b
e
l
X
0.54
0.93
5.2
E
-
09
8.4
0.02
−2.05
0.165
9.2
<LOD
<LOD
<LOD
<LOD
<LOD
1.0
nm
nm
nm
nm
nm
nm
nm
FU3-PL-18-TiD1
A
s
t
e
r
X
0.98
0.89
nm
nm
0.01
−2.35
0.067
9.2
<LOD
<LOD
<LOD
<LOD
<LOD
1.0
−412
−111
−4.9
−23.6
nm
nm
nm
FU3-PL-17-TiG2
Fati Ufu
1.76
0.84
2.7
E
-
08
9.9
0.01
−2.59
0.070
21.5
<LOD
<LOD
<LOD
<LOD
<LOD
2.3
-
−93
−2.3
−6.1
nm
nm
nm
FU3-PL-21-TiD2
Fati Ufu
0.71
2.07
3.1
E
-
09
9.9
0.03
−2.11
0.111
12.6
<LOD
<LOD
<LOD
<LOD
<LOD
1.5
−410
−109
−4.4
−23.3
nm
nm
nm
FU3-PL-20-TiD1
Tutafi
2.36
1.18
1.4
E
-
08
9.2
0.05
−1.89
0.156
22.2
<LOD
<LOD
<LOD
<LOD
<LOD
2.4
−396
−111
−4.5
−23.6
nm
nm
nm
FU3-PL-21-TiD3
Tutafi
0.84
1.67
nm
nm
0.03
−2.11
0.053
11.7
<LOD
<LOD
<LOD
<LOD
<LOD
1.4
−415
−109
−4.7
−24.2
nm
nm
nmHelium isotope ratios were in the range 7.0–9.9 Ra over the Fatu Kapa area, in agreement with plume data [7]. They could not be measured at Kulo Lasi unfortunately. Carbon isotopes ratios were around −5‰ for CO2 at Fatu Kapa whereas at Kulo Lasi the ratio showed very different results ranging from −0.2 to −4.1‰. As for methane, δ
13C were slightly lower at Kulo Lasi (~−28‰) versus Fatu Kapa (~−23‰) and δD was about −110‰ in all samples from Fatu Kapa. δD (CH4) could not be measured in the Kulo Lasi fluids because of the too low concentrations of CH4. Carbon isotope ratios of longer hydrocarbons were in the −27 to −22‰ at both vent fields. To be noted one sample from Fati Ufu in the Fatu Kapa area showed remarkably lower isotopic ratios with δ
13C (CO2) = −2.3‰, δ
13C (CH4) = −6.1‰ and δD (CH4) = −93‰. We do not have any explanation for this but do not have any reasons either to consider it as an outlier.


## 4.2. Major and Minor Elements

Major and minor elements measurements data are compiled in Table3. Fluids from Fatu Kapa all exhibited a higher salinity than seawater up to 4.6 wt% NaCl whereas at Kulo Lasi fluids with both lower (2.8 wt% NaCl) and higher (4.3 wt% NaCl) salinity were sampled. Mg and SO4 concentrations tend to be zero in the purest samples at Fatu Kapa. But, the purest fluids from Kulo Lasi showed significant levels of Mg and SO4, associated with an extremely acidic pH (<2.5) and a high T (343°C). Although we cannot totally discard that some mixing with seawater occurred, endmember concentrations of the Kulo Lasi fluids were then estimated to be close to the purest fluids sampled whereas they were obtained from mixing lines at Fatu Kapa assuming Mg zero (Table 5).Table 5
Endmember compositions in fluids from the Kulo Lasi and Fatu Kapa vent fields. Kulo Lasi endmembers cannot be extrapolated at Mg = 0. Values presented here for both brine and condensed vapour phases correspond to concentrations in the fluid with the lowest Mg. Elemental compositions in endmember fluids from the various sites of the Fatu Kapa vent field were calculated using the mixing lines (FigureS1) and assuming Mg = 0. Values of the purest fluid were used when linear regression was not possible (∗). Note that only one sample was available for the A
s
t
e
r
X site (
1
).
Zone
Site
Depth
T
pH
NaCl
Cl
Si
SO4
Br
Na
K
Mg
Ca
Li
Rb
Sr
Fe
Mn
Cu
Zn
Na/Cl
Br/Cl
Na/K
CH4/Mn
°C
(wt%)
mM
mM
mM
µM
mM
mM
mM
mM
µM
µM
µM
µM
µM
µM
µM
×103
Kulo Lasi
NaCl poor
1475
345
2.24
2.9
497
8.2
8.8
738
388
18.5
24.6
11.6
149
26
7.3
4796
862
14
45
0.78
1.48
21
0.007∗
Kulo Lasi
NaCl rich
1475
345
2.36
4.3
735
14.6
6.2
1135
612
29.5
26.5
10.9
238
46
3.4
9884
1416
2.5
175
0.83
1.54
21
0.001∗
Fatu Kapa
Stéphanie
1555
280
3.4
4.5
767
4.7∗
0.0
1569
532
54.5
0.0
98.9
708
114
282∗
655∗
268
6.6∗
<LOD
0.69
2.05
10
0.76∗
Fatu Kapa
Carla
1664
280
2.8
3.5
594
4.3
0.0
1132
477
59.9
0.0
31.4
691
105
114∗
287∗
53
nm
4.4∗
0.80
1.90
8
1.37∗
Fatu Kapa
I
d
e
f
X
1572
270
3.7
3.9
665
4.2∗
0.0
1282
518
66.4
0.0
44.3
751
113
160∗
28∗
60
nm
3.4∗
0.78
1.93
8
1.08∗
Fatu Kapa
O
b
e
l
X
1669
270
4.6
4.5
771
4.6
0.0
1458
580
71.0
0.0
85.9
777
nm
nm
nm
nm
nm
nm
0.75
1.89
8
-
Fatu Kapa
A
s
t
e
r
X
(
1
)
1540
265
4.4
4.1
693
3.7
1.0
1344
533
64.9
1.2
51.1
755
nm
nm
nm
nm
nm
nm
0.77
1.94
8
-
Fatu Kapa
Fati Ufu
1523
300
3.8
4.6
790
4.9
0.0
1589
580
48.2
0.0
85.4
722
nm
nm
nm
nm
nm
nm
0.73
2.01
12
-
Fatu Kapa
Fati Ufu
1503
280
3.3
4.1
700
4.9
0.0
1380
538
40.0
0.0
65.0
583
nm
nm
nm
nm
nm
nm
0.77
1.97
13
-
Fatu Kapa
Tutafi
1580
315
4.1
4.2
713
5.1
0.0
1405
535
52.9
0.0
65.1
635
nm
nm
nm
nm
nm
nm
0.75
1.97
10
-
IAPSO
Standard sw
-
-
-
3.2
546
0.0
28.2
839
468
10.2
53.2
10.3
27
1.3
90
<LOD
<LOD
<LOD
<LOD
0.9
1.5
46
-
Kulo Lasi
Reference sw
1150
-
-
3.2
551
0.1
29.0
833
457
9.8
53.2
10.6
25
4.4
93
<LOD
<LOD
<LOD
<LOD
0.83
1.5
47
-
Fatu Kapa
Reference sw
1488
-
-
3.3
565
0.0
28.8
841
483
10.4
54.5
10.7
22
5.8
<LOD
<LOD
<LOD
<LOD
<LOD
0.85
1.5
46
-
Fatu Kapa
Reference sw
1572
2
-
3.3
557
0.0
28.7
841
477
10.4
54.2
10.8
23
nm
nm
nm
nm
nm
nm
0.86
1.5
46
-
∗Maximum value when linear regression was not possible; (
1
) only one sample.Fluids from Fatu Kapa were enriched compared to seawater in alkali, alkaline Earth, and transition metals as well as in strontium, bromide, and silica. Conversely, the fluids from Kulo Lasi exhibited a much more complex pattern. They were all highly enriched in transition metals and silica compared to seawater and fluids from Fatu Kapa (e.g., Fe up to ~10 mM). The enrichment versus seawater in alkali metals was not as striking as for Fatu Kapa fluids. As for the alkaline Earth metals, the amount of Ca was identical to seawater and fluids were depleted in Sr compared to seawater. Finally, both depletion and enrichment in Br were observed in the fluids from Kulo Lasi.


## 4.3. Organic Geochemistry

First of all, we would like to mention that because solubility of organic compounds decreases withT and because samples were processed at room temperature, the measured concentrations are probably lower than in situ concentrations. Moreover, it is very likely that a portion of the OM was adsorbed on small particles in the fluids which are not taken into account using our extraction and analytical techniques. As a result, the concentrations we report here probably represent lower estimates of in situ concentrations. However, since in situ measurement techniques are not available yet, these values are the best estimates we can obtain. Note that they also are the first to be published for SVOCs.Formate and acetate reached 16.3 and 15.5μM, respectively, and covaried with Mg in the Kulo Lasi fluids (Figure 4). Concentrations of formate and acetate were significantly higher in the Fatu Kapa area but no correlation with Mg could be observed. Nevertheless, the purest fluids usually showed the highest concentrations. Formate reached 68 ppb at Stéphanie and 722 ppb at Fati Ufu whereas it could not be detected at I
d
e
f
X and Tutafi and was not measured at Carla. Acetate was detected in all analysed samples and concentrations were an order of magnitude higher than the ones of formate (543–2309 ppb) (Table 6).Table 6
Measured concentration of Total Organic Carbon (TOC), formate, acetate, and a selection of individual semi-volatile organic compounds extracted from hydrothermal fluids of the Kulo Lasi and Fatu Kapa vent fields.
Compound
Rtmin
Units
BlankDry
BlankMQ
FU3-PL-14-TiG2deepsea water
FU3-PL-08-TiD2Stéphanie
FU3-PL-04-TiD3Stéphanie
FU3-PL-09-TiG2Stéphanie
FU3-PL-08-TiG3Carla
FU3-PL-06-TiG1Carla
FU3-PL-14-TiG1Idefix
FU3-PL-11-TiD3Idefix
FU3-PL-21-TiG2Fati Ufu
FU3-PL-17-TiD2Fati Ufu
FU3-PL-21-TiG1Fati Ufu
FU3-PL-21-TiG3Tutafi
FU3-PL-20-TiG1Tutafi
pH
-
-
-
-
3.83
4.65
5.42
4.17
4.91
3.97
4.9
4.22
4.26
4.69
3.65
4.14
Mg
-
mM
-
-
54.2
0.6
18.7
44.3
2.7
23.6
0.8
15.5
13.3
17.6
19.3
0.8
0.7
TOC
-
ppm
na
<0.005
na
0.165
na
na
na
na
0.498
na
na
6.514
na
0.304
na
Formate
-
ppb
na
nd
na
65.8
<LOQ
na
na
na
<LOQ
<LOQ
111.7
721.6
na
<LOQ
na
Acetate
-
ppb
na
nd
na
1155.1
543.2
na
na
na
1033.6
995.1
1740.9
2308.8
na
1067.3
na
Nonane
4.68
ppb
nd
nd
0.85 ± 0.51
1.59 ± 0.52
1.17 ± 0.51
1.08 ± 0.51
0.72 ± 0.51
0.58 ± 0.51
0.84 ± 0.51
0.52 ± 0.50
0.64 ± 0.50
0.50 ± 0.51
0.28 ± 0.51
1.52 ± 0.52
2.29 ± 0.54
Decane
5.911
ppb
nd
<0.03
2.21 ± 0.44
2.03 ± 0.44
2.02 ± 0.44
2.10 ± 0.44
3.05 ± 0.45
1.63 ± 0.44
6.92 ± 0.51
2.20 ± 0.44
6.47 ± 0.50
5.58 ± 0.48
2.88 ± 0.45
9.18 ± 0.56
22.16 ± 0.95
Undecane
7.183
ppb
nd
<0.2
11.35 ± 0.97
6.79 ± 0.76
9.52 ± 0.87
11.48 ± 0.98
13.81 ± 1.14
9.61 ± 0.87
23.13 ± 1.88
10.89 ± 0.94
19.13 ± 1.55
26.06 ± 2.14
12.26 ± 1.03
20.48 ± 1.66
26.93 ± 2.21
Dodecane
8.394
ppb
nd
nd
3.36 ± 0.65
1.33 ± 0.57
2.30 ± 0.60
2.98 ± 0.63
3.35 ± 0.65
2.64 ± 0.61
5.12 ± 0.76
3.35 ± 0.65
4.76 ± 0.73
6.52 ± 0.86
3.30 ± 0.65
4.00 ± 0.69
5.14 ± 0.76
Tridecane
9.549
ppb
nd
nd
1.39 ± 0.54
0.35 ± 0.53
0.73 ± 0.53
0.86 ± 0.53
1.37 ± 0.54
1.39 ± 0.54
1.63 ± 0.55
2.21 ± 0.57
1.75 ± 0.55
3.89 ± 0.65
2.27 ± 0.57
1.06 ± 0.54
1.42 ± 0.54
Tetradecane
10.641
ppb
nd
nd
0.53 ± 0.47
0.56 ± 0.47
0.57 ± 0.47
0.59 ± 0.47
0.67 ± 0.46
0.66 ± 0.46
0.59 ± 0.47
0.72 ± 0.46
0.69 ± 0.46
0.64 ± 0.46
0.72 ± 0.46
0.72 ± 0.46
0.70 ± 0.46
Pentadecane
11.675
ppb
nd
nd
0.44 ± 0.28
0.40 ± 0.28
0.48 ± 0.27
0.44 ± 0.28
0.52 ± 0.27
0.59 ± 0.27
0.43 ± 0.28
0.60 ± 0.27
0.57 ± 0.27
0.47 ± 0.28
0.49 ± 0.27
0.62 ± 0.27
0.58 ± 0.27
Hexadecane
12.65
ppb
nd
nd
0.25 ± 0.73
0.40 ± 0.74
0.42 ± 0.73
0.49 ± 0.73
0.64 ± 0.73
0.59 ± 0.74
0.26 ± 0.73
0.84 ± 0.74
0.53 ± 0.73
0.39 ± 0.73
0.37 ± 0.73
0.65 ± 0.74
0.48 ± 0.73
Heptadecane
13.576
ppb
nd
nd
0.57 ± 0.32
1.08 ± 0.32
0.61 ± 0.32
0.87 ± 0.32
1.13 ± 0.33
0.85 ± 0.32
1.20 ± 0.33
1.48 ± 0.33
0.85 ± 0.32
0.67 ± 0.32
0.78 ± 0.32
1.10 ± 0.33
0.98 ± 0.32
Octadecane
14.452
ppb
nd
nd
0.17 ± 0.17
0.30 ± 0.18
0.28 ± 0.18
0.30 ± 0.18
0.35 ± 0.18
0.33 ± 0.18
0.39 ± 0.18
0.42 ± 0.18
0.49 ± 0.19
0.29 ± 0.18
0.25 ± 0.18
0.47 ± 0.18
0.50 ± 0.19
Nonadecane
15.295
ppb
nd
nd
1.08 ± 1.34
1.36 ± 1.35
1.24 ± 1.35
1.38 ± 1.34
1.64 ± 1.36
1.40 ± 1.36
1.33 ± 1.35
1.83 ± 1.38
1.26 ± 1.33
0.86 ± 1.33
1.02 ± 1.34
1.10 ± 1.33
1.36 ± 1.35
Eicosane
16.104
ppb
nd
nd
1.09 ± 1.23
1.75 ± 1.27
1.05 ± 1.25
0.94 ± 1.23
1.13 ± 1.24
1.69 ± 1.27
1.03 ± 1.24
1.46 ± 1.26
1.00 ± 1.23
0.71 ± 1.24
1.19 ± 1.24
1.25 ± 1.24
1.50 ± 1.26
Nonanoic acid
6.914
ppb
nd
nd
3.72 ± 2.53
8.07 ± 2.96
<0.37
5.71 ± 2.67
4.49 ± 2.56
3.49 ± 2.50
4.91 ± 2.60
7.12 ± 2.87
8.94 ± 3.09
9.23 ± 3.10
na
2.86 ± 2.45
9.90 ± 3.21
Decanoic acid
7.542
ppb
nd
nd
1.17 ± 1.65
0.86 ± 1.59
nd
0.53 ± 1.60
0.41 ± 1.65
nd
0.61 ± 1.62
nd
0.84 ± 1.67
0.56 ± 1.68
na
1.09 ± 1.64
0.83 ± 1.66
Undecanoic acid
8.178
ppb
nd
nd
0.18 ± 0.19
0.29 ± 0.20
nd
0.23 ± 0.19
0.25 ± 0.20
0.28 ± 0.19
0.22 ± 0.20
nd
0.26 ± 0.19
0.34 ± 0.19
na
0.35 ± 0.20
0.33 ± 0.19
Dodecanoic acid
8.773
ppb
nd
nd
0.42 ± 0.48
2.10 ± 0.51
0.55 ± 0.48
0.55 ± 0.48
0.78 ± 0.48
0.49 ± 0.47
2.01 ± 0.51
0.69 ± 0.48
1.29 ± 0.49
1.08 ± 0.49
na
1.45 ± 0.49
0.61 ± 0.48
Tridecanoic acid
9.31
ppb
nd
nd
0.28 ± 0.20
0.35 ± 0.19
0.23 ± 0.21
0.24 ± 0.21
0.24 ± 0.20
0.33 ± 0.20
0.27 ± 0.20
0.25 ± 0.21
0.26 ± 0.21
0.32 ± 0.20
na
0.31 ± 0.19
0.27 ± 0.20
Tetradecanoic acid
9.859
ppb
nd
<0.06
0.94 ± 0.32
1.86 ± 0.31
1.44 ± 0.31
0.87 ± 0.33
0.92 ± 0.32
4.28 ± 0.35
1.41 ± 0.31
2.74 ± 0.31
0.90 ± 0.32
1.15 ± 0.32
na
1.42 ± 0.31
1.07 ± 0.32
Pentadecanoic acid
10.355
ppb
nd
nd
0.54 ± 0.30
1.44 ± 0.30
0.82 ± 0.28
0.46 ± 0.30
0.76 ± 0.29
0.57 ± 0.29
1.06 ± 0.29
0.58 ± 0.30
0.52 ± 0.30
0.78 ± 0.29
na
1.02 ± 0.29
0.77 ± 0.29
Hexadecanoic acid
10.902
ppb
nd
nd
1.46 ± 1.20
6.66 ± 1.37
4.47 ± 1.27
1.78 ± 1.20
3.90 ± 1.25
2.91 ± 1.23
7.30 ± 1.41
3.61 ± 1.24
3.24 ± 1.23
4.92 ± 1.29
na
6.09 ± 1.34
5.59 ± 1.32
Heptadecanoic acid
11.317
ppb
nd
nd
0.54 ± 0.61
3.23 ± 0.58
nd
0.89 ± 0.53
2.04 ± 0.54
1.82 ± 0.54
1.04 ± 0.62
1.62 ± 0.55
<0.03
2.89 ± 0.59
na
2.87 ± 0.59
2.79 ± 0.57
Octadecanoic acid
11.78
ppb
nd
nd
0.94 ± 2.16
8.70 ± 2.82
6.32 ± 2.55
1.67 ± 2.32
6.36 ± 2.48
3.49 ± 2.30
11.83 ± 3.29
5.15 ± 2.35
2.64 ± 2.09
5.26 ± 2.40
na
9.19 ± 2.86
9.66 ± 2.96
Ethyl, Benzene
4.344
ppb
nd
<0.1
nd
<0.1
<0.1
nd
nd
<0.1
<0.1
na
0.10 ± 0.35
<0.1
<0.1
nd
0.44 ± 0.23
p-,m-Xylene
4.443
ppb
nd
nd
0.03 ± 0.05
0.10 ± 0.05
0.11 ± 0.05
0.08 ± 0.05
0.10 ± 0.05
0.11 ± 0.05
0.18 ± 0.05
na
0.33 ± 0.05
0.21 ± 0.05
0.15 ± 0.05
0.11 ± 0.05
0.71 ± 0.08
o-Xylene
4.708
ppb
nd
<0.02
0.02 ± 0.05
0.07 ± 0.06
0.06 ± 0.05
0.02 ± 0.06
0.03 ± 0.08
0.06 ± 0.05
0.14 ± 0.06
na
0.33 ± 0.07
0.19 ± 0.06
0.13 ± 0.06
0.06 ± 0.05
0.68 ± 0.09
Styrene
4.831
ppb
nd
nd
0.59 ± 0.14
0.22 ± 0.16
nd
nd
0.46 ± 0.14
nd
0.29 ± 0.15
na
0.21 ± 0.15
0.20 ± 0.15
0.24 ± 0.14
0.37 ± 0.14
0.20 ± 0.14
isopropyl, Benzene
5.006
ppb
nd
nd
0.04 ± 0.05
0.06 ± 0.05
0.07 ± 0.05
0.07 ± 0.05
0.06 ± 0.05
0.08 ± 0.05
0.09 ± 0.05
na
0.09 ± 0.05
0.04 ± 0.06
0.05 ± 0.05
0.09 ± 0.05
0.09 ± 0.05
n-Propyl, Benzene
5.468
ppb
nd
nd
0.03 ± 0.04
0.02 ± 0.04
0.03 ± 0.04
0.02 ± 0.04
0.03 ± 0.04
0.03 ± 0.04
0.03 ± 0.04
na
0.04 ± 0.04
0.03 ± 0.04
0.03 ± 0.05
0.03 ± 0.04
0.04 ± 0.04
1,2,4-triMethyl-Benzene
5.572
ppb
nd
nd
0.03 ± 0.04
0.05 ± 0.04
0.06 ± 0.04
0.04 ± 0.04
0.06 ± 0.05
0.06 ± 0.04
0.04 ± 0.05
na
0.08 ± 0.04
0.07 ± 0.05
0.07 ± 0.04
0.08 ± 0.04
0.07 ± 0.04
1,3,5-triMethyl-Benzene
5.95
ppb
nd
nd
0.02 ± 0.06
0.11 ± 0.07
0.08 ± 0.07
0.06 ± 0.06
0.09 ± 0.06
0.09 ± 0.06
0.11 ± 0.06
na
0.30 ± 0.07
0.25 ± 0.06
0.20 ± 0.07
0.13 ± 0.06
0.19 ± 0.06
sec-Butyl-Benzene
6.106
ppb
nd
nd
0.27 ± 0.05
0.04 ± 0.04
nd
0.04 ± 0.05
0.05 ± 0.06
0.05 ± 0.05
0.06 ± 0.05
na
nd
0.05 ± 0.05
nd
nd
0.07 ± 0.05
2,isopropyl, Toluene
6.305
ppb
nd
nd
0.07 ± 0.03
0.03 ± 0.03
0.03 ± 0.03
0.03 ± 0.03
0.05 ± 0.03
0.03 ± 0.03
0.04 ± 0.03
na
0.04 ± 0.03
0.04 ± 0.03
0.03 ± 0.03
0.05 ± 0.03
0.07 ± 0.03
n-Butyl, Benzene
6.66
ppb
nd
<0.08
0.06 ± 0.03
0.01 ± 0.03
0.01 ± 0.02
0.01 ± 0.03
0.02 ± 0.03
0.01 ± 0.02
0.02 ± 0.02
na
0.02 ± 0.03
0.02 ± 0.02
nd
0.03 ± 0.03
0.03 ± 0.03
Naphthalene
8.351
ppb
nd
<0.01
1.39 ± 0.07
0.49 ± 0.05
0.32 ± 0.05
0.13 ± 0.04
1.24 ± 0.07
0.69 ± 0.05
1.08 ± 0.06
na
0.90 ± 0.06
0.64 ± 0.05
1.99 ± 0.09
1.19 ± 0.06
1.19 ± 0.06
Acenaphthene
11.796
ppb
nd
nd
<0.009
<0.009
<0.009
<0.009
<0.009
<0.009
<0.009
na
<0.009
<0.009
<0.009
<0.009
<0.009
Fluorene
12.778
ppb
nd
nd
nd
0.05 ± 0.03
<0.01
<0.01
0.14 ± 0.03
0.10 ± 0.03
0.16 ± 0.03
na
0.14 ± 0.03
0.09 ± 0.03
0.06 ± 0.03
0.09 ± 0.03
0.07 ± 0.03
Phenanthrene
14.582
ppb
nd
nd
0.02 ± 0.04
0.10 ± 0.04
0.06 ± 0.04
0.06 ± 0.04
0.29 ± 0.05
0.13 ± 0.04
0.20 ± 0.05
na
0.16 ± 0.05
0.10 ± 0.04
0.06 ± 0.04
0.23 ± 0.05
0.17 ± 0.05
Anthracene
14.788
ppb
nd
nd
nd
nd
nd
nd
nd
nd
nd
na
nd
nd
nd
nd
nd
Fluoranthene
17.117
ppb
nd
nd
<0.04
<0.04
<0.04
<0.04
0.06 ± 0.16
<0.04
<0.04
na
0.04 ± 0.16
<0.04
<0.04
0.05 ± 0.16
<0.04
Pyrene
17.52
ppb
nd
nd
<0.03
0.03 ± 0.11
0.03 ± 0.10
<0.03
0.14 ± 0.11
0.07 ± 0.10
0.10 ± 0.11
na
0.06 ± 0.10
0.05 ± 0.11
0.03 ± 0.10
0.09 ± 0.10
0.06 ± 0.10Figure 4
Mixing lines of formate and acetate versus Mg for the Kulo Lasi fluids. Note that the reference deep-sea water sample (FU-PL05-TiG2 noted as SW here) was taken at 1150 m depth above the southern wall of the caldera (see Figure1 for location and Table 3) and thus very likely within the plume [7]. This would account for the unusual concentrations of formate and acetate detected.Heavier extractable organic compounds were not detected in the dry control experiment and only a few were detectable but below limit of quantification (LOQ) in the MQ water blank experiment (Table6). This showed that sample preparation and storage could be considered as contamination-free steps. The levels of heavier extractable organic compounds appeared rather high in the reference water at Fatu Kapa certainly because of the overall spread hydrothermal discharges and diffuse venting in the region [7] (Table 6, Figure 5). This sample was indeed taken mid-way between O
b
e
l
X and A
s
t
e
r
X fields at about 20 m above the seafloor. As a consequence, it is difficult to assess possible contamination originating from sampling device or seawater contribution in the present case. However, earlier studies have shown that they generally did not represent major sources of contamination as for the studied compounds [27, 37]. Nevertheless, in comparison to deep-sea water both the qualitative (Kulo Lasi) and quantitative (Fatu Kapa) data obtained suggested enrichment of the fluids in hydrothermally derived compounds, namely, n-alkanes (C9–C12), n-FAs (C9, C12, C14–C18), and PAHs (fluorene, phenanthrene, pyrene) ([39]; Table 6, Figures 5 and 6). Such enrichment was unclear for >C12  n-alkanes; C10, C11, C13  n-FAs; BTEXs; naphthalene, acenaphthene, and fluoranthene because of their very low concentration and/or the measurement uncertainty.Figure 5
Distribution of n-alkanes, n-fatty acids, mono-, and polyaromatic hydrocarbons (BTEX and PAH) in the purest fluids of the Stéphanie, Carla,I
d
e
f
X, Fati Ufu, and Tutafi sites collected within the Fatu Kapa vent field. Because organic geochemistry does not seem to follow a simple mixing model, endmember concentrations cannot be calculated. To that respect composition of the purest fluids is presented and assumed to be close to endmembers composition. Note that quantitative results are not available for the Kulo Lasi fluids (see Figure 6 for chromatograms).Figure 6
Only qualitative results could be obtained at Kulo Lasi. This figure presents a selection of representative chromatograms obtained for the Kulo Lasi fluid samples. For the sake of clarity, close-ups of a few peaks are shown to illustrate the enrichment of fluids (FU-PL06-TiG1 in red and FU-PL06-TiD3 in green) versus the reference deep-sea water (FU-PL05-TiG2 in blue).Differences in concentrations seemed to exist among the vents over the Fatu Kapa area. Fluids from the Stéphanie vent field had concentrations in hydrocarbons equal or below the reference water sample whereas they were clearly enriched in C9, C12, C14–C18 n-FAs. The Carla fluids were slightly enriched in C9–C12  n-alkanes and showed the highest concentrations in PAHs. Fluids from I
d
e
f
X, Fati Ufu, and Tutafi shared some similarities: a strong enrichment in decane and undecane, alike concentrations in PAHs, and the presence of significant amounts of xylene. However, fluids expelled at the Tutafi vent appeared the most enriched in C9–C11  n-alkanes and xylenes. In terms of fatty acids and considering the analytical error, the 5 vents showed consistent concentrations with C9, C16, and C18 being major. Note that fluids from Fati Ufu seemed depleted in C17 and C18.Generally we did not observe strong linear correlation between the concentration of individual compounds and Mg. Nonetheless, these relations showed that both enrichment and depletion of organic compounds seemed to occur in hydrothermal fluids versus deep-sea water.


## 5. Discussion

The elemental and gas composition of hydrothermal fluids is mainly affected by water/rock interactions and thus the nature of the host rocks, phase separation, magmatic fluid contribution, conductive cooling, and seawater mixing in local recharge zones [45]. In the following discussion we attempt to unravel the occurrence of these various processes both at Kulo Lasi and at Fatu Kapa. Much less is known on processes that control organic geochemistry and are therefore discussed here as well as some implications of the presence of organic compounds in hydrothermal fluids. Implications related to the composition of the fluids are dependent on fluxes; therefore, we give here an attempt to provide order of magnitude estimates of heat and mass fluxes.


### 5.1. Plume-Fluids Relations

The geochemistry and dynamics of the plumes over the Wallis and Futuna region have been studied elsewhere [7]. The Kulo Lasi plume has been proposed to be the result of both high-T and diffuse venting from multiple vents located both on the floor and on the wall of the caldera. Consistently, both types of venting have been observed [6]. Helium, nephelometry, and Mn profiles recorded above the northern sampling area showed constant elevated concentrations in the 300 masf and were assumed to be the results of diffuse venting. Our results show that they are obviously the result of the numerous small black smokers observed on the seafloor (Figure 2). The methane concentration in the sampled fluids was extremely low which cannot account for the elevated concentration of CH4 in the water column reported by Konn et al. [7]. The strong difference in the CH4/Mn ratios between the plume (0.7–4.5) and the sampled fluids (0.001–0.01) is another line of evidence that the methane plume has another origin compared to hydrothermal fluids and likely come from degassing of the lava flows as suggested by the authors. Although other fluid discharges likely remain undiscovered, this is consistent with a past eruption and accumulation of the water mass in the caldera [39].A great diversity of the fluid compositions was expected from the geological settings and the water column survey and was indeed confirmed by the mixing lines that point to as many endmembers as sampled areas (FigureS1). CH4/TDM ratios also differed among the vents but it was not due to sole CH4 concentration variations as suggested earlier (Table 5) [7]. Finally, the very weak nephelometry of the Fatu Kapa plume is likely best explained by the low metal contents of the fluids.


### 5.2. Reaction Zone Depth

The solubility of Quartz in hydrothermal fluids has been studied by different authors (e.g., [46]). According to these works silica concentration in the fluid may be used to estimate the depth of the reaction zone. The silica concentration measured in the Kulo Lasi and Fatu Kapa fluids indicates a hydrothermal reaction zone at seafloor or in the water column (Figure S2). Both observations suggest that, in this area, fluids are not in equilibria with Quartz at the pressure and temperature of the fluid emission. And this prevents using Si as a geothermometer to determine the depth of the reaction zone.All fluids at Fatu Kapa were indeed highly depleted in Si with respect to the Quartz saturation curve at 170 bar, 300°C (Si ~12 mM in FigureS2). A higher temperature in the reaction zone (>350°C at 200 bar) may explain a lower Si concentration in the fluid at equilibrium as Quartz solubility decreases (Figure S2). The dispersion of a great number of vent fields over a large area of recent lava flows may be due to complex fluid pathways that favour conductive cooling of the fluid and subsurface loss of silica before venting on the seafloor. Consistently, amorphous silica was common in the seafloor deposits at Fatu Kapa where opal was abundant as a late mineral in sulphides and as silica crusts (slabs) at the surface of the deposits [6]. In conclusion, this would indicate a fairly shallow reaction zone at Fatu Kapa (a few 100 mbsf) in agreement with the geological settings and the possible occurrence of dikes.


### 5.3. Chlorinity

Phase separation is often accounted for salinity deviation in hydrothermal fluids versus seawater [47, 48]. Phase separation is of great importance in metal transportation and ore-forming processes, for example, [24, 49–51]. It also implies that seawater experiences dramatic changes in its physical and chemical properties as it reaches the super- or subcritical state. In particular, strong modification of the density and ionic strength of seawater enables unconventional chemical reactions, hence a likely importance in hydrothermal organic geochemistry, for example, [52]. The measured P and T of the Kulo Lasi fluids are almost on the critical curve of seawater meaning that liquid and vapor phase may coexist at Kulo Lasi. An adiabatic decompression of supercritical seawater (initial fluid and equivalent to 3.2 wt% NaCl) as it rises towards the seafloor would cause it to separate, at about 320–350 bar and 415–420°C, into two phases having the NaCl percentages observed at Kulo Lasi (Figure S3) [53, 54].Similarly, the excess salinity of the Fatu Kapa fluids (9 to 41%) could be explained by phase separation and is supported by the Br/Cl ratios which significantly differed from seawater [45, 55]. Since we have not sampled any Cl-depleted fluids we may infer that phase separation may have occurred in the past and that only the brine phase was venting at the time of the cruise. Alternatively water-rock reactions could represent a significant Cl source to the fluids [56]. Indeed, the felsic lavas collected in the Fatu Kapa area contained up to 10 times more Cl than MORB(Aurélien Jeanvoine, personal communication).


### 5.4. Water-Rock Reactions

Generally, fluids from Kulo Lasi and Fatu Kapa were not typical of back-arc settings but shared similarities with ridge, arc, and back-arc settings fluid signatures [3]. The Kulo Lasi fluids have unusually high concentrations of Mg (24.6 to 34.9 mM) and SO4 (6.2 to 12.0 mM) at low pH (2.24 to 3.32) and high T (338–343°C) which indicate that significant seawater mixing at subsurface or during sampling is rather unlikely. In back-arc context, the occurrence of Mg and SO4 in endmember fluids can be explained by a magmatic fluid input as observed at the Desmos [5, 57], Rota 1 and Brother sites [58, 59]. Magmatic-derived SO2 would disproportionate according to reaction (1) at temperatures measured at Kulo Lasi (e.g., [5, 60]). This is consistent with widespread occurrences of native sulfur on fresh lava near the active vents [39] as well as the low pH of the fluids. (1)
3
S
O
2
a
q
+
2
H
2
O
=
S
0
s
+
4
H
+
+
2
S
O
4Yet CO2 concentrations are low and the Na : K : Mg ratios are strongly different to seawater. The latter suggests a contribution of Mg by dissolution of magnesium silicates [39]. Besides, the high Li and Rb concentrations and the presence of recent lava injected in the caldera point to water/fresh hot volcanic rocks interactions. Notably, such interactions are capable of producing the extremely high concentration of H2 measured in the Cl-depleted sample and thus the very unusual H2/CH4 observed [61] (Figure S4). High concentrations of metals are consistent with the highly acidic nature of the fluids coupled with high H2/H2S ratios [62, 63].The relatively mild pH,3He/CO2, and R/Ra ratios of the Fatu Kapa fluids are diagnostic of the occurrence of seawater/MORB interactions [64–66] (Figure S5). Consistently, the geochemistry of the Fatu Kapa fluids was very similar to the Vienna Woods ones whose composition is mainly the result of interactions with basalts [3, 4]. Yet metal concentrations were lower at Fatu Kapa while Ca, K, and Rb were higher and Li is similar. Plausible explanations for the extremely low metal concentrations observed in the Fatu Kapa fluids are conductive cooling; water/metal-poor rocks interactions; subsurface metal trapping under silica and barite slabs [6]. Given the wide variety of lithologies sampled in the area, fluid compositions are likely the results of interactions with a wide range of rock source chemistries. To that respect, the composition of the local lavas that are characteristic of andesite, trachy-andesite, dacite, and trachy-dacite probably best explains the enrichment in Ca and in the mobile alkali metals K and Rb.


### 5.5. What Controls Organic Geochemistry?

The origin of hydrocarbon gases and SVOCs in natural systems including hydrothermal systems has been the focus of many studies since the abiotic origin of some hydrocarbons was postulated ([67, 68] for a review). Both field and experimental studies have tried to unravel the origin of hydrocarbons making use of stable isotopes (e.g., reviews of [34, 35]). Although there are strong discrepancies among studies, the variation of δ
13C with the carbon number may be a reasonable indicator of the origin. The trend observed in the Cl-depleted sample of Kulo Lasi was very similar to the ones attributed to an abiogenic origin in the Precambrian shields or in the Lost City hydrothermal field [69, 70]. The Kulo Lasi Cl-rich sample exhibited a pattern that has been observed in several Fischer-Tropsch type (FTT) experiments [34]. The strong positive or negative fractionation between C1 and C2 observed in the hot fluids of Kulo Lasi is likely due to chain initiation [71]. Conversely, the low-T (135°C) sample that was collected in a beehive-type smoker covered with bacterial mats showed a regular positive trend which has been proposed to be diagnostic of a thermogenic origin. Although we concede that the abiogenic origin of C2+ hydrocarbon gases in the Kulo Lasi field will need more investigation, methane is clearly at the border of abiogenic and thermogenic domains both at Kulo Lasi and at Fatu Kapa with δ
13C values ranging from −29 to −6.1‰ ([72] and Figure 7). Carbon isotopes of CH4 and CO2 suggest that methane underwent oxidation, possibly by bacteria, at both sites and may explain the extremely low concentrations observed (Figure 8 in [73]). Consistently and according to thermodynamic calculations, methanogenesis should be limited under the P, T, and redox conditions present at the Futuna sites and CH4 consumption might be prevalent [31].Figure 7
Modified after Etiope and Sherwood Lollar [9]. The isotopic composition of CH4 in the Fatu Kapa fluids falls into the abiotic gas category but differs from the typical isotopic signature of CH4 at Mid-Atlantic Ridge’s vent fields.By contrast, carbon isotopes have not appeared to be useful up to date in determining the origin of heavier organic compounds [74]. Several processes are likely to occur simultaneously and to use several C sources, resulting in a nondiagnostic bulk δ
13C signature. Several experimental and theoretical studies indicate that a range of organic compounds including linear alkanes and FAs could form and persist in natural hydrothermal systems (e.g., [31–35]). However, according to the calculated fH2 at P and T of the study sites, the redox conditions are likely buffered by Hematite-Magnetite (HM) or an even more oxidizing mineral assemblage which appear less favourable for abiotic synthesis than Pyrite-Pyrrhotite-Magnetite, Fayalite-Magnetite-Quartz, or ultramafic rocks assemblages [27, 32, 33] (Table 4). The occurrence of organic compounds in our fluids must thus be attributed to a great part to other processes. Microbial production and thermal degradation of microorganisms, OM detritus, and/or refractory dissolved OM represent good candidates to produce soluble organic compounds. PAHs are indeed common products of pyrolysis of OM [26, 75, 76]. Long chained fatty acids are major constituent of organisms and their presence in the Futuna fluids could be easily associated with thermal degradation of biomass or OM [26, 77]. Yet the distribution of the compounds found in the fluids does not match a simple process of OM degradation. Only >C13  n-FAs occurred in sediments with C16 being the most abundant (Figure S6). However, similar to our samples, both odd and even carbon number n-FAs were observed in the C14–C20 range with odd FAs being less abundant. Petroleum exhibits nearly equal levels of C14–C20  n-FAs. Only the even series has been reported in both massive sulphide deposits (MSD) and hydrothermal mussels with C16 being the most abundant. Short chain FAs (<C13) have only been reported in Lost City fluids but here again only the even series occurred. In any case C9 was reported whereas it was nearly the most abundant in our fluids. Abiotic processes may still be considered as nonanoic acid could be synthesized from CO2 and H2 [31], nonane [78], or undecane [79]. As a difference the presence of C16 and C18 n-FAs in significant amount in the fluids from Fatu Kapa may represent a direct microbial contribution. The distribution observed in the Fatu Kapa fluids likely reflects the occurrence of several concomitant processes possibly including production reactions (abiotic and thermogenic) and consumption mechanisms (adsorption and complexation).Nonvolatile n-alkanes are usually associated with lowerT processes such as in oil fields or at the Middle Valley hydrothermal vent field [80]. In the Guaymas basin, where n-alkane-rich sediment samples have been reported, it is less clear what temperature they were exposed to. However and as far as we understood high temperatures were rather associated with absence of n-alkanes and presence of PAHs consistently with high-temperature OM pyrolysis [26, 81, 82]. Pyrolytic processes resulted in the presence of light hydrocarbon gases with an exception of some high T (>200°C) fluids containing C9 and C10  n-alkanes. n-Alkanes also occur in solids from unsedimented hydrothermal vent fields ([76] and references therein). Notably, the n-alkanes distribution in our fluids does not resemble any aspects neither the ones resulting of low-T processes nor the ones created by high-T FTT reactions [83, 84] (Figure S7). C10–C20  n-alkanes usually occur in equivalent amounts in petroleum or show a consistent decrease with molecular weight. Experimental FTT reactions produced consistent increasing concentrations from C9 to C12 and then consistent decreasing concentrations to C20. Similar patterns are also associated with the kerosene fraction of petroleum [85]. Distribution patterns in hydrothermal solids are difficult to picture as usually only chromatograms are provided in the studies, for example, [86], but they largely differ by the simple fact that <C14 alkanes were not detected in most cases as in sediments from various locations [87]. The smaller alkanes may well be preferentially entrained in fluid circulation but they are more likely the result of other processes, especially high-temperature ones, and including abiotic reactions. Note that the latter should not be reduced to sole FTT reactions because supercritical water is a fabulous medium for unconventional reactions [88–90].Formate and acetate have been given more attention in both laboratory [91–93] and field hydrothermal studies [28, 29] as these small molecules are likely to prevail according to thermodynamic studies (e.g., [31–33]). Where usually formate dominates, acetate was found to be more abundant in fluids from Fatu Kapa. According to Shock studies, at 280–300°C, formic acid concentrations should not be much higher than acetic acid, but this is not enough to explain our “reverse” concentrations. And especially it is not consistent with higher amounts in the 300°C fluids. A ratio close to 1 was observed at Kulo Lasi which may indicate that different production/consumption processes occur. Also the concentrations of the formate and acetate plotted on a line versus Mg which suggest that the fate of these volatile fatty acids at Kulo Lasi is controlled by simple mixing; that is there would be no consumption/production when fluid mixes with seawater (Figure 4). The deep-seawater concentrations were high compared to what is usually reported in the literature which was most likely due to plume contribution [27, 28]. This supports the simple mixing model hypothesis and is consistent with the near absence of organisms around those chimneys.


### 5.6. Organic Compounds: Implications for Biology, Mineral Resources, and C Cycling

The idea that life could have originated in hydrothermal systems from abiotic reactions was postulated in the late 70s [94]. However, the question of the origin of organic compounds in hydrothermal systems has remained ever since they were evidenced in natural environments [95]. On the one hand, a biogenic or thermogenic origin seems most likely for most compounds investigated so far; on the other hand, one cannot exclude that some of the formate and aliphatic hydrocarbons form abiotically [13, 26–28, 30, 96]. As detailed in the previous section, our results are consistent with a mix of origin although abiotic synthesis likely occurs to a far smaller extent than other processes that would overprint an abiotic signature.Upon the hot topic of the origin of life, the mere presence of organic compounds is highly important for the fauna at the local and regional scales. It is well established that VFAs constitute a significant food source for some microorganisms and thus help sustaining hydrothermal ecosystems [97–100]. Besides, some bacteria have proven to be capable of using naphthalene [101] and tubeworms, hydrocarbons [102].Organics can form complexes with metals [20, 21]. This greatly improves the dispersion of metals in the ocean and prevents them from precipitation as sulphides or oxyhydroxydes [23, 103]. Notably fatty acids are efficient ligands that play a major role in making metals bioavailable as well as in transporting them both through the upper crust ([17] and references therein) and through the water column in the plume [11, 104–106]. In addition, they have been shown to be involved in growth/dissolution processes of some minerals [19, 107]. For these reasons, they are of particular importance in ore-forming processes. Hydrocarbons which are weaker ligands would react with sulfates to generate bisulfide (HS−), which in turn would easily react with metal chlorides to form metal sulphides according to the following mass balance equations:(2)
3
S
O
4
2
-
+
3
H
+
+
4
R
–
C
H
3
⟶
4
R
–
C
O
2
H
+
H
S
-
+
4
H
2
O
(3)
H
S
-
+
M
e
C
l
2
⟶
M
e
S
+
H
+
+
2
C
l
-where R is a carbonated chain, either aliphatic or aromatic, and represents OM [108]. To that respect hydrocarbons are likely to be involved in depositional processes of metals. Notably associations of aliphatic and aromatic hydrocarbons with mineral deposits have also been observed on the EPR [109] and in sulphide sedimentary deposits on land [104].


### 5.7. Fluxes: Importance of Back-Arc Hydrothermal Systems to the Ocean Geochemistry

Hydrothermal input to the ocean via plumes has long been neglected but recent results of the GEOTRACES program clearly show its importance in terms of metals and trace elements transportation and implications for ocean biogeochemistry [13, 110–113]. While it is now well established that MOR hydrothermal discharge has a large impact on the global ocean chemistry and element cycles, the relative impact of hydrothermal activity from other hydrothermal settings has not been established. The extensive hydrothermal activity reported in the Wallis and Futuna region suggests that back-arc system hydrothermalism may be of much greater importance than previously anticipated [7, 114]. Estimation of hydrothermal fluxes is generally challenging and very few data are available in the literature [115–118]. Therefore we believe that any kind of estimation, even orders of magnitudes are of importance to make advances in this field. We propose to combine two different approaches based on geophysical data and video recordings (see here), respectively, to propose such estimates with some confidence.


#### 5.7.1. Estimation Using Geophysics

We can make an order of magnitude estimate of the heat flux from the different hydrothermally active areas based on the physical characteristics of the plumes. Marshall and coworkers [119–121] have proposed a scaling relationship between the heat flux at an interface, Hf, the ambient buoyancy frequency (N) in the surroundings of the plume, the characteristic size (R
s) of the heat transfer region, and the equilibrium height (or depth; h) reached by the plume, as(4)
H
f
=
ρ
·
C
p
g
·
α
·
R
s
·
N
·
h
5
3
,where ρ is seawater density (1030 kg·m−3), C
p is heat capacity of seawater (~4000 J·kg−1·K−1), and g is gravitational acceleration (9.81 m·s−2), and α is the thermal expansion coefficient of seawater (10−4 K−1). The ambient buoyancy frequency (N) can be estimated to be between 0.001 and 0.002 s−1 from CTD profiles in the area using a routine in the UNESCO Sea Water Library described by Jackett and Mcdougall [122]. The radius (R
s) of the Kulo Lasi caldera is 2500 m and the plume rose in average about 200 m above seafloor (top layer boundary) [7]. For order of magnitude estimates, the ~130 km2 Fatu Kapa area can be approximated by a disk of radius 6400 m, with a similar plume height. Introducing these numbers in (4) leads to heat flux estimates ranging between 100 and 800 W·m−2 for the Kulo Lasi caldera and 50 and 400 W·m−2 for the Fatu Kapa area, which is greatly dependent on the value for buoyancy frequency. While these estimates scale proportionally with the area considered to be hydrothermally active, they integrate the sources within the area which do not demand that the whole area be active. We estimate that total heat inputs are in the 2–16 GW for the Kulo Lasi caldera and 5–40 GW for the Fatu Kapa areas.


#### 5.7.2. Estimation Based on Video Postprocessing

Video recordings could be used to estimate fluid velocities of the Carla andO
b
e
l
X chimneys and of a few smokers at Kulo Lasi using for instance the Typhoon algorithm [123] (Figures S8–S11). This optical flow method recovers the (2D) fluid flow from the apparent displacements, in an image sequence, of tracers advected by the flow. Here, the plume acts as the tracer. Compensation for the camera and vehicle motion and parallax correction were not possible, so the investigated video sequences where chosen according to (i) the overall stability of the camera and vehicle and (ii) the plume being as perpendicular to the camera as possible. The relevant lengths scales (image spatial resolution and diameter of the chimneys) had to be estimated from known object sizes in the same ground, typically shrimps. External diameters of the chimney were used for calculation as any estimation of the internal diameter on video recordings would be too speculative. Note that (i) chimney samples taken at Kulo Lasi exhibited similar internal and external diameters; (ii) the large anhydrite chimneys (e.g., O
b
e
l
X, Carla) at Fatu Kapa did not seem to have any central conduit but rather exhibited a sponge-like structure leaking fluid at a high velocity from the entire volume. As a result, we believe the overestimation resulting from this assumption to be limited. Finally, the observed flow velocity is assumed to be constant across the jet section. Given all these limitations and assumptions, the resulting fluxes values should be taken as an indication of their order of magnitude.The fluid velocity was estimated to be on average 0.05, 0.15, and 1 m s−1 for Kulo Lasi, Carla, and O
b
e
l
X, respectively. In terms of heat fluxes, Carla (diameter ca. 70 cm) would generate ~6 MW while O
b
e
l
X (diameter ca. 250 cm) would produce ~5.7 GW, respectively. Associated mass fluxes would be 54 L s−1 and 5 m3 s−1 which means, for instance, that the single O
b
e
l
X chimney could generate an input of 2.6 × 107 mol y−1 CH4 to the ocean. Comparatively, estimation of the total efflux of methane from serpentinisation ranges from 15 to 84 × 109 mol y−1 including 9 × 109 mol y−1 for the sole slow spreading ridges. Similarly, the Carla chimney would release about 5.7 × 103 mol y−1 of dodecane that may help forming 1.4 mol y−1 of metal sulphides (see Section 5.6). Cumulative observations during the dives brought to a total of 220 smokers of various sizes (~5 cm to ~2.5 m in diameter) and apparent flows (strong, medium, slow). We assigned the strong, medium, and slow flows observed to the velocities of O
b
e
l
X, Carla, and Kulo Lasi, respectively. At Kulo Lasi about 100 smokers were counted during the Nautile dives and all appeared very similar in diameter (~3 cm) and fluid flow (0.05). Keeping in mind these uncertainties, an order of magnitude of the heat and mass fluxes generated by hot smokers at Fatu Kapa are estimated to be 6.8 GW and 6 m3 s−1 for the Fatu Kapa area versus 9 MW and 6 L s−1 for the Kulo Lasi caldera. This means, for example, that the total Fe flux from hot fluids emanating from the caldera would be up to 1.9 × 106 mol y−1 versus recent estimations of the global hydrothermal iron input that are about 109 mol y−1 [112, 124]. The average nonanoic acid concentration in Fatu Kapa purest fluids is 7.25 ppb, which would result in 1.4 × 106 mol y−1 released in the ocean by the Fatu Kapa hot smokers. The carboxylic acid functional group of fatty acids makes them good potential ligands to form coordination complexes with iron, which stabilises iron in the plume in its reduced form [103, 125]. Hence, the example of nonanoic acid suggests that fatty acids could largely contribute to iron stabilisation.However, the high-temperature fluxes calculated above failed to include heat fluxes from diffusive venting, which was largely present in both areas and is thought to be an important part of the global hydrothermal heat flux (up to 98%) [126]. The surface of the diffusive areas was also assessed on the videos. However, because the velocity of diffusive fluids could not be estimated using Typhoon, we assumed hydrothermal waters are exiting the seafloor at the minimum velocity reported for low temperature flow (0.04 m s−1) [127]. The cumulative surface of diffusive areas with a typical temperature of 10°C reached 100 m2 at Kulo Lasi and 2885 m2 at Fatu Kapa. In addition, a particular area of about 300 m2 at Kulo Lasi consisted in hundreds of silica chimney diffusing a 40°C fluid [6]. The resulting contribution of diffuse venting to the heat flux would be 2.14 GW and 5.3 GW at Kulo Lasi and Fatu Kapa, respectively. This brings the total heat flux estimates at 2.15 GW and 12 GW, respectively, which is consistent with the estimates obtained using the lower N value as well as the fact that only a small portion of the total surface of the sites was explored with the submersible.


#### 5.7.3. Summary

According to these different estimates heat efflux at Kulo Lasi and Fatu Kapa are conservatively estimated to be at least for 1-2 GW and 5–10 GW, respectively; this estimate is based on the lowN value, whereas using the higher N suggests a flux almost 10x higher. It seems highly likely that the Wallis and Futuna active areas combined with the 3 calderas to the East [114] have a heat flux of >10 GW. Vent fields on MOR have been reported to generate between 10 MW and 25 GW ([116, 117, 127, 128] and references therein) and the total hydrothermal heat flux at MORs is estimated to be about 1000 GW [129, 130]. This suggests that the presently discovered area might be of significant importance in the global budget and that back-arc hydrothermal activity contributes as much as MOR systems, and, possibly more, to the global ocean chemistry and cycles. Few estimates of hydrothermal heat flux have been published and the relative importance of heat, fluid, and geochemical hydrothermal fluxes from different environments will require studies designed to more accurately gauge these fluxes.


## 5.1. Plume-Fluids Relations

The geochemistry and dynamics of the plumes over the Wallis and Futuna region have been studied elsewhere [7]. The Kulo Lasi plume has been proposed to be the result of both high-T and diffuse venting from multiple vents located both on the floor and on the wall of the caldera. Consistently, both types of venting have been observed [6]. Helium, nephelometry, and Mn profiles recorded above the northern sampling area showed constant elevated concentrations in the 300 masf and were assumed to be the results of diffuse venting. Our results show that they are obviously the result of the numerous small black smokers observed on the seafloor (Figure 2). The methane concentration in the sampled fluids was extremely low which cannot account for the elevated concentration of CH4 in the water column reported by Konn et al. [7]. The strong difference in the CH4/Mn ratios between the plume (0.7–4.5) and the sampled fluids (0.001–0.01) is another line of evidence that the methane plume has another origin compared to hydrothermal fluids and likely come from degassing of the lava flows as suggested by the authors. Although other fluid discharges likely remain undiscovered, this is consistent with a past eruption and accumulation of the water mass in the caldera [39].A great diversity of the fluid compositions was expected from the geological settings and the water column survey and was indeed confirmed by the mixing lines that point to as many endmembers as sampled areas (FigureS1). CH4/TDM ratios also differed among the vents but it was not due to sole CH4 concentration variations as suggested earlier (Table 5) [7]. Finally, the very weak nephelometry of the Fatu Kapa plume is likely best explained by the low metal contents of the fluids.


## 5.2. Reaction Zone Depth

The solubility of Quartz in hydrothermal fluids has been studied by different authors (e.g., [46]). According to these works silica concentration in the fluid may be used to estimate the depth of the reaction zone. The silica concentration measured in the Kulo Lasi and Fatu Kapa fluids indicates a hydrothermal reaction zone at seafloor or in the water column (Figure S2). Both observations suggest that, in this area, fluids are not in equilibria with Quartz at the pressure and temperature of the fluid emission. And this prevents using Si as a geothermometer to determine the depth of the reaction zone.All fluids at Fatu Kapa were indeed highly depleted in Si with respect to the Quartz saturation curve at 170 bar, 300°C (Si ~12 mM in FigureS2). A higher temperature in the reaction zone (>350°C at 200 bar) may explain a lower Si concentration in the fluid at equilibrium as Quartz solubility decreases (Figure S2). The dispersion of a great number of vent fields over a large area of recent lava flows may be due to complex fluid pathways that favour conductive cooling of the fluid and subsurface loss of silica before venting on the seafloor. Consistently, amorphous silica was common in the seafloor deposits at Fatu Kapa where opal was abundant as a late mineral in sulphides and as silica crusts (slabs) at the surface of the deposits [6]. In conclusion, this would indicate a fairly shallow reaction zone at Fatu Kapa (a few 100 mbsf) in agreement with the geological settings and the possible occurrence of dikes.


## 5.3. Chlorinity

Phase separation is often accounted for salinity deviation in hydrothermal fluids versus seawater [47, 48]. Phase separation is of great importance in metal transportation and ore-forming processes, for example, [24, 49–51]. It also implies that seawater experiences dramatic changes in its physical and chemical properties as it reaches the super- or subcritical state. In particular, strong modification of the density and ionic strength of seawater enables unconventional chemical reactions, hence a likely importance in hydrothermal organic geochemistry, for example, [52]. The measured P and T of the Kulo Lasi fluids are almost on the critical curve of seawater meaning that liquid and vapor phase may coexist at Kulo Lasi. An adiabatic decompression of supercritical seawater (initial fluid and equivalent to 3.2 wt% NaCl) as it rises towards the seafloor would cause it to separate, at about 320–350 bar and 415–420°C, into two phases having the NaCl percentages observed at Kulo Lasi (Figure S3) [53, 54].Similarly, the excess salinity of the Fatu Kapa fluids (9 to 41%) could be explained by phase separation and is supported by the Br/Cl ratios which significantly differed from seawater [45, 55]. Since we have not sampled any Cl-depleted fluids we may infer that phase separation may have occurred in the past and that only the brine phase was venting at the time of the cruise. Alternatively water-rock reactions could represent a significant Cl source to the fluids [56]. Indeed, the felsic lavas collected in the Fatu Kapa area contained up to 10 times more Cl than MORB(Aurélien Jeanvoine, personal communication).


## 5.4. Water-Rock Reactions

Generally, fluids from Kulo Lasi and Fatu Kapa were not typical of back-arc settings but shared similarities with ridge, arc, and back-arc settings fluid signatures [3]. The Kulo Lasi fluids have unusually high concentrations of Mg (24.6 to 34.9 mM) and SO4 (6.2 to 12.0 mM) at low pH (2.24 to 3.32) and high T (338–343°C) which indicate that significant seawater mixing at subsurface or during sampling is rather unlikely. In back-arc context, the occurrence of Mg and SO4 in endmember fluids can be explained by a magmatic fluid input as observed at the Desmos [5, 57], Rota 1 and Brother sites [58, 59]. Magmatic-derived SO2 would disproportionate according to reaction (1) at temperatures measured at Kulo Lasi (e.g., [5, 60]). This is consistent with widespread occurrences of native sulfur on fresh lava near the active vents [39] as well as the low pH of the fluids. (1)
3
S
O
2
a
q
+
2
H
2
O
=
S
0
s
+
4
H
+
+
2
S
O
4Yet CO2 concentrations are low and the Na : K : Mg ratios are strongly different to seawater. The latter suggests a contribution of Mg by dissolution of magnesium silicates [39]. Besides, the high Li and Rb concentrations and the presence of recent lava injected in the caldera point to water/fresh hot volcanic rocks interactions. Notably, such interactions are capable of producing the extremely high concentration of H2 measured in the Cl-depleted sample and thus the very unusual H2/CH4 observed [61] (Figure S4). High concentrations of metals are consistent with the highly acidic nature of the fluids coupled with high H2/H2S ratios [62, 63].The relatively mild pH,3He/CO2, and R/Ra ratios of the Fatu Kapa fluids are diagnostic of the occurrence of seawater/MORB interactions [64–66] (Figure S5). Consistently, the geochemistry of the Fatu Kapa fluids was very similar to the Vienna Woods ones whose composition is mainly the result of interactions with basalts [3, 4]. Yet metal concentrations were lower at Fatu Kapa while Ca, K, and Rb were higher and Li is similar. Plausible explanations for the extremely low metal concentrations observed in the Fatu Kapa fluids are conductive cooling; water/metal-poor rocks interactions; subsurface metal trapping under silica and barite slabs [6]. Given the wide variety of lithologies sampled in the area, fluid compositions are likely the results of interactions with a wide range of rock source chemistries. To that respect, the composition of the local lavas that are characteristic of andesite, trachy-andesite, dacite, and trachy-dacite probably best explains the enrichment in Ca and in the mobile alkali metals K and Rb.


## 5.5. What Controls Organic Geochemistry?

The origin of hydrocarbon gases and SVOCs in natural systems including hydrothermal systems has been the focus of many studies since the abiotic origin of some hydrocarbons was postulated ([67, 68] for a review). Both field and experimental studies have tried to unravel the origin of hydrocarbons making use of stable isotopes (e.g., reviews of [34, 35]). Although there are strong discrepancies among studies, the variation of δ
13C with the carbon number may be a reasonable indicator of the origin. The trend observed in the Cl-depleted sample of Kulo Lasi was very similar to the ones attributed to an abiogenic origin in the Precambrian shields or in the Lost City hydrothermal field [69, 70]. The Kulo Lasi Cl-rich sample exhibited a pattern that has been observed in several Fischer-Tropsch type (FTT) experiments [34]. The strong positive or negative fractionation between C1 and C2 observed in the hot fluids of Kulo Lasi is likely due to chain initiation [71]. Conversely, the low-T (135°C) sample that was collected in a beehive-type smoker covered with bacterial mats showed a regular positive trend which has been proposed to be diagnostic of a thermogenic origin. Although we concede that the abiogenic origin of C2+ hydrocarbon gases in the Kulo Lasi field will need more investigation, methane is clearly at the border of abiogenic and thermogenic domains both at Kulo Lasi and at Fatu Kapa with δ
13C values ranging from −29 to −6.1‰ ([72] and Figure 7). Carbon isotopes of CH4 and CO2 suggest that methane underwent oxidation, possibly by bacteria, at both sites and may explain the extremely low concentrations observed (Figure 8 in [73]). Consistently and according to thermodynamic calculations, methanogenesis should be limited under the P, T, and redox conditions present at the Futuna sites and CH4 consumption might be prevalent [31].Figure 7
Modified after Etiope and Sherwood Lollar [9]. The isotopic composition of CH4 in the Fatu Kapa fluids falls into the abiotic gas category but differs from the typical isotopic signature of CH4 at Mid-Atlantic Ridge’s vent fields.By contrast, carbon isotopes have not appeared to be useful up to date in determining the origin of heavier organic compounds [74]. Several processes are likely to occur simultaneously and to use several C sources, resulting in a nondiagnostic bulk δ
13C signature. Several experimental and theoretical studies indicate that a range of organic compounds including linear alkanes and FAs could form and persist in natural hydrothermal systems (e.g., [31–35]). However, according to the calculated fH2 at P and T of the study sites, the redox conditions are likely buffered by Hematite-Magnetite (HM) or an even more oxidizing mineral assemblage which appear less favourable for abiotic synthesis than Pyrite-Pyrrhotite-Magnetite, Fayalite-Magnetite-Quartz, or ultramafic rocks assemblages [27, 32, 33] (Table 4). The occurrence of organic compounds in our fluids must thus be attributed to a great part to other processes. Microbial production and thermal degradation of microorganisms, OM detritus, and/or refractory dissolved OM represent good candidates to produce soluble organic compounds. PAHs are indeed common products of pyrolysis of OM [26, 75, 76]. Long chained fatty acids are major constituent of organisms and their presence in the Futuna fluids could be easily associated with thermal degradation of biomass or OM [26, 77]. Yet the distribution of the compounds found in the fluids does not match a simple process of OM degradation. Only >C13  n-FAs occurred in sediments with C16 being the most abundant (Figure S6). However, similar to our samples, both odd and even carbon number n-FAs were observed in the C14–C20 range with odd FAs being less abundant. Petroleum exhibits nearly equal levels of C14–C20  n-FAs. Only the even series has been reported in both massive sulphide deposits (MSD) and hydrothermal mussels with C16 being the most abundant. Short chain FAs (<C13) have only been reported in Lost City fluids but here again only the even series occurred. In any case C9 was reported whereas it was nearly the most abundant in our fluids. Abiotic processes may still be considered as nonanoic acid could be synthesized from CO2 and H2 [31], nonane [78], or undecane [79]. As a difference the presence of C16 and C18 n-FAs in significant amount in the fluids from Fatu Kapa may represent a direct microbial contribution. The distribution observed in the Fatu Kapa fluids likely reflects the occurrence of several concomitant processes possibly including production reactions (abiotic and thermogenic) and consumption mechanisms (adsorption and complexation).Nonvolatile n-alkanes are usually associated with lowerT processes such as in oil fields or at the Middle Valley hydrothermal vent field [80]. In the Guaymas basin, where n-alkane-rich sediment samples have been reported, it is less clear what temperature they were exposed to. However and as far as we understood high temperatures were rather associated with absence of n-alkanes and presence of PAHs consistently with high-temperature OM pyrolysis [26, 81, 82]. Pyrolytic processes resulted in the presence of light hydrocarbon gases with an exception of some high T (>200°C) fluids containing C9 and C10  n-alkanes. n-Alkanes also occur in solids from unsedimented hydrothermal vent fields ([76] and references therein). Notably, the n-alkanes distribution in our fluids does not resemble any aspects neither the ones resulting of low-T processes nor the ones created by high-T FTT reactions [83, 84] (Figure S7). C10–C20  n-alkanes usually occur in equivalent amounts in petroleum or show a consistent decrease with molecular weight. Experimental FTT reactions produced consistent increasing concentrations from C9 to C12 and then consistent decreasing concentrations to C20. Similar patterns are also associated with the kerosene fraction of petroleum [85]. Distribution patterns in hydrothermal solids are difficult to picture as usually only chromatograms are provided in the studies, for example, [86], but they largely differ by the simple fact that <C14 alkanes were not detected in most cases as in sediments from various locations [87]. The smaller alkanes may well be preferentially entrained in fluid circulation but they are more likely the result of other processes, especially high-temperature ones, and including abiotic reactions. Note that the latter should not be reduced to sole FTT reactions because supercritical water is a fabulous medium for unconventional reactions [88–90].Formate and acetate have been given more attention in both laboratory [91–93] and field hydrothermal studies [28, 29] as these small molecules are likely to prevail according to thermodynamic studies (e.g., [31–33]). Where usually formate dominates, acetate was found to be more abundant in fluids from Fatu Kapa. According to Shock studies, at 280–300°C, formic acid concentrations should not be much higher than acetic acid, but this is not enough to explain our “reverse” concentrations. And especially it is not consistent with higher amounts in the 300°C fluids. A ratio close to 1 was observed at Kulo Lasi which may indicate that different production/consumption processes occur. Also the concentrations of the formate and acetate plotted on a line versus Mg which suggest that the fate of these volatile fatty acids at Kulo Lasi is controlled by simple mixing; that is there would be no consumption/production when fluid mixes with seawater (Figure 4). The deep-seawater concentrations were high compared to what is usually reported in the literature which was most likely due to plume contribution [27, 28]. This supports the simple mixing model hypothesis and is consistent with the near absence of organisms around those chimneys.


## 5.6. Organic Compounds: Implications for Biology, Mineral Resources, and C Cycling

The idea that life could have originated in hydrothermal systems from abiotic reactions was postulated in the late 70s [94]. However, the question of the origin of organic compounds in hydrothermal systems has remained ever since they were evidenced in natural environments [95]. On the one hand, a biogenic or thermogenic origin seems most likely for most compounds investigated so far; on the other hand, one cannot exclude that some of the formate and aliphatic hydrocarbons form abiotically [13, 26–28, 30, 96]. As detailed in the previous section, our results are consistent with a mix of origin although abiotic synthesis likely occurs to a far smaller extent than other processes that would overprint an abiotic signature.Upon the hot topic of the origin of life, the mere presence of organic compounds is highly important for the fauna at the local and regional scales. It is well established that VFAs constitute a significant food source for some microorganisms and thus help sustaining hydrothermal ecosystems [97–100]. Besides, some bacteria have proven to be capable of using naphthalene [101] and tubeworms, hydrocarbons [102].Organics can form complexes with metals [20, 21]. This greatly improves the dispersion of metals in the ocean and prevents them from precipitation as sulphides or oxyhydroxydes [23, 103]. Notably fatty acids are efficient ligands that play a major role in making metals bioavailable as well as in transporting them both through the upper crust ([17] and references therein) and through the water column in the plume [11, 104–106]. In addition, they have been shown to be involved in growth/dissolution processes of some minerals [19, 107]. For these reasons, they are of particular importance in ore-forming processes. Hydrocarbons which are weaker ligands would react with sulfates to generate bisulfide (HS−), which in turn would easily react with metal chlorides to form metal sulphides according to the following mass balance equations:(2)
3
S
O
4
2
-
+
3
H
+
+
4
R
–
C
H
3
⟶
4
R
–
C
O
2
H
+
H
S
-
+
4
H
2
O
(3)
H
S
-
+
M
e
C
l
2
⟶
M
e
S
+
H
+
+
2
C
l
-where R is a carbonated chain, either aliphatic or aromatic, and represents OM [108]. To that respect hydrocarbons are likely to be involved in depositional processes of metals. Notably associations of aliphatic and aromatic hydrocarbons with mineral deposits have also been observed on the EPR [109] and in sulphide sedimentary deposits on land [104].


## 5.7. Fluxes: Importance of Back-Arc Hydrothermal Systems to the Ocean Geochemistry

Hydrothermal input to the ocean via plumes has long been neglected but recent results of the GEOTRACES program clearly show its importance in terms of metals and trace elements transportation and implications for ocean biogeochemistry [13, 110–113]. While it is now well established that MOR hydrothermal discharge has a large impact on the global ocean chemistry and element cycles, the relative impact of hydrothermal activity from other hydrothermal settings has not been established. The extensive hydrothermal activity reported in the Wallis and Futuna region suggests that back-arc system hydrothermalism may be of much greater importance than previously anticipated [7, 114]. Estimation of hydrothermal fluxes is generally challenging and very few data are available in the literature [115–118]. Therefore we believe that any kind of estimation, even orders of magnitudes are of importance to make advances in this field. We propose to combine two different approaches based on geophysical data and video recordings (see here), respectively, to propose such estimates with some confidence.


### 5.7.1. Estimation Using Geophysics

We can make an order of magnitude estimate of the heat flux from the different hydrothermally active areas based on the physical characteristics of the plumes. Marshall and coworkers [119–121] have proposed a scaling relationship between the heat flux at an interface, Hf, the ambient buoyancy frequency (N) in the surroundings of the plume, the characteristic size (R
s) of the heat transfer region, and the equilibrium height (or depth; h) reached by the plume, as(4)
H
f
=
ρ
·
C
p
g
·
α
·
R
s
·
N
·
h
5
3
,where ρ is seawater density (1030 kg·m−3), C
p is heat capacity of seawater (~4000 J·kg−1·K−1), and g is gravitational acceleration (9.81 m·s−2), and α is the thermal expansion coefficient of seawater (10−4 K−1). The ambient buoyancy frequency (N) can be estimated to be between 0.001 and 0.002 s−1 from CTD profiles in the area using a routine in the UNESCO Sea Water Library described by Jackett and Mcdougall [122]. The radius (R
s) of the Kulo Lasi caldera is 2500 m and the plume rose in average about 200 m above seafloor (top layer boundary) [7]. For order of magnitude estimates, the ~130 km2 Fatu Kapa area can be approximated by a disk of radius 6400 m, with a similar plume height. Introducing these numbers in (4) leads to heat flux estimates ranging between 100 and 800 W·m−2 for the Kulo Lasi caldera and 50 and 400 W·m−2 for the Fatu Kapa area, which is greatly dependent on the value for buoyancy frequency. While these estimates scale proportionally with the area considered to be hydrothermally active, they integrate the sources within the area which do not demand that the whole area be active. We estimate that total heat inputs are in the 2–16 GW for the Kulo Lasi caldera and 5–40 GW for the Fatu Kapa areas.


### 5.7.2. Estimation Based on Video Postprocessing

Video recordings could be used to estimate fluid velocities of the Carla andO
b
e
l
X chimneys and of a few smokers at Kulo Lasi using for instance the Typhoon algorithm [123] (Figures S8–S11). This optical flow method recovers the (2D) fluid flow from the apparent displacements, in an image sequence, of tracers advected by the flow. Here, the plume acts as the tracer. Compensation for the camera and vehicle motion and parallax correction were not possible, so the investigated video sequences where chosen according to (i) the overall stability of the camera and vehicle and (ii) the plume being as perpendicular to the camera as possible. The relevant lengths scales (image spatial resolution and diameter of the chimneys) had to be estimated from known object sizes in the same ground, typically shrimps. External diameters of the chimney were used for calculation as any estimation of the internal diameter on video recordings would be too speculative. Note that (i) chimney samples taken at Kulo Lasi exhibited similar internal and external diameters; (ii) the large anhydrite chimneys (e.g., O
b
e
l
X, Carla) at Fatu Kapa did not seem to have any central conduit but rather exhibited a sponge-like structure leaking fluid at a high velocity from the entire volume. As a result, we believe the overestimation resulting from this assumption to be limited. Finally, the observed flow velocity is assumed to be constant across the jet section. Given all these limitations and assumptions, the resulting fluxes values should be taken as an indication of their order of magnitude.The fluid velocity was estimated to be on average 0.05, 0.15, and 1 m s−1 for Kulo Lasi, Carla, and O
b
e
l
X, respectively. In terms of heat fluxes, Carla (diameter ca. 70 cm) would generate ~6 MW while O
b
e
l
X (diameter ca. 250 cm) would produce ~5.7 GW, respectively. Associated mass fluxes would be 54 L s−1 and 5 m3 s−1 which means, for instance, that the single O
b
e
l
X chimney could generate an input of 2.6 × 107 mol y−1 CH4 to the ocean. Comparatively, estimation of the total efflux of methane from serpentinisation ranges from 15 to 84 × 109 mol y−1 including 9 × 109 mol y−1 for the sole slow spreading ridges. Similarly, the Carla chimney would release about 5.7 × 103 mol y−1 of dodecane that may help forming 1.4 mol y−1 of metal sulphides (see Section 5.6). Cumulative observations during the dives brought to a total of 220 smokers of various sizes (~5 cm to ~2.5 m in diameter) and apparent flows (strong, medium, slow). We assigned the strong, medium, and slow flows observed to the velocities of O
b
e
l
X, Carla, and Kulo Lasi, respectively. At Kulo Lasi about 100 smokers were counted during the Nautile dives and all appeared very similar in diameter (~3 cm) and fluid flow (0.05). Keeping in mind these uncertainties, an order of magnitude of the heat and mass fluxes generated by hot smokers at Fatu Kapa are estimated to be 6.8 GW and 6 m3 s−1 for the Fatu Kapa area versus 9 MW and 6 L s−1 for the Kulo Lasi caldera. This means, for example, that the total Fe flux from hot fluids emanating from the caldera would be up to 1.9 × 106 mol y−1 versus recent estimations of the global hydrothermal iron input that are about 109 mol y−1 [112, 124]. The average nonanoic acid concentration in Fatu Kapa purest fluids is 7.25 ppb, which would result in 1.4 × 106 mol y−1 released in the ocean by the Fatu Kapa hot smokers. The carboxylic acid functional group of fatty acids makes them good potential ligands to form coordination complexes with iron, which stabilises iron in the plume in its reduced form [103, 125]. Hence, the example of nonanoic acid suggests that fatty acids could largely contribute to iron stabilisation.However, the high-temperature fluxes calculated above failed to include heat fluxes from diffusive venting, which was largely present in both areas and is thought to be an important part of the global hydrothermal heat flux (up to 98%) [126]. The surface of the diffusive areas was also assessed on the videos. However, because the velocity of diffusive fluids could not be estimated using Typhoon, we assumed hydrothermal waters are exiting the seafloor at the minimum velocity reported for low temperature flow (0.04 m s−1) [127]. The cumulative surface of diffusive areas with a typical temperature of 10°C reached 100 m2 at Kulo Lasi and 2885 m2 at Fatu Kapa. In addition, a particular area of about 300 m2 at Kulo Lasi consisted in hundreds of silica chimney diffusing a 40°C fluid [6]. The resulting contribution of diffuse venting to the heat flux would be 2.14 GW and 5.3 GW at Kulo Lasi and Fatu Kapa, respectively. This brings the total heat flux estimates at 2.15 GW and 12 GW, respectively, which is consistent with the estimates obtained using the lower N value as well as the fact that only a small portion of the total surface of the sites was explored with the submersible.


### 5.7.3. Summary

According to these different estimates heat efflux at Kulo Lasi and Fatu Kapa are conservatively estimated to be at least for 1-2 GW and 5–10 GW, respectively; this estimate is based on the lowN value, whereas using the higher N suggests a flux almost 10x higher. It seems highly likely that the Wallis and Futuna active areas combined with the 3 calderas to the East [114] have a heat flux of >10 GW. Vent fields on MOR have been reported to generate between 10 MW and 25 GW ([116, 117, 127, 128] and references therein) and the total hydrothermal heat flux at MORs is estimated to be about 1000 GW [129, 130]. This suggests that the presently discovered area might be of significant importance in the global budget and that back-arc hydrothermal activity contributes as much as MOR systems, and, possibly more, to the global ocean chemistry and cycles. Few estimates of hydrothermal heat flux have been published and the relative importance of heat, fluid, and geochemical hydrothermal fluxes from different environments will require studies designed to more accurately gauge these fluxes.


## 5.7.1. Estimation Using Geophysics

We can make an order of magnitude estimate of the heat flux from the different hydrothermally active areas based on the physical characteristics of the plumes. Marshall and coworkers [119–121] have proposed a scaling relationship between the heat flux at an interface, Hf, the ambient buoyancy frequency (N) in the surroundings of the plume, the characteristic size (R
s) of the heat transfer region, and the equilibrium height (or depth; h) reached by the plume, as(4)
H
f
=
ρ
·
C
p
g
·
α
·
R
s
·
N
·
h
5
3
,where ρ is seawater density (1030 kg·m−3), C
p is heat capacity of seawater (~4000 J·kg−1·K−1), and g is gravitational acceleration (9.81 m·s−2), and α is the thermal expansion coefficient of seawater (10−4 K−1). The ambient buoyancy frequency (N) can be estimated to be between 0.001 and 0.002 s−1 from CTD profiles in the area using a routine in the UNESCO Sea Water Library described by Jackett and Mcdougall [122]. The radius (R
s) of the Kulo Lasi caldera is 2500 m and the plume rose in average about 200 m above seafloor (top layer boundary) [7]. For order of magnitude estimates, the ~130 km2 Fatu Kapa area can be approximated by a disk of radius 6400 m, with a similar plume height. Introducing these numbers in (4) leads to heat flux estimates ranging between 100 and 800 W·m−2 for the Kulo Lasi caldera and 50 and 400 W·m−2 for the Fatu Kapa area, which is greatly dependent on the value for buoyancy frequency. While these estimates scale proportionally with the area considered to be hydrothermally active, they integrate the sources within the area which do not demand that the whole area be active. We estimate that total heat inputs are in the 2–16 GW for the Kulo Lasi caldera and 5–40 GW for the Fatu Kapa areas.


## 5.7.2. Estimation Based on Video Postprocessing

Video recordings could be used to estimate fluid velocities of the Carla andO
b
e
l
X chimneys and of a few smokers at Kulo Lasi using for instance the Typhoon algorithm [123] (Figures S8–S11). This optical flow method recovers the (2D) fluid flow from the apparent displacements, in an image sequence, of tracers advected by the flow. Here, the plume acts as the tracer. Compensation for the camera and vehicle motion and parallax correction were not possible, so the investigated video sequences where chosen according to (i) the overall stability of the camera and vehicle and (ii) the plume being as perpendicular to the camera as possible. The relevant lengths scales (image spatial resolution and diameter of the chimneys) had to be estimated from known object sizes in the same ground, typically shrimps. External diameters of the chimney were used for calculation as any estimation of the internal diameter on video recordings would be too speculative. Note that (i) chimney samples taken at Kulo Lasi exhibited similar internal and external diameters; (ii) the large anhydrite chimneys (e.g., O
b
e
l
X, Carla) at Fatu Kapa did not seem to have any central conduit but rather exhibited a sponge-like structure leaking fluid at a high velocity from the entire volume. As a result, we believe the overestimation resulting from this assumption to be limited. Finally, the observed flow velocity is assumed to be constant across the jet section. Given all these limitations and assumptions, the resulting fluxes values should be taken as an indication of their order of magnitude.The fluid velocity was estimated to be on average 0.05, 0.15, and 1 m s−1 for Kulo Lasi, Carla, and O
b
e
l
X, respectively. In terms of heat fluxes, Carla (diameter ca. 70 cm) would generate ~6 MW while O
b
e
l
X (diameter ca. 250 cm) would produce ~5.7 GW, respectively. Associated mass fluxes would be 54 L s−1 and 5 m3 s−1 which means, for instance, that the single O
b
e
l
X chimney could generate an input of 2.6 × 107 mol y−1 CH4 to the ocean. Comparatively, estimation of the total efflux of methane from serpentinisation ranges from 15 to 84 × 109 mol y−1 including 9 × 109 mol y−1 for the sole slow spreading ridges. Similarly, the Carla chimney would release about 5.7 × 103 mol y−1 of dodecane that may help forming 1.4 mol y−1 of metal sulphides (see Section 5.6). Cumulative observations during the dives brought to a total of 220 smokers of various sizes (~5 cm to ~2.5 m in diameter) and apparent flows (strong, medium, slow). We assigned the strong, medium, and slow flows observed to the velocities of O
b
e
l
X, Carla, and Kulo Lasi, respectively. At Kulo Lasi about 100 smokers were counted during the Nautile dives and all appeared very similar in diameter (~3 cm) and fluid flow (0.05). Keeping in mind these uncertainties, an order of magnitude of the heat and mass fluxes generated by hot smokers at Fatu Kapa are estimated to be 6.8 GW and 6 m3 s−1 for the Fatu Kapa area versus 9 MW and 6 L s−1 for the Kulo Lasi caldera. This means, for example, that the total Fe flux from hot fluids emanating from the caldera would be up to 1.9 × 106 mol y−1 versus recent estimations of the global hydrothermal iron input that are about 109 mol y−1 [112, 124]. The average nonanoic acid concentration in Fatu Kapa purest fluids is 7.25 ppb, which would result in 1.4 × 106 mol y−1 released in the ocean by the Fatu Kapa hot smokers. The carboxylic acid functional group of fatty acids makes them good potential ligands to form coordination complexes with iron, which stabilises iron in the plume in its reduced form [103, 125]. Hence, the example of nonanoic acid suggests that fatty acids could largely contribute to iron stabilisation.However, the high-temperature fluxes calculated above failed to include heat fluxes from diffusive venting, which was largely present in both areas and is thought to be an important part of the global hydrothermal heat flux (up to 98%) [126]. The surface of the diffusive areas was also assessed on the videos. However, because the velocity of diffusive fluids could not be estimated using Typhoon, we assumed hydrothermal waters are exiting the seafloor at the minimum velocity reported for low temperature flow (0.04 m s−1) [127]. The cumulative surface of diffusive areas with a typical temperature of 10°C reached 100 m2 at Kulo Lasi and 2885 m2 at Fatu Kapa. In addition, a particular area of about 300 m2 at Kulo Lasi consisted in hundreds of silica chimney diffusing a 40°C fluid [6]. The resulting contribution of diffuse venting to the heat flux would be 2.14 GW and 5.3 GW at Kulo Lasi and Fatu Kapa, respectively. This brings the total heat flux estimates at 2.15 GW and 12 GW, respectively, which is consistent with the estimates obtained using the lower N value as well as the fact that only a small portion of the total surface of the sites was explored with the submersible.


## 5.7.3. Summary

According to these different estimates heat efflux at Kulo Lasi and Fatu Kapa are conservatively estimated to be at least for 1-2 GW and 5–10 GW, respectively; this estimate is based on the lowN value, whereas using the higher N suggests a flux almost 10x higher. It seems highly likely that the Wallis and Futuna active areas combined with the 3 calderas to the East [114] have a heat flux of >10 GW. Vent fields on MOR have been reported to generate between 10 MW and 25 GW ([116, 117, 127, 128] and references therein) and the total hydrothermal heat flux at MORs is estimated to be about 1000 GW [129, 130]. This suggests that the presently discovered area might be of significant importance in the global budget and that back-arc hydrothermal activity contributes as much as MOR systems, and, possibly more, to the global ocean chemistry and cycles. Few estimates of hydrothermal heat flux have been published and the relative importance of heat, fluid, and geochemical hydrothermal fluxes from different environments will require studies designed to more accurately gauge these fluxes.


## 6. Concluding Remarks

The study of the geochemical characteristics of hydrothermal fluids from the Wallis and Futuna area confirmed the great potential of the region to generate a variety of fluid chemistries, as it was expected considering its particular geological context. This supports the idea that the hydrothermal contribution of back-arc environments is of great interest for the global ocean chemistry. Our order of magnitude estimates of fluxes suggest that back-arc hydrothermal activity contributes as much as MOR systems and possibly more. Notably the soleO
b
e
l
X chimney could generate ~1‰ of the total hydrothermally derived CH4. The diversity observed in the Wallis and Futuna area also emphasizes that each new field presents its own characteristics and that exploration should continue. A huge number of sites remain to be discovered according to the newly published estimation of vent fields occurring on Earth [131].A special focus was brought on organic geochemistry because of the few data available in modern hydrothermal systems despite the recent growing interest for oceanic OM. Concentrations of SVOCs are the first to be reported which will have implications in a wide range of questions and fields. Our results are relevant to the understanding of C cycling and complete the works by Hawkes and Rossel who demonstrated that DOM is recycled if not removed partially through hydrothermal systems but who could not identify compounds in DOM. Identification of organic molecules is especially needed to better understand organometallic chemistry at hydrothermal vents and thus utilisation by microbes, metal export, and ore-forming processes. The distribution patterns obtained revealed the occurrence of several processes controlling organic geochemistry and notably that one cannot exclude abiotic synthesis to occur in the study area but very likely to a so small extent that the signature would be overprinted.This brings the idea that using natural concentrations to feed thermodynamic models of abiotic synthesis and/or guide the design of experimental work should enable making progress in unravelling the origin of organic compounds in hydrothermal systems. In addition, growing techniques as clumped isotopes [132] and position specific isotopes measurements [133] are available and should also help answering this question.



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*Source: 7692839-2018-03-11.xml*