Gas hydrates of nonpressurized (GC) and pressurized (DAPC) sediment cores from the Hakon Mosby Mud Volcano, SW Barents Sea

• Main Authors: Pape, Thomas, Feseker, Tomas, Kasten, Sabine, Fischer, David, Bohrmann, Gerhard
• Format: Dataset
• Language: English
• Published: PANGAEA 2011
• Subjects: ARK-XXII/1b; Center for Marine Environmental Sciences; GC; Gravity corer; HERMES; Hotspot Ecosystem Research on the Margins of European Seas; MARUM; Norwegian Sea; PC; Piston corer; Polarstern; PS70; PS70/053-1; PS70/054-1; PS70/068-1; PS70/069-1; PS70/081-1; PS70/092-1; PS70/093-1; PS70/094-1; PS70/097-1; PS70/098-1; PS70/102-1; PS70/110-1; PS70/113-1; PS70/117-1; PS70/122-1; PS70/126-1; PS70/133-1; Barents Sea
• Online Access: https://doi.pangaea.de/10.1594/PANGAEA.770365; https://doi.org/10.1594/PANGAEA.770365

The occurrence of gas hydrates at submarine mud volcanoes (MVs) located within the gas hydrate stability zone (GHSZ) is controlled by upward fluid and heat flux associated with MV activity. Determining the spatial distribution of gas hydrates at MVs is crucial to evaluate their sensitivity to known episodic changes in volcanic activity. We determined the hydrocarbon inventory and spatial distribution of hydrates at an individual MV structure. The Håkon Mosby Mud Volcano (HMMV), located at 1,250 m water depth on the Barents Sea slope, was investigated by combined pressure core sampling, heat flow measurements, and pore water chemical analysis. Quantitative pressure core degassing revealed gas-sediment ratios between 3.1 and 25.7, corresponding to hydrate concentrations of up to 21.3% of the pore volume. Hydrocarbon compositions and physicochemical conditions imply that gas hydrates incipiently crystallize as structure I hydrate, with a dissociation temperature of around 13.8°C at this water depth. Based on numerous in situ measurements of the geothermal gradient in the seabed, pore water sulfate profiles and microbathymetric data, we show that the thickness of the GHSZ increases from less than 1 m at the warm center to around 47 m in the outer parts of the HMMV. We estimate the total mass of hydrate-bound methane stored at the HMMV to be about 102.5 kt, of which 2.8 kt are located within the morphological Unit I around the center and thus are likely to be dissociated in the course of a large eruption.