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Flat-Topped Mounds in Western Ross Sea: Carbonate Mounds Or Subglacial Volcanic Features?

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Flat-Topped Mounds in Western Ross Sea: Carbonate Mounds Or Subglacial Volcanic Features? Flat-topped mounds in western Ross Sea: Carbonate mounds or subglacial volcanic features? L. Lawver1, J. Lee2, Y. Kim2, and F. Davey3 1University of Texas at Austin, Institute for Geophysics, Jackson School of Geoscience, 10100 Burnet Road, R2200, Austin, Texas 78758, USA 2Korea Polar Research Institute (KOPRI), Unit of New Antarctic Station, Get-pearl Tower, 12 Gaetbeol-ro, Yeonsoo-Gu, Incheon, 406-840, Korea 3GNS Science, P.O. Box 30368, Lower Hutt, 5040, New Zealand ABSTRACT up to 14 km thick and documents an extension- the surface. They also identify a pockmark close rifting history that may extend back as far as to the mounds cluster and overlying their BSR Detailed multibeam bathymetry data in the the Cretaceous (Davey et al., 1983; Cooper region. Lawver et al. (2007) report the presence western Ross Sea, Antarctica, delineate a fi eld et al., 1987). The major extension of the basin of an extensive fi eld of pockmarks lying to the of unusual fl at-topped seafl oor mounds located probably occurred only since the late Eocene east and northeast of the mounds and extending ~50 km west of Franklin Island and an arcuate (~38 Ma; De Santis et al., 2001; Davey et al., from the Lee Arch to Franklin Island at depths zone of pockmarks to the northwest and west 2006). The most recent extensional deformation of 450–500 m (Fig. 1). The presence of natural of Franklin Island. Sixteen mounds occur in an has focused on the central part of the basin (Lee gas in the subsurface has been associated with area about 30 km square at a depth of ~500 m, Arch and Discovery Graben of the Terror Rift, roughly circular depressions in the seafl oor— within the Terror Rift, the active extensional Cooper et al., 1987) where major faulting and pockmarks—where natural gas has apparently part of the Victoria Land Basin. The mounds volcanism still occur (Cooper et al., 1987; Hall escaped (King and Maclean, 1970; Hovland, tend to be circular in the east and linear in the et al., 2007). Extensive volcanism continues 1981; Hovland and Judd, 1988), and these have west, with their steepest slope to the southeast, along the axis of the Victoria Land Basin, from been found in many regions globally (e.g., Judd and shallowest slope to the northwest, consis- Ross Island to Mount Melbourne (Fig. 1), where and Hovland, 2007; Pilcher and Argent, 2007). tent with erosion by northwest ice-sheet move- recent subice volcanism has occurred at Shield These pockmarks are inferred to result from ment. The largest mound is ~4 km across and Nunatak (Wörner and Viereck, 1987). Franklin the expulsion of sub-seafl oor gas occurrences 100 m high. Five similar features were delin- Island, a recently active volcanic center (Arm- associated with the phase change from hydrate eated to the south and east of Franklin Island strong, 1978; Rilling et al., 2009), lies along a to free gas, and support the existence of exten- at depths of 400–650 m. Seismic, gravity, volcanic ridge under the eastern part of Victoria sive gas in the sedimentary section, as found and magnetic data indicate that the mounds Land Basin that is imaged on aeromagnetic data on the Ross Shelf by Deep Sea Drilling Leg 28 are largely low-density , nonmagnetic bodies (Chiappini et al., 1999). Numerous, additional (McIver, 1972). These results suggest an alter- overlying a largely nondisrupted sedimentary small, young volcanic centers lie in this region. nate interpretation for the mounds—that they section, but some mounds have an associated Lawver et al. (2007) documented a group of are carbonate mounds (Lawver et al., 2008), small (~50 nT), short-wavelength, normal or low, fl at-topped mounds in a restricted region similar to those seen in the Porcupine Bight off reversed magnetic anomaly, indicating a mag- of the Lee Arch to the west of Franklin Island. northwest Europe (Shannon et al., 2007). netic core to the mounds. Their proximity to They speculated that they may be caused by New multibeam bathymetry, gravity, and inferred subsurface gas hydrates suggests they subglacial eruptions, similar to those that occur geomagnetic data over the mound and pock- may be carbonate banks, but they also occur in Iceland, and give rise to low-density and mag- mark fi elds have been integrated with existing close to volcanic centers including Franklin netized hyloclastite rocks, because the magnetic geophysical data to defi ne their characteristics Island. Our preferred interpretation is that anomalies are subdued over the features. The and extent in more detail and examine their they are of volcanic origin, erupted during a mound fi eld lies at an offset (accommodation cause. We present gravity and magnetic models geomagnetic reversal and under a grounded zone) in the Terror Rift (Salvini et al., 1997). of some of the mounds, indicating the low ice sheet forming hyaloclastite edifi ces, previ- Detailed analyses of multichannel seismic density and some localized magnetization of ously unknown under the Ross Sea. The pock- data across the region west of the mounds by the mounds. marks range from 200 m to 500 m in diameter. Geletti and Busetti (2011) have delineated bot- tom simulating refl ectors (BSRs) and sub-BSRs METHODS INTRODUCTION that they infer are caused by gas hydrates. They document a mound over a fault that they sug- The new data were recorded across part of the The southern part of the western Ross Sea gest is caused by the fault releasing pressure on southern part of mound fi eld and to the south (Fig. 1) coincides with a major rift basin, the the gas hydrates, allowing free gas to form and and east of Franklin Island by RVIB Araon using Victoria Land Basin, which contains sediments rise up the fault zone to form a mud volcano at a Kongsberg Simrad EM122 multibeam echo- Geosphere; June 2012; v. 8; no. 3; p. 645–653; doi:10.1130/GES00766.1; 7 fi gures. Received 15 November 2011 ♦ Revision received 26 February 2012 ♦ Accepted 7 March 2012 ♦ Published online 17 May 2012 For permission to copy, contact [email protected] 645 © 2012 Geological Society of America Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/8/3/645/3341751/645.pdf by guest on 30 September 2021 Lawver et al. sounder in February 2011. Seawater velocity- depth profi les were recorded at three stations using an Applied Microsystems SV Plus V2 sound-velocity probe lowered to the seafl oor. A Micro-g LaCoste Air-Sea System II gravity meter system was used for gravity recordings Mt Melbourne with base ties at Lyttleton, New Zealand, at the start and the end of survey. Instrument drift was low (0.5 mGal over 30 days), and an accuracy DG of 1 mGal is estimated in good sea conditions. LA A Bartington Instruments Ltd. Mag-03M three- component fl uxgate magnetometer was installed 3 TR on the ship’s mast for three-component mag- netic data. These magnetic data were processed using the methods of Korenaga (1995), but only 1 4 a limited data set was recovered. The multibeam LA data were integrated with existing multibeam data recorded by RVIB Nathanial B. Palmer Franklin Island (NBP9602, NBP9702, NBP0301, NBP0302, TR NBP0401, and NBP0701 data obtained via 2 GeoMapApp) (Figs. 2–5). The new potential fi eld data and those from NBP0401 have been used for modeling. DG DATA: MOUNDS Beaufort Island The new data extend the area of the fi eld of Transantarctic Mountains unusual fl at-topped seafl oor mounds located west of Franklin Island by ~6 km to the south- west. An additional nine mounds have been Ross Island S delineated. The total fi eld lies ~20 km north- E west of a major volcanic ridge (Fig. 2, Davey Bank) and covers an area about 30 km square at 1200 a depth of ~500 m (Fig. 3). The largest mound is ~4 km across and 100 m high (Fig. 3). The Figure 1. Western Ross Sea region (red box on inset National Aeronautics and Space mounds are generally circular in the east and lin- Administration image of Antarctica). Bathymetry, 100-m intervals after Davey (2004), ear in the west (Fig. 3), have a northerly trend masked at western limit of marine data. Thick orange-dashed lines show extent of the to their distribution, and are probably fault con- Victoria Land Basin. Thick, solid yellow lines show location of the Terror Rift (T R) com- trolled. The southeast fl anks of the mounds have prising the Discovery Graben (DG) and Lee Arch (LA) (Cooper et al., 1987). Red-outlined the steepest slope, with the shallowest slope to boxes denote: 1—mounds region (Fig. 2); 2—Franklin Island region mounds (Fig. 4); the northwest, consistent with emplacement of 3—northern pockmark region (Fig. 5B); and 4—southern pockmark region (Fig. 5A). relatively unconsolidated deposits under a north- Mounds Davey Bank Figure 2. Three-dimensional view of western mounds and Davey Bank from the northeast. Figure 3 Location is red-outlined box 1 in Figure 1. The extent of Figure 3 76.2°S is shown by the thin black line. Vertical exaggeration ~35:1. 76.0°S 165.5°E 166.0°E 75.8°S 166.5°E Depth (m) 646 Geosphere, June 2012 Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/8/3/645/3341751/645.pdf by guest on 30 September 2021 Ross Sea volcanic mounds west-moving ice sheet or possibly by northwest- 165°30′ 165°40′ 165°50′ 166°00′ 166°10′ trending seafl oor currents. Schopka et al.
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