Influences of the Tonga Subduction Zone on seafloor massive sulfide deposits along the Eastern Lau Spreading Center and Valu Fa Ridge

Evans, Guy N.; Tivey, Margaret K.; Seewald, Jeffrey S.; Wheat, C. G.

doi:10.1016/j.gca.2017.08.010

Cited by 11 publications

(4 citation statements)

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“…Pyrrhotite has previously been found in trace amounts in chimneys on Brothers volcano (Berkenbosch et al , 2012). Pyrrhotite and isocubanite (cubic cubanite) were recently described in chimneys from the Kilo Moana vent field in the Lau Basin (Evans et al , 2017. Pyrrhotite and isocubanite are indicative of more reducing conditions than pyrite and chalcopyrite.…”

Section: Atypical Composition Of Hydrothermal Mineralization For a Bamentioning

confidence: 94%

“…The low pH may also be explained by subsurface deposition of Cu and Fe sulfides. Petrographic and geochemical data for the sulfide deposits clearly supports formation from reduced fluids (pyrrhotite), and the presence of significant silica, low Cu, and abundant Zn suggests moderate to high fluid pH(Evans et al , 2017). Loss of sulfate and calcium from subsurface deposition of anhydrite can also occur.As a result, the fluid is hot, enriched in H 2 , and may have a low pH.…”

mentioning

confidence: 89%

“…, in the Lau Basin (Baker et al , 2010, Bertine and Keene, 1975, Evans et al , 2017, Fouquet et al , 1991, Hawkins et al , 1986., Herzig et al , 1998, Kim et al , 2009, Lisitsyn et al , 1992, Lupton et al , 2009, Von Stackelberg, 1988)}, in the North Fiji Basin (Auzende et al , 1995, Bendel et al , 1993, Halbach et al , 2001, in the Manus Basin (e.g., (Auzende et al , 1996, Bach et al , 2007, Binns and Scott, 1993, Both et al , 1986, Gamo et al , 1997, Gemmell et al , 1999, Gena et al , 2001, Kim et al , 2004, Lisitsyn et al , 1993, Moss and Scott, 2001, in the Mariana basin (e.g., (Baker et al , 2008, de Ronde et al , 2014a, Hein et al , 2014, Ishibashi et al , 2006 and in the Okinawa basin (Glasby, 2008, Halbach et al , 1989, Halbach and Pracejus, 1993, Hou et al , 2005, Iizasa et al , 1992, Kimura et al , 1988, Noguchi et al , 2007.…”

mentioning

confidence: 99%

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Volcanic and hydrothermal processes in submarine calderas: The Kulo Lasi example (SW Pacific)

Fouquet

Pelleter

Konn

et al. 2018

Ore Geology Reviews

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The study area is located at the transition between the northern end of the Tonga Trench and the North Fiji fracture zone, where tectonic movements are reputed to be the fastest in the world. To the southeast of Futuna Island, a broad area of volcanism occurs within a region characterized by a change in the tectonic fabric between a NE-SW oriented volcanic graben and the N-S oriented Alofi ridge. In 2010, the active volcano Kulo Lasi, which represents the most recent volcanic episode in the Futuna area, was discovered in the center of this extensive volcanic zone. Kulo Lasi is a 20 km diameter shield volcano that rises 400 m above the seafloor. It is composed of basaltic to trachy-andesitic lava with no obvious geochemical affinity with the Tonga subduction that occurs 500 km to the east. The central caldera is 5 km in diameter and 300 m deep and is located at a water depth of 1500 m. Diving operations with the submersible Nautile and high-resolution AUV mapping, have revealed the presence of numerous active and inactive hydrothermal fields on the floor and the walls of the caldera. Four tectono-volcanic stages can be distinguished at Kulo Lasi caldera. In stage 1, the shield volcano is built. Annular reverse faults develop at the summit and control circulation of water/rock-dominated hydrothermal fluids and hightemperature alteration of rocks along the nascent normal faults. Mixing of hydrothermal fluids with seawater is favored along normal superficial faults, leading to the formation of low-temperature Fe/Mn mineralization at the summit of the volcano. During stage 2, the caldera collapse, gradually revealing outcrops of the altered and mineralized zones formed during Stage 1. As the magma chamber cools and collapses, less heat is available. As a result, medium to low-temperature (<100 °C) Fe/Si deposits form on the floor of the caldera. In stage 3, refilling and ascent of the magma chamber at depth promote the uplift of a central resurgent dome devoid of recent lava emission. The depth of the magma chamber under the dome is estimated to be 1.6 km. Annular dykes feeding the new lava flows are controlled by the deep reverse faults at the outer rim of the caldera floor. The eruptive events are accompanied by short-lived emission of magmatic fluids, rich in SO2, materialized by the presence of native sulfur depositions on the surface of the most recent lava flows. During stage 4 (present day), black smoker sulfide chimneys, controlled by the deep reverse faults, form at the surface of the most recent lava flows at the outer part of the caldera floor. The fluids emitted result from the mixing of a deep fluid of the water/rock reaction type and of shallow seawater superheated in contact with the hot dykes. Hydrogen is generated during reaction of seawater with the hot dikes and H2 is enriched in the mixed fluids. Active (43°C) siliceous chimneys at the base of the caldera walls and low-temperature vents (6°C) perched on Please note that this is an author-produced PDF of an article accepted for publication following...

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Section: Atypical Composition Of Hydrothermal Mineralization For a Bamentioning

confidence: 94%

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confidence: 89%

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confidence: 99%

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Volcanic and hydrothermal processes in submarine calderas: The Kulo Lasi example (SW Pacific)

Fouquet

Pelleter

Konn

et al. 2018

Ore Geology Reviews

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“…Samples were collected from different vent sites spanning from the northern trough to the southern ridge of the ELSC using IGT samplers deployed by ROV Jason II during R/V Roger Revelle cruise RR1507 in April-May 2015. While some data on the chemistry of vent fluids from the ELSC collected on other cruises have been reported (Takai et al, 2008;Mottl et al, 2011;Evans et al, 2017), the full fluid chemistry for the samples used in this study is reported in Seewald (2017).…”

Section: Geologic Settings and Sample Collectionmentioning

confidence: 99%

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The Production and Fate of Nitrogen Species in Deep-Sea Hydrothermal Environments

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Indeed, I have come so far from when I first approached him in the summer of 2012. For all that, and much more, I am truly grateful.Jeff Seewald is another person with whom I have worked very closely with through the course of this thesis. I have thoroughly enjoyed my time in his lab. Jeff spent a lot of time teaching me how to set up high-temperature, high-pressure experiments and very patiently coached me the optimized techniques and systems for sampling. In addition, he has been 'a fountain of optimism' through long hours in the lab.I would also like to thank the other members of my thesis committee: Stefan Sievert and Shuhei Ono. Stefan played an instrumental role in getting me on the 9°50'N East Pacific Rise cruise in 2017, and provided insights into the microbial dynamics at Crab Spa (yes, it is spelled correctly this time). Shuhei was always enthusiastic to hear about my thesis progress, and offered valuable advice and encouragements during our meetings. I am also indebted to Frieder Klein who not only chaired both my thesis proposal and defense, but also went above and beyond, providing suggestions to this final draft.This thesis would not have come to fruition without the expert technical assistance of Sean Sylva, whose incredible patience and recommendations helped troubleshoot both the bomb setup and instruments used for my work in the Seewald Lab. Labmates from the first summer when I first started my experiments, Niya Grozeva and Justin Snook, both provided tremendous assistance, shared neatly-kept notes, and most importantly, offered lab companionship. I am also thankful to Zoe Sandwith, who kept the IRMS in the Wankel Lab humming, dealt with leaks in the Valco valve, did the argon sniffing, and took care many other issues that would have taken much longer to fix without her help.I have benefited greatly from the body of works carried out by many colleagues. Archived samples from the Seewald Lab, which were the main part of Chapter 3, were collected during numerous cruises before I entered the Joint Program. Many of these were collected with the help of Eoghan Reeves and Jill McDermott, both former advisees of Jeff's. They have been very generous in providing sample data and insights that were instrumental to my work. Annie Bourbonnais, Marv Lilley, and Dave Butterfield generously shared their Juan de Fuca Ridge sample data, which also made up a sizeable part of the compilation. Tina Lin and Mike Rappe provided crustal fluid samples, which became great complements to the Juan de Fuca discussions. Jesse McNichol's thesis work on Crab Spa incubations laid the groundwork for development of Chapter 4 of this thesis.The world-class education I had received for my PhD would not happened without the highly acclaimed field experts at WHOI and MIT. Moreover, the Academic Programs Office had been a propelling force behind the scene. I would like to specifically thank Meg Tivey, Jim Yoder, Julia Westwater, Lea Fraser, and Christine Charette. I am also indebted to John Farrington who, despite not being the Dean...

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Mineralogy and geochemistry of hydrothermal sulphide from a submarine volcanic high at 18°36.4′S Central Lau Spreading Center, Southwest Pacific

Ray

Paropkari

2023

Acta Oceanol. Sin.

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Influences of the Tonga Subduction Zone on seafloor massive sulfide deposits along the Eastern Lau Spreading Center and Valu Fa Ridge

Cited by 11 publications

References 64 publications

Volcanic and hydrothermal processes in submarine calderas: The Kulo Lasi example (SW Pacific)

Volcanic and hydrothermal processes in submarine calderas: The Kulo Lasi example (SW Pacific)

Untitled

Mineralogy and geochemistry of hydrothermal sulphide from a submarine volcanic high at 18°36.4′S Central Lau Spreading Center, Southwest Pacific

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