Geological causes of recent (∼100 yr) vertical land movement in the Netherlands

Kooi, H.; Johnston, Paul; Lambeck, Kurt; Smither, Catherine; Molendijk, Ronald

doi:10.1016/s0040-1951(98)00209-1

Cited by 89 publications

(88 citation statements)

References 29 publications

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“…This is much more consistent with geological data than previous geodetic estimates, e.g. uplift s 1.6 mm/ yr for the Eifel with respect to reference points in other parts of the uplifting Rhenish shield [1] or 0.8 mm/yr for the Maastricht area, outside the region of main uplift [12,32]. Overestimates of regional relative motion may again have resulted partly from the use of only two or three national height surveys, where adjacent loops have been frequently measured at quite di¡erent times, and thus under highly variable subsoil moisture conditions.…”

Section: Vertical Motions Of Tectonic Origin and Geodetic Motion Ratesupporting

confidence: 90%

“…This is mainly due to the very low actual rates of crustal motion in these regions, implying that long periods of observation are needed for tectonic displacements to exceed the measurement noise and that many non-tectonic causes of such movements have also to be considered. However, the high geodetic rate estimates have contributed to the assumption that many areas currently experience increased tectonic activity [12,13] or that the contribution of transient seismotectonic processes is recorded at the geodetic timescale [14].…”

Section: Introductionmentioning

confidence: 99%

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Reconciling geodetic and geological rates of vertical crustal motion in intraplate regions

Demoulin¹

2004

Earth and Planetary Science Letters

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Tectonic motion rates of individual faults and regional deformation in an intraplate setting are estimated, based on the analysis of ten yearly surveys of a regional levelling network in NE Ardenne (W Europe). Owing to the frequency and number of measurement epochs, much greater than in classical comparisons of general surveys, the tectonic and near-surface components of ground motion are clearly separated. The marked temporal variability in ground motion strongly depends on the amount of precipitation fallen during the six months preceding each survey and the subsequent drying off of the subsoil at the time of the surveys. Moreover, the ground response to this influence varies from place to place, leading to high differential movements at the local scale. Taking into account the percentage of surveyed faults which moved tectonically during the time of the study, I calculate fault motion rates of 0.06^0.09 mm/ yr, similar to geological rates. Moreover, the data indicate that one way for intraplate normal faults to accommodate tectonic strain aseismically is intermittent fault creep, with short episodes of a few mm displacement separated by many year-long time intervals of fault quiescence. A flexural deformation shows the superposition of a tilt event on a trend corresponding to a tilt rate of 0.16 Wrad/yr for a 2.8-km-long segment. ß

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Section: Vertical Motions Of Tectonic Origin and Geodetic Motion Ratesupporting

confidence: 90%

Section: Introductionmentioning

confidence: 99%

Reconciling geodetic and geological rates of vertical crustal motion in intraplate regions

Demoulin¹

2004

Earth and Planetary Science Letters

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“…The model, however, places sea level at −18.5± 6.5 8.9 m. In the absence of the δ 18 O and Red Sea curves, it places sea level at −10.4 ± 4.4 m. In the absence of these curves, the model also identifies as an outlier early Eemian lacustrine sediment in the same core. These results suggest that the North Sea in the region of this boring is subsiding faster than the Kooi et al (1998) estimates.…”

Section: Outlier Analysismentioning

confidence: 66%

“…Finally, our model identifies as an outlier early Weichselian (post-Eemian) lacustrine sediment from a boring in the North Sea (Zagwijn, 1983). The sediment indicates freshwater conditions at a relative sea level of about -40 m, which we adjust to −23 ± 3 m based upon the subsidence estimates of Kooi et al (1998). The model, however, places sea level at −18.5± 6.5 8.9 m. In the absence of the δ 18 O and Red Sea curves, it places sea level at −10.4 ± 4.4 m. In the absence of these curves, the model also identifies as an outlier early Eemian lacustrine sediment in the same core.…”

Section: Outlier Analysismentioning

confidence: 99%

Probabilistic assessment of sea level during the last interglacial stage

Kopp¹,

Simons²,

Mitrovica³

et al. 2009

Nature

698

578

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The Last Interglacial (LIG) stage (ca. 130-115 ka), with polar temperatures likely 3-5 • C warmer than today, serves as a partial analogue for low-end future warming scenarios. Multiple indicators suggest that LIG global sea level (GSL) was higher than at present; based upon a small set of local sea level indicators, the Intergovernmental Panel on Climate Change (IPCC)'s Fourth Assessment Report inferred an elevation of approximately 4-6 m. While this estimate may be correct, it is based upon overly simplistic assumptions about the relationship between local sea level and global sea level. Sea level is often viewed as a simple function of changing global ice volume. This perspective neglects local variability, which arises from several factors, including the distortion of the geoid and the elastic and isostatic deformation of the solid Earth by shifting ice masses. Accurate reconstruction of past global and local sea levels, as well as ice sheet volumes, therefore requires integrating globally distributed data sets of local sea level indicators. To assess the robustness of the IPCC's global estimate and search for patterns in local sea level that are diagnostic of meltwater sources, we have compiled a comprehensive database that includes a variety of local sea level indicators from 47 localities, as well as a global sea level record derived from oxygen isotopes. We generate a global synthesis from these data using a novel statistical approach that couples Gaussian process regression to Markov Chain Monte Carlo simulation of geochronological errors. Our analysis strongly supports the hypothesis that global sea level during the Last Interglacial was higher than today, probably peaking between 6-9 m above the present level. This level is close to that expected from the complete melting of the Greenland Ice Sheet, or from major melting of both the Greenland and West Antarctic Ice Sheets. In the period when sea level was within 10 m of the modern value, the fastest rate of sea level rise sustained for a 1 ky period was likely about 80-110 cm per century. Combined with the evidence for mildly higher temperatures during the LIG, our results highlight the vulnerability of ice sheets to even relatively low levels of sustained global warming.

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“…The net area averaged sediment accumulation rate of 4.2 mm year −1 in the Kleine Noordwaard study area is just enough to compensate the actual rate of sea-level rise and soil subsidence in the Netherlands, which are 2 mm year −1 (Ligvoet et al 2015) and 0.5-2.5 mm year −1 for the Biesbosch (Kooi et al 1998). However, the accumulation can not compensate the high end scenarios for sea-level rise in the Netherlands of 0.4 to 10.5 mm y −1 (Katsman et al 2011), especially since freshly deposited sediment will compact over the years and thus result in a lower net accumulation.…”

Section: Discussionmentioning

confidence: 87%

Factors controlling sediment trapping in two freshwater tidal wetlands in the Biesbosch area, The Netherlands

2017

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Purpose A thorough understanding of mechanisms controlling sedimentation and erosion is vital for a proper assessment of the effectiveness of delta restoration. Only few field-based studies have been undertaken in freshwater tidal wetlands. Furthermore, studies that measured sediment deposition in newly created wetlands are also sparse. This paper aims to identify the factors controlling the sediment trapping of two newly created freshwater tidal wetlands. Materials and methods Two recently re-opened polder areas in the Biesbosch, The Netherlands are used as study area. Field measurements of water levels, flow velocities, and turbidity at both the in-and outlet of the areas were carried out to determine the sediment budgets and trapping efficiencies under varying conditions of river discharge, tide, and wind in the period 2014-2016. Results and discussion Short-term sediment fluxes of the two study areas varied due to river discharge, tide, and wind. A positive sediment budget and trapping efficiency was found for the first study area, which has a continuing supply of river water and sediment. Sediment was lost from the second study area which lies further from the river and had a lower sediment supply. The daily sediment budget is positively related to upstream river discharge, and in general, export takes place during ebb and import during flood. However, strong wind events overrule this pattern, and trapping efficiencies decrease for increasing wind strengths at mid-range river discharges and for the highest river discharges due to increased shear stress. Conclusions Delta restoration, based on sedimentation to compensate for sea-level rise and soil subsidence, could only be effective when there is a sufficient supply of water and sediment. Management to enhance the trapping efficiency of the incoming sediment should focus on directing sufficient river flow into the wetland, ensuring the supply of water and sediment within the system during a tidal cycle, creating sufficiently large residence time of water within the polder areas for sediment settling, and decreasing wave shear stress by the establishment of vegetation or topographic irregularities.

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Geological causes of recent (∼100 yr) vertical land movement in the Netherlands

Cited by 89 publications

References 29 publications

Reconciling geodetic and geological rates of vertical crustal motion in intraplate regions

Reconciling geodetic and geological rates of vertical crustal motion in intraplate regions

Probabilistic assessment of sea level during the last interglacial stage

Factors controlling sediment trapping in two freshwater tidal wetlands in the Biesbosch area, The Netherlands

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