Prepared by Richard Dunne October 2013
The Chagos Islands
Physical Environment – Key Facts
Over the last 20 years the Chagos has been a relatively stable
physical environment,
and these low-lying coral islands should continue to be able to
support human
habitation, as they have done for much of the last 200 years
(Dunne et al. 2012).
Island Morphology
- The Chagos islands are all of low
elevation with only 18% of their land above 2 m and 7% above 3 m (Woodroffe 2008). They were formed between 6,000 and 4,000
years beforepresent (BP) (Perry et al. 2011) when sea level had risen to
about its present level.
- Reef islands are accumulations of
sand and gravel (derived from the surrounding reef) that are transported and deposited by waves and wave-induced currents
on reef surfaces. The location of islands therefore, results from the unique combination
of hydrodynamic forces and the sediment available for transport and deposition. The
maximum elevation of reef islands is controlled by wave runup against the shoreline, which
controls the maximum level of sediment deposition. Wave overtopping (and associated
inundation) therefore, is a natural mechanism that allows a fresh layer of sediment to be
added to island surfaces, thus increasing land levels (Kench et al. 2006).
- Increasing land elevation through
overwash processes, combined with differential erosion and accretion of island shorelines, controls the dynamic physical
adjustment of islands on reef surfaces (Webb & Kench 2010) and provides mechanisms for
islands to adjust to changing environmental boundary conditions.
- A comparison of the shape of Diego
Garcia atoll between 1824 and 1971 suggests that any changes to the size of the island over this timespan have been
minor (Stoddart 1971a).
- A comparison of island morphology in
Salomon and Egmont Atolls between 1905 and the present day suggests that some islands may have decreased in size
to a small extent (Ile Boddam -4.7%, Ile de la Passe -2.8%) but that others have
increased (Ile Takamata +6.3%; Egmont Atoll +36.5%). This is over a time period when GMSL rose by
about 20 cm (Dunne unpublished).
- A survey of 27 Pacific Atoll islands
over a 20 to 61 year period during which sea-level has risen at 2mm year-1 has demonstrated that 43% of the islands remained stable, 43% increased in size, and 14% decreased (Webb & Kench 2010). The
study showed that these islands are robust and can increase in area despite sea-level
rise, that erosion may be balanced by deposition on other parts of the shore, and that the
islands are dynamic landforms that adjust in response to physical conditions.
Furthermore the study results were applicable to islands in other reef settings and contradicted
widespread perceptions that all reef islands are eroding in response to recent sea-level rise.
Seismic Activity
- The Chagos lie in an area of the Indo–Australian
tectonic plate where there is intense intraplate deformation, with high seismic activity.
- Large earthquakes occurred in the
area in 1912 (M6.8) and 1983 (M7.6) with a “swarm” of moderate sized earthquakes in 1965–1968 (Wiens 1986).
- Since 1973, there have been 314
earthquakes greater than M4.5 within a 500 km (270 nm) radius of Diego Garcia (USGS/NEIC PDE, 2011. http:
//earthquake.usgs.gov/ earthquakes/ eqarchives/epic/.Catalogue searched 13 Jun 2011).
Vertical land movement
- Although in an area of seismic
activity, there is no record of island subsidence, indeed onDiego Garcia minor crustal uplift of 0.63} 0.28 SE mm year−1 has occurred between 1996 and 2009 (Dunne et al. 2012).
- On Diego Garcia there is tentative
evidence of ‘emergence’ of the atoll (Woodroffe 2005) but this is actually due to a slight lowering of the sea level
since the mid-Holocene (3,000 years ago).
- There is no known evidence of
subsidence in the archipelago in the past 100 years (Dunne et al. 2012).
- Tectonic plate movements and seismic
activity can cause changes to island elevation and there is some inference of uplift having occurred on several islands
(part of Coin du Mire in Peros Banhos atoll, and North Brother and Resurgent in the Three
Brothers group).
Sea Level
- Sea level rise (SLR) is an
inescapable consequence of increasing greenhouse gas concentrations, whether these are due to anthropogenic causes or
otherwise.
- Global mean sea level (GMSL) is
controlled primarily by volume changes of the world’s oceans and is currently rising at a rate of 3.2 } 0.4 mm year-1 (Colorado University Sea Level Research Group - http://sealevel.colorado.edu/) although more recent analysis suggests that part of this rise might be due to the Pacific Decadal Oscillation
and that the true rate of rise is 2.7 mm year-1 (Hamlington et al. 2013).
- Over the period, 1901-2010, GMSL has
risen by between 17 and 21 cm as measured by tide gauges (IPCC 2013b; IPCC 2013a).
- There is no evidence that the rate of
GMSL rise accelerated during the 20th Century (Gregory et al. 2013).
- Due to continued warming of the world’s
oceans induced by increasing greenhouse gas (GHG) concentrations, global mean sea level is projected to rise
by between 26–97 cm by the end of the 21st century, depending on which Intergovernmental
Panel on Climate Change Representative Concentration Pathway (RCP) will be realized
in the future. There are large uncertainties in the ranges projected by the models. Under
RCP 4.5 or 6, both of which are considered realistic, GMSL will rise by a further 24 cm by
2050 and 64 cm by 2100 from today’s levels (2013) computed from figures in IPCC (2013b) and
IPCC (2013a).
- Regionally, because of changes in
wind- and buoyancy-driven ocean currents in response to global warming, local sea-level rise (SLR) could be higher or
lower than the global mean, but on past history is likely to be lower in the Chagos region of the
Indian Ocean (Han et al. 2010).
- In the Chagos Archipelago no
significant SLR can be detected in the instrument record (tide gauge at Diego Garcia 1988-2011, and satellite altimetry
1993-2011) (Dunne et al. 2012).
- There is also no long term change in
the incidences of the highest sea level (e.g., extreme spring tides) when island flooding or inundation is most likely to
take place (Dunne et al. 2012).
Erosion and Flooding
- There are recent documented reports
of sea-water inundation and flooding in the Chagos islands, e.g., on Diego Garcia (Sheppard 2012a; Sheppard 2012b)
which have been attributed to rising sea level. Sheppard (2012a) has also characterised this
as “accelerating both on Diego Garcia and on northern atolls”
- Inundation is however a regular
feature at different locations on these islands and there is no evidence to suggest that this is increasing over time on Diego
Garcia (Dunne 2013).
- Erosion is a natural process on all
low lying coral islands and is manifest in seasonal removal and deposition of sediments from different shorelines driven by
the changing monsoonal winds and currents. These effects are evident in the Chagos over
decades to hundreds of years e.g., (Woodroffe 2011).
- Inundation and erosion has regularly
been reported by researchers for over 120 years, e.g., on Diego Garcia (Bourne 1886).
- On Diego Garcia, shoreline erosion
has been particularly evident since major engineering work began in the 1970s and has been exacerbated by reef bedrock
removal, shoreline engineering and vegetation clearance (EG&G Environmental
Consultants 1980; Moffatt & Nichol 2008).
Cyclones, Storms, and Wind/Wave environment
- The Chagos lie outside the Indian
Ocean cyclone belt and experience relatively low wind speeds (Dunne et al. 2012).
- The last known cyclone to pass over
the islands was in 1891.
- There is no evidence of changes in
the wind or wave environment in the past 20 years (Dunne et al. 2012).
- Projected changes in the wind/wave
climate of the Indian Ocean for the years 2075-2100 compared to 1980-2009 are that significant wave height (Hs) will decrease by about 5% (IPCC 2013b; IPCC 2013a). Significant wave height is the mean of the
upper ⅓ of the largest waves.
- There are no projected future changes
in either the location of the tropical cyclone belt or the frequency of storms for the Indian Ocean (IPCC 2013b; IPCC
2013a).
Overtopping and flooding
- The potential for wave overtopping of
the island of Ile du Coin (Peros Banhos atoll) and Ile Boddam (Salomon atoll) which led to the conclusion that “both Ile Boddam and Ile du Coin are likely to experience severe overtopping” in the 2002 Phase 2B Feasibility Study (Posford Haskoning Ltd 2002) has since been demonstrated to be flawed
(Kench 2012).
- Modelling of the response of low
lying coral islands to increases in sea level demonstrates that, subject to sediment supply, beach ridges increase in height
and migrate inland and retain their capacity to protect the island from wave overtopping
(Cowell & Kench 2001).
Rainfall and Water resources
- The Chagos islands (Salomon &
Peros Banhos atolls in particular) have the highest annual rainfall totals of all Indian Ocean atolls (Stoddart 1971b), approximately
3,750 and 4,000 mm year-1 respectively
(Posford Haskoning Ltd 2002).
- Completely dry months do not occur on
Salomon & Peros Banhos atolls (Stoddart 1971b).
- Freshwater on all the islands is
contained in lenses trapped in the coral basement and is suitable for domestic consumption.
- The water supply ‘population capacity’
of the two principal islands in the northern atolls would be approximately 3,000 for Ile du Coin and 1,500 for Ile
Boddam for an average water demand of 100 litres per person per day (Posford Haskoning Ltd
2002).
- Diego Garcia obtains all its
freshwater supplies from the island lenses, sufficient to support a population of several thousand military and civilian contractors.
Phase 2B Resettlement Study 2002
- The ‘General conclusions’ found in
section 1.11 of the Executive Summary appear to be predicated largely on the Section 6 of the Feasibility Study and
as such are considered to be flawed (Kench 2012).
- Reviews of the critical Section 6 of
the Study were superficial and demonstrated that those tasked with assessing the robustness of the science by the FCO (Mr
Little & Dr Sheppard) were not qualified to do so (Kench 2012) as a consequence they
failed to detect scientific errors in the Study which led to the flawed ‘General conclusions’
(above).
References
Bourne, G. C. (1886) On the Island of Diego Garcia of the Chagos
Group. Proceedings of the Royal
Geographical Society and Monthly Record of
Geography 8(6): 385-393.
Cowell, P. J. & Kench, P. S. (2001) The Morphological Response
of Atoll Islands to Sea-Level Rise. Part
2: Application of the Modified Shoreface Translation Model (STM). Journal of Coastal
Research (Special Issue
34): 645-656.
Dunne, R. P. (2013) Sharks on the lawn in Diego Garcia - but is
rising sea level to blame? Ocean
Challenge (Summer
2013).
Dunne, R. P., Barbosa, S. M. & Woodworth, P. L. (2012)
Contemporary sea level in the Chagos
Archipelago, central Indian Ocean. Global and Planetary Change 82-83: 25-37.
EG&G Environmental Consultants. (1980) Environmental survey of
construction and dredging related
activities on Diego Garcia, Indian Ocean. pp. 1-107. Hawaii.
Gregory, J. M., White, N. J., Church, J. A., Bierkens, M. F. P.,
Box, J. E., van den Broeke, M. R., Cogley,
J. G., Fettweis, X., Hanna, E., Huybrechts, P., Konikow, L. F.,
Leclercq, P. W., Marzeion, B.,
Oerlemans, J., Tamisiea, M. E., Wada, Y., Wake, L. M. & van de
Wal, R. S. W. (2013)
Twentieth-Century Global-Mean Sea Level Rise: Is the Whole Greater
than the Sum of the
Parts? Journal of Climate 26(13): 4476-4499.
Hamlington, B. D., Leben, R. R., Strassburg, M. W., Nerem, R. S.
& Kim, K. Y. (2013) Contribution of
the pacific decadal oscillation to global mean sea level trends. Geophysical Research Letters:
2013GL057297.
Han, W., Meehl, G. A., Rajagopalan, B., Fasullo, J. T., Hu, A.,
Lin, J., Large, W. G., Wang, J. w., Quan, X.
W., Trenary, L. L., Wallcraft, A., Shinoda, T. & Yeager, S.
(2010) Patterns of Indian Ocean sealevel
change in a warming climate. Nature Geosci 3(546): 550.
IPCC. (2013a) Working Group I contribution to the IPCC 5th
Assessment Report "Climate Change
2013: The Physical Science Basis - 30 September 2013. pp. 2216.
Stockholm.
IPCC. (2013b) Working Group I Contribution to the IPCC Fifth
Assessment Report, Climate Change
2013: The Physical Science Basis - Summary for Policymakers - 27
September 2013. pp. 36.
Kench, P. S. (2012) Review of the Coastal Processes and Ocean
Study: Feasibility Study for
Resettlement of the Chagos Archipelago (Royal Haskoning, 2002).
pp. 15. Auckland:
University of Auckland.
Kench, P. S., McLean, R. F., Brander, R. W., Nichol, S. L.,
Smithers, S. G., Ford, M. R., Parnell, K. E. &
Aslam, M. (2006) Geological effects of tsunami on mid-ocean atoll
islands: The Maldives
before and after the Sumatran tsunami. Geology 34(3): 177-180.
Moffatt & Nichol. (2008) Diego Garcia Shoreline Erosion Study.
p. 120. Long Beach, CA: Moffatt &
Nichol, 2780 Kilroy Airport Way, Suite 600, Long Beach, CA 90806.
Perry, C. T., Kench, P. S., Smithers, S. G., Riegl, B., Yamano, H.
& O'Leary, M. J. (2011) Implications of
reef ecosystem change for the stability and maintenance of coral
reef islands. Global Change
Biology 17(12): 3679-3696.
Posford Haskoning Ltd. (2002) Feasibility Study for the
Resettlement of the Chagos Archipelago:
Phase 2B. In: London.
Prepared by Richard Dunne October 2013
Sheppard, C. (2012a) Seawater inundations in the Chagos
archipelago at high tides, and shoreline
erosion. CCT unpublished report.
Sheppard, C. R. (2012b) Sharks on the lawn - The reality of rising
sea-level on Indian Ocean islands.
Ocean Challenge (Autumn 2012): 17.
Stoddart, D. R. (1971a) Geomorphology at Diego Garcia Atoll. In: Atoll Research Bulletin, Geography
and Ecology of Diego Garcia Atoll, Chagos
Archipelago, eds. D. R. Stoddart & J. D.
Taylor, pp.
7-26. Atoll Research Bulletin: The Smithsonian Institution.
Stoddart, D. R. (1971b) Rainfall on Indian Ocean Islands. Atoll Research Bulletin 147: 1-22.
Webb, A. P. & Kench, P. S. (2010) The dynamic response of reef
islands to sea-level rise: Evidence
from multi-decadal analysis of island change in the Central
Pacific. Global and Planetary
Change 72(3): 234-246.
Wiens, D. A. (1986) Historical seismicity near Chagos: a complex
deformation zone in the equatorial
Indian Ocean. Earth and
Planetary Science Letters 76(3-4): 350-360.
Woodroffe, C. D. (2005) Late Quaternary sea-level highstands in
the central and eastern Indian
Ocean: A review. Global and Planetary Change 49(1-2): 121-138.
Woodroffe, C. D. (2008) Reef-island topography and the
vulnerability of atolls to sea-level rise.
Global and Planetary Change 62(1-2): 77-96.
Woodroffe, S. A. (2011) Sea-level
changes and shoreline dynamics. Unpublished report