Sea-level change, glacial rebound and mantle viscosity fornorthern Europe

Lambeck, Kurt; Smither, Catherine; Johnston, Paul

doi:10.1046/j.1365-246x.1998.00541.x

Cited by 552 publications

(501 citation statements)

References 60 publications

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“…Similar findings from the Skagerrak support this interpretation. There, the small coral reefs are under the influence of the isostatic balance of the glacial rebound of Scandinavia lifting the lithosphere and bringing the corals continuously under the influence of the low-saline Baltic water (e.g., Lambeck et al, 1998). Foraminiferal assemblages in the coral facies have only a small contribution of D. coronata, which indicates that the abundance of this species mirrors similar ecological requirements as the corals.…”

Section: Maya Mud Volcanomentioning

confidence: 99%

Growth and demise of cold-water coral ecosystems on mud volcanoes in the West Alboran Sea: The messages from the planktonic and benthic foraminifera

et al. 2011

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The Dhaka and Maya mud volcanoes (MVs), located in the Mud Diapir Province in the Western Alboran Basin along the Moroccan Coasts, were cored during the TTR-17, Leg 1 cruise. Cores were taken on the top of the volcanoes at a water depth of 370 m on the Dhaka MV (core TTR17-MS411G) and at 410 m water depth on the Maya MV (core TTR17-MS419G), respectively. On both mud volcanoes the extruded mud breccia provides the nucleation point for the colonization and development of cold-water corals and associated ecosystems. Two phases of cold-water coral growth are observed: (1) between slightly older than 4175± 62 years BP and around 2230± 59 years BP at Dhaka, and (2) between slightly older than 15583 ± 185 years BP and around 7613 ± 38 years BP at Maya MV. On the top of the Maya MV only a small patch reef and/or isolated corals proliferated, whereas a more extended patch reef colonized the top of the Dhaka MV. At both sites the cold-water coral development was triggered by the availability of a suitable substrate for initial coral settling, provided either as a firm ground or as single clasts. Subsequently coral growth was supported by enhanced nutrient flux possibly related to upwelling and/or strong currents. During the intervals of coral growth planktonic foraminiferal assemblages were dominated by Neogloboquadrina incompta. The decline of coral ecosystems on the mud volcanoes is accompanied at surface by a shift from the N. incompta dominated assemblage to a Globorotalia inflata dominated assemblage, possibly reflecting more oligotrophic conditions. This shift is coeval to the passage from wet to arid conditions at the end of the African Humid Period at Maya MV. It is interpreted as an effect of an early human impact on a fragile environment, which was already stressed by desiccation at the time of the development of complex human society along the Mediterranean coasts, at Dhaka MV.

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Section: Maya Mud Volcanomentioning

confidence: 99%

Growth and demise of cold-water coral ecosystems on mud volcanoes in the West Alboran Sea: The messages from the planktonic and benthic foraminifera

et al. 2011

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“…Fjeldskaar 1994;Lambeck et al 1998;Milne et al 2001;Steffen and Kaufmann 2005). They also inform us on vertical land motion-an important component of present-day RSL change for Norway.…”

Section: Present-day Vertical Land Motion In Norwaymentioning

confidence: 95%

“…The ice model is made of two parts: The Fennoscandian and Barents Sea ice sheets are represented by the model of Lambeck et al (1998), which has been shown to provide good fit to paleo sea level data from the region. For other areas of the globe, we use the ICE-3G ice sheet reconstruction of Tushingham and Peltier (1991).…”

Section: Glacial Isostatic Adjustment Modelingmentioning

confidence: 99%

“…Lambeck et al 1998) and/or GNSS observations (e.g. Milne et al 2001Milne et al , 2004 to help constrain Earth model parameters.…”

Section: Earth Model Sensitivity Test and Determining A Best-fit Modelmentioning

confidence: 99%

“…Paleo observations from across Fennoscandia, including Norway, show a spatial pattern of RSL change over the past *10,000 years that largely reflects vertical land motion (e.g. Lambeck et al 1998). This process, termed Glacial Isostatic Adjustment (GIA), provides a measure of the Earth's viscous relaxation in response to past ice mass loss.…”

Section: Introductionmentioning

confidence: 99%

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Estimates of twenty-first century sea-level changes for Norway

2013

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In this work we establish a framework for estimating future regional sea-level changes for Norway. Following recently published works, we consider how different physical processes drive non-uniform sea-level changes by accounting for spatial variations in (1) ocean density and circulation (2) ice and ocean mass changes and associated gravitational effects on sea level and (3) vertical land motion arising from past surface loading change and associated gravitational effects on sea level. An important component of past and present sea-level change in Norway is glacial isostatic adjustment. Central to our study, therefore, is a reassessment of vertical land motion using a far larger set of new observations from a permanent GNSS network. Our twenty-first century sea-level estimates are split into two parts. Firstly, we show regional projections largely based on findings from the Fourth Assessment Report of the Intergovernmental Panel on Climate Change (IPCC AR4) and dependent on the emission scenarios A2, A1B and B1. These indicate that twenty-first century relative sea-level changes in Norway will vary between -0.2 to 0.3 m (1-sigma ± 0.13 m). Secondly, we explore a high-end scenario, in which a global atmospheric temperature rise of up to 6°C and emerging collapse for some areas of the Antarctic ice sheets are assumed. Using this approach twenty-first century relative sea-level changes in Norway are found to vary between 0.25 and 0.85 m (min/ max ± 0.45 m). We attach no likelihood to any of our projections owing to the lack of understanding of some of the processes that cause sea-level change.

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