Production and off-bank transport of carbonate sediment, Black Rock, southwest Little Bahama Bank

Hoskin, Charles M.; Reed, John K.; Mook, David

doi:10.1016/0025-3227(86)90115-5

Cited by 31 publications

(17 citation statements)

References 12 publications

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“…The bathymetrical pattern is in good agreement with previous experimental studies (e.g. Hoskin et al, 1986;Hassan, 1998;Vogel et al, 1996Vogel et al, , 2000see Wisshak, 2006 for a review) as well as qualitative assessments of bioeroding communities (e.g. Golubic et al, 1975;Zeff and Perkins, 1979;Budd and Perkins, 1980;Wisshak et al, 2005).…”

Section: Carbonate Bioerosion and Accretion Ratessupporting

confidence: 88%

“…7) -roughly following the course of the Gulf Stream -there are three studies that allow for a semi-direct comparison. These are the experiments in the cold-temperate Swedish Kosterfjord in 59 • northern latitude (Wisshak et al, 2005, Wisshak, 2006 on the one hand and the studies on the tropical Bahamas (26 • N) carried out by Hoskin et al (1986) and Vogel et al (1996Vogel et al ( , 2000 on the other. These experiments applied a similar experimental design with respect to the utilised micritic limestone as substrate, a similar gravimetrical approach for determining the rates (except for Vogel et al, 1996Vogel et al, , 2000, who used SEM surveys for quantifying bioerosion), and the investigation over an extended bathymetrical range.…”

Section: Latitudinal Gradientmentioning

confidence: 99%

“…7 right), Hoskin determined microbioerosion rates of −259, −237, −40, −2 and −0.5 g/m 2 /yr after one year in 0, 2, 32, 79, and 477 m of water depth, respectively (figure 4 in Hoskin et al, 1986), and Vogel et al found an average −210, −105, −13, −6, and −2 g/m 2 /yr combining one and two years of exposure in 2, 30, 100, 150 and 275 m depth (figure 7 in Vogel et al, 2000). In addition, Hoskin et al (1986) determined grazing rates of specific grazers such as the chiton Acanthopleura granula which degrades about −100 g/m 2 /yr and the echinoid Echinometra lacunter reaching the impressive value of −6670 g/m 2 /yr, indicating that the overall bioerosion at least for the shallowest waters in this tropical setting is probably far stronger than found in the Azores. This is also indicated by most bioerosion experiments carried out in the other warm-water coral provinces were total bioerosion rates -particularly governed by grazing echinoids and parrot fish -are usually in the range of −500 to −10000 g/m 2 /yr (see Table 1 in Wisshak, 2006 for a compilation of available experimental data).…”

Section: Latitudinal Gradientmentioning

confidence: 99%

“…7. Carbonate bioerosion and accretion rates along a latitudinal and environmental gradient of the N-Atlantic from the cold-temperate Kosterfjord (data from Wisshak, 2006; up-facing substrates only), to the warm-temperate Azores archipelago, to the tropical Bahamas (data from Hoskin et al, 1986;3-D substrates). In addition, the vertical extend of the photic zonation is illustrated (data from Wisshak et al, 2005 andVogel et al, 2000).…”

Section: Carbonate Budgetmentioning

confidence: 99%

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Temperate carbonate cycling and water mass properties from intertidal to bathyal depths (Azores)

Wisshak¹,

Form

Jakobsen³

et al. 2010

Biogeosciences

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Abstract. The rugged submarine topography of the Azores supports a diverse heterozoan association resulting in intense biotically-controlled carbonate-production and accumulation. In order to characterise this cold-water (C) factory a 2-year experiment was carried out in the southern Faial Channel to study the biodiversity of hardground communities and for budgeting carbonate production and degradation along a bathymetrical transect from the intertidal to bathyal 500 m depth.Seasonal temperatures peak in September (above a thermocline) and bottom in March (stratification diminishes) with a decrease in amplitude and absolute values with depth, and tidal-driven short-term fluctuations. Measured seawater stable isotope ratios and levels of dissolved nutrients decrease with depth, as do the calcium carbonate saturation states. The photosynthetic active radiation shows a base of the euphotic zone in ∼70 m and a dysphotic limit in ∼150 m depth.Bioerosion, being primarily a function of light availability for phototrophic endoliths and grazers feeding upon them, is ∼10 times stronger on the illuminated upside versus the shaded underside of substrates in the photic zone, with maximum rates in the intertidal (−631 g/m 2 /yr). Rates rapidly decline towards deeper waters where bioerosion and carbonate accretion are slow and epibenthic/endolithic communities take years to mature. Accretion rates are highest in the lower euphotic zone (955 g/m 2 /yr), where the substrate is less prone to hydrodynamic force. Highest rates are found -inversely to bioerosion -on down-facing substrates, suggesting that bioerosion may be a key factor governing the preferCorrespondence to: M. Wisshak (max.wisshak@gzn.uni-erlangen.de) ential settlement and growth of calcareous epilithobionts on down-facing substrates.In context of a latitudinal gradient, the Azores carbonate cycling rates plot between known values from the coldtemperate Swedish Kosterfjord and the tropical Bahamas, with a total range of two orders in magnitude. Carbonate budget calculations for the bathymetrical transect yield a mean 266.9 kg of epilithic carbonate production, −54.6 kg of bioerosion, and 212.3 kg of annual net carbonate production per metre of coastline in the Azores C factory.

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Section: Carbonate Bioerosion and Accretion Ratessupporting

confidence: 88%

Section: Latitudinal Gradientmentioning

confidence: 99%

Section: Latitudinal Gradientmentioning

confidence: 99%

Section: Carbonate Budgetmentioning

confidence: 99%

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Temperate carbonate cycling and water mass properties from intertidal to bathyal depths (Azores)

Wisshak¹,

Form

Jakobsen³

et al. 2010

Biogeosciences

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“…For example, Echinometra lucunter -a species that is common in the Bahamas and Bermuda but also on many Atlantic hotspot islands such as the Cape Verdes (see Fig. 7f) -is capable of eroding 6670 to 7000 g/m 2 /yr (Hunt, 1969;Hoskin et al, 1986). Another good example is Paracentrotus lividus, which is the most conspicuous bioeroding echinoderm in the Azores, Madeira, the Canaries and the Cape Verdes, being especially abundant at 1-2 m depth (Madeira et al, 2011).…”

Section: Bioerosionmentioning

confidence: 99%

Coastal evolution on volcanic oceanic islands: A complex interplay between volcanism, erosion, sedimentation, sea-level change and biogenic production

Ramalho¹,

Quartau

Trenhaile

et al. 2013

Earth-Science Reviews

153

147

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The growth and decay of oceanic hotspot volcanoes are intrinsically related to a competition between volcanic construction and erosive destruction, and coastlines are at the forefront of such confrontation. In this paper, we review the several mechanisms that interact and contribute to the development of coastlines on oceanic island volcanoes, and how these processes evolve throughout the islands' lifetime. Volcanic constructional processes dominate during the emergent island and subaerial shield-building stages. During the emergent island stage, surtseyan activity prevails and hydroclastic and pyroclastic structures form; these structures are generally ephemeral because they can be rapidly obliterated by marine erosion. With the onset of the subaerial shield-building stage, coastal evolution is essentially characterized by rapid but intermittent lateral growth through the formation of lava deltas, largely expanding the coastlines until they, typically, reach their maximum extension. With the post-shield quiescence in volcanic activity, destructive processes gradually take over and coastlines retreat, adopting a more prominent profile; mass wasting and marine and fluvial erosion reshape the landscape and, if conditions are favorable, biogenic processes assume a prominent role. Posterosional volcanic activity may temporarily reverse the balance by renewing coastline expansion, but islands inexorably enter in a long battle for survival above sea level. Reef growth and/or uplift may also prolong the island's lifetime above the waves. The ultimate fate of most islands, however, is to be drowned through subsidence and/or truncation by marine erosion.Keywords complex, interplay, between, volcanism, erosion, sedimentation, sea, level, islands, change, coastal, biogenic, production, oceanic, evolution, volcanic, GeoQuest Disciplines Medicine and Health Sciences | Social and Behavioral Sciences Publication DetailsRamalho, R. S., Quartau, R., Trenhaile, A. S., Mitchell, N. C., Woodroffe, C. D. & Avila, S. P. (2013). Coastal evolution on volcanic oceanic islands: a complex interplay between volcanism, erosion, sedimentation, sealevel change and biogenic production. Earth-Science Reviews, 127 140-170. AbstractThe growth and decay of oceanic hotspot volcanoes are intrinsically related to a competition between volcanic construction and erosive destruction, and coastlines are at the forefront of such confrontation. In this paper, we review the several mechanisms that interact and contribute to the development of coastlines on oceanic island volcanoes, and how these processes evolve throughout the islands' lifetime. Volcanic constructional processes dominate during the emergent island and subaerial shield-building stages. During the emergent island stage, surtseyan activity prevails and hydroclastic and pyroclastic structures form; these structures are generally ephemeral because they can be rapidly obliterated by marine erosion. With the onset of the subaerial shield-building stage, coastal evolution is essentially ch...

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Source and supply of sediment to a shoreline salient in a fringing reef environment

Cuttler

Hansen

Lowe

et al. 2018

Earth Surf Processes Landf

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Reef‐associated landforms are coupled to the health of the reef ecosystem which produces the sediment that forms and maintains these landforms. However, this connection can make reef‐fronted coastlines sensitive to the impacts of climate change, given that any decline in ecosystem health (e.g. decreasing sediment supply) or changes to physical processes (e.g. sea level rise, increasing wave energy) could drive the sediment budgets of these systems into a net erosive state. Therefore, knowledge of both the sediment sources and transport mechanisms is required to predict the sensitivity of reef‐associated landforms to future climate change. Here, we examine the benthic habitat composition, sediment characteristics (composition, texture, and age), and transport mechanisms and pathways to understand the interconnections between coastal morphology and the reef system at Tantabiddi, Ningaloo Reef, Western Australia. Benthic surveys and sediment composition analysis revealed that although live coral accounts for less than 5% of the benthic cover, coral is the dominant sediment constituent (34% on average). Sediment ages (238U/230Th) were mostly found to be thousands of years old, suggesting that the primary sediment source is relic reef material (e.g. Holocene reef framework). Sediment transport across the lagoon was quantified through measurements of ripple migration rates, which were found to be shoreward migrating and responsible for feeding the large shoreline salient in the lee of the reef. The derived sediment fluxes were comparable with previously measured rates of sediment production by bioerosion. These results suggest that sediment budgets of systems dependent on old (>103 years) source materials may be more resilient to climate change as present‐day reef health and community composition (i.e. sources of ‘new’ carbonate production) have limited influence on sediment supply. Therefore, the vulnerability of reef‐associated landforms in these systems will be dictated by future changes to mechanisms of sediment generation (e.g. bioerosion) and/or physical processes. © 2018 John Wiley & Sons, Ltd.

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Production and off-bank transport of carbonate sediment, Black Rock, southwest Little Bahama Bank

Cited by 31 publications

References 12 publications

Temperate carbonate cycling and water mass properties from intertidal to bathyal depths (Azores)

Temperate carbonate cycling and water mass properties from intertidal to bathyal depths (Azores)

Coastal evolution on volcanic oceanic islands: A complex interplay between volcanism, erosion, sedimentation, sea-level change and biogenic production

Source and supply of sediment to a shoreline salient in a fringing reef environment

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