|CMIP5||Coupled Model Intercomparison Project Phase 5|
|GCM||General Circulation Model, Global Climate Model|
|PSMSL||Permanent Service for Mean Sea Level|
|SLR||Sea Level Rise|
|SONEL||Système d'Observation du Niveau des Eaux Littorales|
|VLM||Vertical Land Movement|
Resilience, as the capacity and capability to proactively counter hazardous events, is highly dependent on clear information on the potential magnitude of those events. Therefore, to develop the resilience of coastal cities, information on local sea level rise is of uttermost importance. The keyword here is “local”: sea level rise around the planet is not homogenous, neither in space nor in time, and detailed local information is hard to get, especially when other relevant processes like local vertical land movement need to be taken into account.
This App by CLIMsystems, Hamilton, New Zealand, exposes information from global climate models combined with datasets on vertical land movement on a local level, and shows this with local population density information (which clearly shows the extend of coastal cities), offering opportunities for data presentation previously unavailable to a wide audience. The application of Esri tools and know-how, and other third party software and data makes this possible in this App.
The GCM data used in this App is from CMIP5 (see http://cmip-pcmdi.llnl.gov/cmip5/guide_to_cmip5.html). It is important to note that not all models available in the CMIP5 database contain data on sea level rise.
The monthly changes in SLR of 28 GCMs between 1986-2005 and 2081-2100 under the RCP4.5 scenario were calculated using a pattern scaling method.
GCM data were retrieved from the Earth System Grid (ESG) data portal for CMIP5, including: the sea surface height (‘zos’), the global average thermosteric sea level change (‘zostoga’) and the global average sea level change (’zosga’) under the RCP4.5 scenario. For some GCMs, only ‘zosga’ was available and was therefore used instead of ‘zostoga’. The data availability is shown in Table 1. More information on the variables applied can be found at http://www.climatechange2013.org/images/report/WG1AR5_Ch13SM_FINAL.pdf and http://www-pcmdi.llnl.gov/ipcc/standard_output.pdf.
The change in sea surface height per month was scaled by the change in global average sea level change following the pattern scaling method. The sea surface height from the GCMs includes the regional variability due to changes in water mass advection, thermohaline circulation, and wind-driven circulation, but does not include the tidal effects.
The value X (cm/cm) in the normalized patterns is interpreted as “regional sea level rises X cm when the global average sea level rises 1 cm”. When the local SLR is faster than the global average, X>1, if it is slower, X<1.
The Representative Concentration Pathways (RCPs) are four greenhouse gas concentration (not emission) trajectories adopted by the IPCC for its Fifth Assessment Report (AR5). The four RCPs (RCP2.6, RCP4.5, RCP6.0, and RCP8.5), are named after a range of radiative forcing values at their peak (RCP2.6: 2.6 W/m2 in 2050) or in the year 2100 (4.5, 6.0, and 8.5 W/m2, respectively) (Table 1).
|Description *||CO2 Equivalent||SRES Equivalent||Publication – IA Model|
|RCP8.5||Rising radiative forcing pathway leading to 8.5 W/m2 in 2100.||1370||A1FI||Raiahi et al. 2007 – MESSAGE|
|RCP6.0||Stabilization without overshoot pathway to 6 W/m2 at 2100||850||B2||Fujino et al.; Hijioka et al. 2008 – AIM|
|RCP4.5||Stabilization without overshoot pathway to 4.5 W/m2 2100||650||B1||Clark et al. 2006; Smith and Wigley 2006; Wise et al. 2009 – GCAM|
|RCP2.6||Peak in radiative forcing at ~ 3 W/m2 before 2100 and decline||490||None||van Vuuren et al., 2007; van Vuuren et al. 2006 - IMAGE|
* Approximate radiative forcing levels were defined as ±5% of the stated level in W/m2 relative to pre-industrial levels. Radiative forcing values include the net effect of all anthropogenic GHGs and other forcing agents.
An important element in the calculation of projected maximum sea level rise, is accounting for variations over the year which can change under climate change. This seasonal aspect has been taken into account by comparing the month with the highest current level with the month with the highest future level. The actual months will be different in different locations.
An example from the App:
The deviation from the yearly mean for the baseline runs between 12cm higher in February and 13cm lower in August. The changes in this variation by 2100 are small, then varying between +15cm and 16cm. The additional 3cm for the maximum month (February) have already been taken into account in the calculation of the 113cm SLR by 2100 for this location. In some location this approach adds more than 5% to the projected SLR.
The App shows a global map of the combined processes of local (absolute) sea level rise and local vertical land movement. The sea level rise values are taken as the median value of an ensemble of 28 GCM’s, under the assumption of the largest greenhouse gas emissions as described by the RCP8.5 scenario in AR5. It also assumes a high climate sensitivity.
Vertical land movement (VLM) is a generic term for all processes that impact the elevation at a given locations (tectonic movements, subsidence, ground water extraction), causing land to move up or down. This is typically a slow process with magnitudes commonly between -10 (sinking) and +10 (rising) mm/year.
Local vertical land movement becomes relevant when looking at the local effects of sea level rise. The orders of magnitude are comparable, and VLM can thus either exacerbate or dampen the sea level rise experienced at a coastal location. In a place where VLM is upward (rising, like Norway), the local experienced SLR is smaller (local SLR can even be negative: sea level going down). When VLM is downward (sinking, like Manila), local experienced SLR is stronger.
Because of its (potential) magnitude local VLM must be considered when sea level rise effects are determined on a local scale.
Note that local sea level rise is usually different from the global mean (regardless of VLM), because of variations in currents, the amount of heating of the sea water (responsible for the thermal expansion), as well as the volume (depth) of the sea water affected. This is expressed in the normalized change patterns extracted from GCM-results.
Vertical land movement can be observed directly, or inferred from related measurements.
Direct observations are available through the SONEL initiative (http://www.sonel.org/) whereby VLM is estimated from continuous GPS measurements at fixed locations, often coinciding with tidal observation stations. The latest set of “solutions” (http://www.sonel.org/-GPS-Solutions-.html?lang=en) contains location (lat/lon) and estimates of VLM (mm/year). As there are requirements for determining the trend (length of the period, completeness, quality, stability of the solution), not all stations have an associated value. With time more and more solutions will become available.
The local observed sea level rise and local vertical land movement have the following relation:
local observed SLR = local absolute SLR – local VLM
(with VLM>0 means that land is rising, VLM<0 land is sinking)
local absolute SLR = global SLR (over the observation period) * local normalized value (from an ensemble of GCMs)
To determine the global SLR over the period that the tidal observations were made, the following curve is used.
Church and White (2011) data can be downloaded from http://www.psmsl.org/products/ reconstructions/ and http://www.cmar.csiro.au/sealevel/sl_data_cmar.html.
Note: The longest part of the global curve is based on tidal observations (up to 1992, after 1992 satellite observations are used). In order to do that, assumptions needed to be made about the local VLM at each tidal station. A global model (mostly for tectonic movements) was used to do this. This creates a “thinking loop” as we are trying to estimate local VLM from data that has been corrected with a modelled VLM. The assumption is that the averaging of the data around the globe minimizes this bias.
To be able to use VLM in places where it has not been observed, the VLM values in the (SONEL or PSMSL) point locations needed to be interpolated spatially over a grid. ArcGIS has multiple models for spatial interpolation of point values which were tested on their performance noting:
The conclusion is that the IDW (Inverse Distance Weighted) model is the most useable. The following parameter choices were made:
|output cell size = 0.25°x0.25°||to confirm with resolution of SLR-patterns|
|power = 2.5||dampens the spatial extend of outliers|
|number of points = 12||creates acceptable spatial coherency|
|extend = -180,180,-90,90||global coverage|
Note: The description of the IDW tool is unclear on how it deals with coordinate system issues. As the station locations are in LAT/LON, the distances between the stations are not simple equations. It is assumed ArcGIS deals with this issue. If this is not the case, there is a bias in the inverse distance weighing. As most stations are relatively close to each other, this will only result in a small error.
The IDW tool does not wrap around the globe (crossing the 360° to 0° meridian). This was managed by executing the IDW tool twice (only for the combined result, see below): once with the 180° meridian centered and once with the 0° meridian centered (the longitudes of the observation stations were either mapped on 0° to 360°, or on -180° to 180°). The resulting images were joined using the following scheme:
The 0° to 360° image was reassembled as: B3+A2+A3+B2, while the -180° to 180°image resulted from A3+B2+B3+A2.
The methodology described combines multiple techniques and datasets to get a best estimate of local vertical land movement around the globe. Its practical usage is limited to the coastlines, where most data is collected, making use in those regions more reliable. The methodology can be reapplied to update the resulting VLM-image when new information from SONEL and/or PSMSL becomes available.
Sea level rise is a very local affair. Multiple variables interact resulting in considerable variation around the world’s coastlines in how sea level rise is expressed locally. The Marine toolbar represents values realized through the application of an ensemble of all the CMIP5 general circulation models that have sea level rise patterns. Across the 28 models there are some where the modelled sea level rise for a location will exceed the ensemble mean while others will be less. People who will use this type of sea level rise data need to be aware of this variability in model outcomes. Moreover, the models are only used to express potential change in sea level rise out to the year 2100 while sea level rise will continue for centuries given the lag in the global climate system set in train by current greenhouse gas concentrations.
Church, J. A., & White, N. J., 2011. Sea-level rise from the late 19th to the early 21st century Surveys in Geophysics, 32(4-5), 585–602. doi:10.1007/s10712-011-9119-1.
Douglas, B. C. (1991) Global sea-level rise. Journal of Geophysical Research-Oceans, 96, 6981-6992.
Douglas, B. C. (1997) Global sea rise: A redetermination. Surveys in Geophysics, 18, 279-292.
Permanent Service for Mean Sea Level (PSMSL), 2014, "Tide Gauge Data", Retrieved 17 Mar 2014 from http://www.psmsl.org/data/obtaining/.
Simon J. Holgate, Andrew Matthews, Philip L. Woodworth, Lesley J. Rickards, Mark E. Tamisiea, Elizabeth Bradshaw, Peter R. Foden, Kathleen M. Gordon, Svetlana Jevrejeva, and Jeff Pugh (2013) New Data Systems and Products at the Permanent Service for Mean Sea Level. Journal of Coastal Research: Volume 29, Issue 3: pp. 493 – 504. doi:10.2112/JCOASTRES-D-12-00175.1.
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Zervas, C. E. 2001. Sea level variations of the United States, 1854-1999. Silver Spring, Md.: U.S. Dept. of Commerce, National Oceanic and Atmospheric Administration, National Ocean Service.