Drowned carbonate platforms in the Bismarck Sea, Papua New Guinea
- First Online:
- Cite this article as:
- Hoffmann, G., Silver, E., Day, S. et al. Mar Geophys Res (2009) 30: 229. doi:10.1007/s11001-010-9079-8
- 319 Views
Extinct volcanic islands in the Bismarck volcanic arc are fringed by well-developed coral reefs. Drowned platforms offshore from these islands provide evidence for subsidence in the central section of the arc, north of the Finisterre Terrane–Australia collision. Bathymetric and backscatter data collected onboard the R/V Kilo Moana in 2004 reveal regularly spaced (~200 m interval) drowned platforms at depths as much as 1,100 m below sea level. However, the adjacent mainland coast has well documented raised terraces indicating long-term uplift. Local subsidence may be due to cessation of magmatic activity and cooling, flexural loading by the uplifting Finisterre Range, loading by nearby active volcanic islands, and/or sediment loading on the seafloor north of the Finisterre Range. We present some simple models in order to test whether flexural loading can account for local subsidence. We find that volcanic and sedimentary loading can explain the inferred relative subsidence.
KeywordsDrowned carbonate platformsPapua New GuineaFlexural modelingSidescan sonar
The creation of submerged carbonate platforms requires a rare combination of relatively rapid subsidence and rapid sea-level rise (Darwin 1897; Campbell 1984). Such platforms have been observed around the Hawaiian Islands (Moore and Campbell 1987; Grigg et al. 2002), in the Solomon Sea, Papua New Guinea (Davies et al. 1987a; Galewsky et al. 1996; Webster et al. 2004), in New Zealand (Stern and Holt 1994), and elsewhere. Subsidence in Hawaii was caused primarily by flexural volcanic loading (Campbell 1984), with the platforms tilting landward towards the locus of loading (Moore and Campbell 1987). In the Solomon Sea, however, subsidence was due to flexural loading of the subducting Australian plate by the overriding South Bismarck Plate, resulting in seaward tilting (Davies et al. 1987b; Abbott et al. 1994; Galewsky et al. 1996; Galewsky 1998; Wallace et al. 2004; Webster et al. 2004).
We present observations of submerged platforms around volcanic islands in the Bismarck Volcanic Arc. Unlike the Hawaiian and Solomon Sea submerged platforms, these newly observed platforms are found in an arc volcanic environment on the overriding tectonic plate. In the Bismarck Volcanic Arc, there are several possible causes of subsidence: (1) flexural loading by nearby active arc volcanoes, (2) flexural loading by accumulated sediment deposition, and (3) fore-arc flexural subsidence caused by uplift of the overriding Bismarck Sea plate, the mirror image of the flexural bulge on the lower plate.
We present a series of models for the submerged platforms around Bagabag Island, covering a range of possible elastic thicknesses, including volcanic loading, sedimentary loading, and buoyant uplift loading. We find that loading by nearby volcanic islands in combination with relatively high sedimentation rates adequately explains the magnitude of relative subsidence required to create the submerged platforms.
Hawaiian drowned platforms
Campbell (1984) reported two submerged carbonate platforms on the Kohala Terrace to the northwest of Hawaii based on bottom photography, SeaMARC II sidescan and bathymetry, seismic reflection profiles, and bottom samples. In profile, the reefs were observed to have a shallow, wide bulge at the rim of the terrace. Campbell reported that the reefs formed in situ in shallow water. Jones (1995) provided an age estimate for the 1,000 m deep reef of ~250 ka based on Electron Spin Resonance measurements of samples collected from the reef.
Jones (1995) expanded on Campbell’s (1984) model of platform-drowning on the flanks of volcanoes. First, as the volcano is building and subsiding due to flexural loading of the underlying lithosphere, shallow-water reefs can grow offshore of a relatively stable shoreline during periods of glacial accumulation and sea-level fall. During rapid sea-level rise in a subsequent interglacial period, the carbonate platforms can be submerged to sufficient depths such that reef-growth ceases. This process repeats itself when reef growth continues upslope during a later glacial maximum. Thus, as the volcano grows and subsides over time, a series of drowned reef platforms can form on its flanks.
Huon Gulf, Papua New Guinea
Volcanic terraces and flat-topped cones
Submarine terraces can also form on the flanks of volcanoes by purely volcanic processes. Geist et al. (2008) described a series of terraces on the Galapagos platform up to 3,500 m deep. The escarpments surrounding the terraces are ~300 m high on average, with slopes of ~24°. Based on sidescan imagery and dredges, they reported that the terraces are composed of basalt. These terraces appear scalloped in morphology, unlike the more continuous edges of the Huon Gulf terraces.
In the vicinity of Hawaii, basaltic flat-topped volcanic cones have been imaged and sampled (Clague et al. 2000). These cones occur near submarine rift zones, and are similar to flat-topped cones found near mid-ocean ridges, such as those shown by Fornari and Campbell (1987). The basal diameter of flat-topped cones can be as large as 8 km, although the mean diameter is ~3 km. They can be several hundred meters high, often with a broad, shallow rim that can make them appear morphologically similar to reef systems. However, flat-topped cones are not multi-tiered, as are many drowned reef structures.
Bismarck Volcanic Arc, Papua New Guinea
The Bismarck Volcanic Arc lies north of the collision of the Finisterre Terrane with the Australian continent in the west, and subduction of the Solomon Sea plate in the east (Fig. 1; Pigram and Davies 1987; Abbott et al. 1994). Although subduction has ceased beneath the western half of the arc, volcanism continues (Johnson et al. 1972). The velocity of the Finisterre collision increases rapidly eastward from the nearby pole of rotation (Tregoning 2002; Wallace et al. 2004). Bagabag Island is located to the north and slightly east of this pole of rotation where the convergence rate is ~20 mm/year. Bagabag Island is extinct and is fringed by reefs around its entire coast, and is located just east of Karkar Island, a highly active volcano (McKee et al. 1976).
We conducted a geophysical survey of the Bismarck Volcanic Arc in November–December 2004 aboard the R/V Kilo Moana. We collected bathymetric data using a hull-mounted 12 kHz Simrad EM120 multibeam echosounder, and backscatter data using a towed 12 kHz Hawaii MR1 sidescan sonar, which has a slightly wider swath width. Additionally, the slant-range correction of the sidescan data assumed a planar bottom, and therefore does not account for rapidly changing topography. Because of this assumption and the fact that the sidescan system was towed, whereas the multibeam system was hull-mounted, there may be misregistration between the sidescan and multibeam data, in particular on steep slopes.
The multibeam bathymetry data are noisy towards the edges of the swath. Noise was particularly problematic around the flanks of volcanic islands, where the rapidly decreasing depth precluded overlapping swaths. Thus, we can use the bathymetric data for general indications of the depths of features on the submarine flanks of volcanic islands, but the noise prevents detailed analysis.
Grieg Bank begins about 16 km north of Bagabag Island (Fig. 3). The bank consists of a two-peaked conical edifice about 1 km tall, followed by a semi-distinct edifice that rises to an active shallow-water reef about 25 km north of Bagabag Island (Figs. 3, 4). The southern conical edifice of Grieg Bank is relatively uniform and low backscatter (Figs. 4, 5). The larger edifice of Grieg Bank consists of a series of high backscatter, slightly sinuous lineations. These lineations are roughly slope-perpendicular and ~0.5–2 km apart.
A series of concentric, slightly sinuous, high backscatter lineations lies on the flanks of Bagabag Island (Fig. 5). These features are roughly slope-perpendicular and up to 900 m deep. Up to five of these concentric high backscatter features are observed in sidescan imagery along a given slope-parallel transect of the island’s flanks. These features are ~0.5–2 km apart. The flanks of Bagabag Island have an average slope of as much as 15° in the regions covered by multibeam data.
Discussion of observations
On Bagabag Platforms, southwest of Bagabag Island, each successive terrace steps inward, and each possesses a shallow, wide bulge around the rim, similar to those observed on the Kohala Terrace (Fig. 4; Campbell 1984). Additionally, the flanks of each terrace are slightly sinuous and have a high backscatter in sidescan imagery, similar to the drowned platforms observed in the Huon Gulf (Fig. 2). Additionally, the Bagabag Platforms bear some resemblance to the flat-topped volcanic cones observed elsewhere (Fornari and Campbell 1987; Clague et al. 2000). However, there is no evidence of rifting in this region, and flat-topped cones have not been reported with multiple tiers. Thus, it is unlikely the Bagabag Platforms represent a flat-topped cone. Also, carbonates and coral material were dredged from the Bagabag Platforms (Arculus and Yeats 2007). Around Bagabag Island and Grieg Bank, we observe sinuous, high backscatter, slope-perpendicular features in sidescan imagery (Fig. 5). These features appear similar to the sinuous, high backscatter, slope-perpendicular drowned carbonate platforms in the Huon Gulf (Fig. 2). The features around Bagabag Island and Grieg Bank are downslope of active shallow water reefs, similar to the drowned carbonate platforms in the Huon Gulf. Therefore, we interpret the features around Bagabag Island and Grieg Bank as drowned carbonate platforms.
The deepest terrace of the Bagabag Platforms is at a depth of 1,100 m. The deepest high backscatter features on Bagabag Island and Grieg Bank are approximately 900 m deep and 1,100 m deep, respectively. We infer that approximately 900 m of relative subsidence has occurred at these locations since the carbonate platforms were active.
For the flexural models we used the point-load (volcanic loading), 2D infinite beam (sedimentary loading), and 2D semi-infinite beam (collisional loading) solutions to the elastic force balance equations (Hertz 1884; Wessel 1996; Watts 2001). For all model runs, we assumed Young’s modulus equals 70 GPa and Poisson’s ratio equals 0.25. Varying these parameters did not significantly affect model outputs. In all cases, we modeled a range of plate elastic thicknesses, as the elastic thickness at the modeled locations is unknown.
The diameter of Karkar is approximately 35 km at its base. It rises from a maximum depth of 1,700 m to a maximum height of 1,840 m above sea level. The island is roughly cone-shaped. We modeled the island as a point-load corresponding to a volume of 1,100 km3 and a density of 2,500 kg/m3. We note that a point-load will over-estimate the amount of subsidence. However, this over-estimate is very slight (~1%) compared to, for instance, a distribution of 20 equally spaced partial point-loads.
The Adelbert terrane is overriding the New Guinea mainland at a rate of about 20 mm/year in the vicinity of Bagabag, based on a relative pole of rotation for the South Bismarck Plate–Australian Plate at 4.18° S, 144.02° E, with a rotation rate of 9 degrees/m.y. (Taylor 1979; Tregoning et al. 1998; Wallace et al. 2004). Uplift occurs along the Ramu–Markham Fault (Fig. 1). Towards the eastern end of the collision, the Ramu–Markham Fault dips to the north at about 45° (Abers and McCaffrey 1994; Stevens et al. 1998). Lacking data on the fault geometry near the Adelbert terrane, we assume a similar fault dip. We used the semi-infinite (broken plate) solutions to the flexure equation to model the elastic response to uplift. We modeled the Adelbert terrane as a block 60 km wide and applied a buoyant force caused by the underlying plate in order to obtain approximately 1,500 m of uplift expected for late-Pleistocene convergence (100 ka).
To model sedimentary loading, we constructed a 100 km-wide layer of uniform density (2,300 kg/m3). The thickness of the layer was 2 km, based on a sedimentation rate of 10 mm/year over 200 ka. We examined displacement 5 km from the edge of this layer.
Flexural model outputs for downward deflection of Bagabag Platforms due to volcanic loading by Karkar
Crustal elastic thickness (km)
Downward deflection due to volcanic loading by Karkar (m)
Downward deflection due to sediment (m)
Downward deflection due to Adelbert uplift (m)
Total downward deflection (m)
The drowned platforms in the vicinity of Bagabag Island are at least 30 km from the edge of the Adelbert Terrane, with the Bagabag Platforms being the closest and Grieg Bank being the farthest. Model outputs for downward deflection at this distance due to uplift of the Adelbert Terrane by buoyant forcing of the under-riding plate are summarized in Table 1. The maximum downward deflection obtained by our simulation is small (<20 m), and occurs only for an elastic thickness less than 5 km. Otherwise, the model predicts that uplift should occur.
Discussion of flexural modeling
The model for loading by Karkar Island assumes that the drowned carbonate platforms nearby predate the initiation of volcanic activity at Karkar. Even if this assumption is true, our model predicts that this loading can only account for a roughly half of the 900 m of relative subsidence inferred from the sidescan and multibeam data.
Additionally, the model predicts up to 180 m of uplift in this region due to the collision of the Adelbert Terrane with the New Guinea mainland. Specifically, as carbonate platforms approach the present location of collision at a rate of 20 mm/year, we expect a small increase in the rate of uplift that would start to counteract any local subsidence over the course of the development of the reef system. Over 100 ka, we expect roughly 2 km of convergence. The change in upward deflection over 2 km is roughly 20 m at a distance of 30 km from the edge of the terrane. Thus, we expect an actual uplift rate of roughly 0.2 mm/year.
Additional subsidence can be obtained, however, from sedimentary loading around Bagabag Island. Sedimentation rates in this region are high (Milliman 1995). For a sedimentation rate of 10 mm/year, with a sediment density of 2,300 kg/m3, a subsidence rate of ~6.8 mm/year is expected. This rate drops away from the loading as it is spread over a longer wavelength. For instance, about 5 km from the edge of a uniform layer of sedimentary loading on a lithosphere with 15 km elastic thickness, we expect about 3 mm/year of subsidence. Over 200 ka or more, this is sufficient to explain several 100 m of subsidence at Bagabag Island. Up to 2 km of sediment, combined with volcanic loading on Karkar Island and possibly increased density of the sub-sediment roots of the volcano may explain the total subsidence inferred from our data. According to seismic data described by Hamilton (1979), there may be as much as 2 km of sediment in the vicinity of Bagabag Island. However, the age of this sediment is unknown.
We interpret the concentric high backscatter features around Bagabag Island, the submarine platforms southwest of Bagabag Island, and the high backscatter features around Grieg Bank to be series of submerged carbonate platforms. From their depth we infer at least 900 m and as much as 1,100 m of subsidence has occurred at each of these locations since the deepest drowned platforms were active.
Flexural modeling of volcanic loading at these locations indicates that such a process could be responsible for a significant portion of the subsidence. However, the magnitude of relative subsidence due to volcanic loading appears to be about a factor of 2 less than the subsidence determined from the depth of the drowned platforms. Bending of the lithosphere due to the Adelbert and Finisterre collisions fail to contribute significantly to, and may even serve to counteract, any local subsidence. However, sedimentary loading in this region could be sufficient to explain the remaining subsidence we inferred at these locations if the carbonate platforms are sufficiently old.
Funding for this research was provided by the Marine Geology and Geophysics section of the U.S. National Science Foundation, grant OCE-0327004 to E. Silver and S. Ward and grant OCE-0328278 to N. Driscoll. Sidescan and multibeam data used in this study were acquired during cruise R/V Kilo Moana 0419. We thank Richard Arculus for sending us the Cruise Report of the R/V Southern Surveyor (06/2007) that describes the dredged carbonates from the Bagabag Platforms. We are grateful to the scientific party and ship’s crew of the R/V Kilo Moana 0419 for their assistance in this project, and to the reviewers of this manuscript for their comments and suggestions.
This article is distributed under the terms of the Creative Commons Attribution Noncommercial License which permits any noncommercial use, distribution, and reproduction in any medium, provided the original author(s) and source are credited.