Skip to main content

Thank you for visiting You are using a browser version with limited support for CSS. To obtain the best experience, we recommend you use a more up to date browser (or turn off compatibility mode in Internet Explorer). In the meantime, to ensure continued support, we are displaying the site without styles and JavaScript.

Remote coral reefs can sustain high growth potential and may match future sea-level trends


Climate-induced disturbances are contributing to rapid, global-scale changes in coral reef ecology. As a consequence, reef carbonate budgets are declining, threatening reef growth potential and thus capacity to track rising sea-levels. Whether disturbed reefs can recover their growth potential and how rapidly, are thus critical research questions. Here we address these questions by measuring the carbonate budgets of 28 reefs across the Chagos Archipelago (Indian Ocean) which, while geographically remote and largely isolated from compounding human impacts, experienced severe (>90%) coral mortality during the 1998 warming event. Coral communities on most reefs recovered rapidly and we show that carbonate budgets in 2015 average +3.7 G (G = kg CaCO3 m−2 yr−1). Most significantly the production rates on Acropora-dominated reefs, the corals most severely impacted in 1998, averaged +8.4 G by 2015, comparable with estimates under pre-human (Holocene) disturbance conditions. These positive budgets are reflected in high reef growth rates (4.2 mm yr−1) on Acropora-dominated reefs, demonstrating that carbonate budgets on these remote reefs have recovered rapidly from major climate-driven disturbances. Critically, these reefs retain the capacity to grow at rates exceeding measured regional mid-late Holocene and 20th century sea-level rise and close to IPCC sea-level rise projections through to 2100.


Warming sea waters, ocean acidification and rising sea levels are effects of climate that pose a major threat to coral reefs globally1,2. At a local scale, reefs are also under ever-growing pressure from multiple direct human disturbances, including eutrophication and over-fishing, as well as disease outbreaks3,4. The net effect of these cumulative disturbances has been to fundamentally change reef ecology, with many reefs exhibiting reduced coral cover, altered coral and reef-associated species abundances and diminished structural complexity5,6,7. On many disturbed reefs these changes are also now impacting the carbonate budgets of reefs8, defined as the balance between the rate at which carbonate is produced by corals, coralline algal and other carbonate producing processes, set against the rate at which carbonate is either denuded by biological erosion (‘bioerosion’), removed by physical processes, or chemically dissolved9. Where carbonate budgets are positive, reefs can maintain their physical three-dimensional structures and sustain high growth potential. However, under conditions of diminished production or increased bioerosion, carbonate budgets can become net negative, limiting reef growth and leading to reef structural collapse10. Such fundamental changes have now occurred across much of the Caribbean, where coral cover loss and community composition changes have caused both carbonate production and erosion rates to decline11,12, significantly diminishing reef growth potential8. Similar trajectories are predicted for many reefs globally due to local disturbances and exacerbated by climate change2,13,14.

Whilst many reefs have succumbed to the combined impacts of climate- and human-driven pressures, there remain regions largely free of direct human pressures due to their geographic remoteness. This raises the question of whether such reefs are better able to cope with global climate change impacts. The geographically isolated Chagos Archipelago, central Indian Ocean (Fig. 1), is one such region. It remains, with the exception of Diego Garcia, remote from direct human disturbance and has fish populations that can be considered semi-pristine15. While the mass coral bleaching event of 1998 caused severe damage to reefs in Chagos, they have demonstrated an impressive capacity for ecological recovery16. Here we use measured rates of both gross carbonate production and bioerosion from 28 reefs across 5 atolls in Chagos to determine their net biological carbonate budgets (G, where G = kg CaCO3m−2 yr−1) and use these data to address two important questions: 1) have these reefs proved sufficiently resilient to recent climatic disturbances to regain rates of carbonate production and erosion that can be considered typical of undisturbed Indo-Pacific reefs? 2) do these reefs retain the capacity to accrete at rates sufficient to offset projected increases in sea level?

Figure 1

Study sites and wave energy regimes.

(A) Location of the Chagos archipelago in the central Indian Ocean. Redrawn using Adobe Illustrator Version CS5 from Global and Planetary Change, Vol 82–83, R. P. Dunne et al. Contemporary sea level in the Chagos Archipelago, central Indian Ocean, p. 25–37, Copyright 2011, with permission from Elsevier; (B) Rose diagram showing the frequency and speed of winds (m s−1) affecting Chagos plotted based on the direction from which winds are generated. Plots based on hourly wind measurements from 1973 to 2001 obtained from Diego Garcia airport (n = 219,943); (C) Major islanded atolls (bold white font) and submerged platforms of the Chagos Archipelago and modelled wave exposures (Joules m−3). Numbered circles denote study sites, white fills are defined as ‘sheltered’ (<1000 J m−3), black fills as ‘exposed’ sites (>1000 J m−3): Diego Garcia - 1) Cannon Point, 2) Middle Island, 3) Horsborough Bay, 4) East Island, 5) Barton Point; Peros Banhos – 6) Ile Diamante, 7) Ile de la Passe, 8) Ile Poule, 9) Ile Gabrielle, 10) Ile Fouquet, 11) Grand Coquillage, 12) Petite Coquillage; Salomon – 13) Ile de Passe, 14) Ile Anglais north, 15) Ile Anglaise middle, 16) Ile Anglaise south, 17) Ile Takamaka, 18) Ile du Sel; Blenheim – 19) Blenheim west; Gt. Chagos Bank – 20) Nelson Island, 21) Danger Island, 22) Eagle Island south, 23) Eagle Island middle, 24) Eagle Island north, 25) Middle Brother, 26) South Brother west, 27) South Brother east; Egmont – 28) Egmont north east. Map generated in ArcMap 10.2.2 ( Atoll outlines were imported into ArcMap from the Millennium Coral Reef Mapping Project (UNEP-WCMC), which is publicly available data on the web at the Institute for Marine Remote Sensing (University of South Florida) website ( The dataset comprises 3 main components: (1) Millennium Coral Reef Mapping Project validated maps provided by the Institute for Marine Remote Sensing, University of South Florida (IMaRS/USF) and Institut de Recherche pour le Développement (IRD, Centre de Nouméa), with support from NASA; (2) Millennium Coral Reef Mapping Project unvalidated maps provided by the Institute for Marine Remote Sensing, University of South Florida (IMaRS/USF), with support from NASA. Unvalidated maps were further interpreted by UNEP-WCMC. Institut de Recherche pour le Développement (IRD, Centre de Nouméa) do not endorse these products; (3) Other data have been compiled from multiple sources by UNEP-WCMC and the WorldFish Centre in collaboration with WRI and TNC.


Net carbonate production rates across all reefs averaged +3.7 G, with rates at the individual reef scale ranging from +9.8 to −5.0 G. Most reefs (25/28, 89%) had net positive budgets and eight (29%) had budgets exceeding 5 G. Only 3 of the 28 reefs had net negative budgets (range: −0.3 to −5.0 G). There was, however, considerable heterogeneity in net G (Fig. 2A), with significant differences among reefs (F24,82 = 8.584, p < 0.001), although not among atolls (F3,82 = 2.192, p = 0.113). To explore the influence of wave exposure on carbonate budgets we compared averaged net and gross rates of production and erosion for sheltered and exposed reefs within each atoll, grouped based on wave energy regime. Average net G ranged from +0.2 to +6.0 G (Fig. 2A), with highest averages on reefs around both the ‘sheltered’ and ‘exposed’ margins of Peros Banhos (averages of +6.0 and +5.6 G respectively), from the ‘sheltered’ margin of Salomon (+5.0 G) and wave exposed sites on the Gt. Chagos Bank and Egmont (+5.4 G). Lowest net production rates were measured around the sheltered margins of Gt. Chagos Bank (+0.2 G) (Fig. 2A). Net G did not differ between sheltered and exposed sites within most atolls, the exception being the Gt. Chagos Bank, where exposed sites had significantly higher net G (atoll x exposure F3,21 = 6.054, p = 0.004).

Figure 2

Net and gross carbonate production and erosion rates and relationships to setting and exposure regime.

Box (median and 50% quantile) and whisker (95% quantile) plots showing (A) net and (B) gross carbonate production rates and (C) bioerosion rates for all sites and within each atoll. Atoll sites are grouped into “sheltered” and “exposed”; (D) Patterns in the net carbonate budgets of individual Chagos reefs assessed by correlation-based principle components analysis of log(x + 1) transformed and normalized environmental data. Eigenvectors of each ecological and physical variable are overlaid; (E) The linear regression and 95% confidence interval for the relationship between coral cover and the net reef carbonate budget at sites across Chagos. Sites are differentiated into those that are either Acropora-dominated, or Porites/Pocillopora-dominated.

The generally high and positive carbonate budgets are reflected in high rates of gross carbonate production (Fig. 2B) and bioerosion (Fig. 2C). Gross carbonate production averaged +6.6 G across all reefs, but differed significantly among reefs (F24,82 = 7.165, p < 0.001). Highest production rates were measured at Ile Poule on the sheltered margin of Peros Banhos (+11.2 G) and the lowest at Nelson at the northern margin of the Gt. Chagos Bank (+1.3 G), a reef with very low live coral cover (3.6%) as a result of recent (2015) Crown-of-Thorns starfish predation. Grouped- exposure/atoll average production ranged from +2.4 to +9.5 G (Fig. 2B) and significantly higher gross production rates were measured on the exposed compared to the sheltered Gt. Chagos Bank/Egmont reefs, while on Salomon production was significantly higher at the sheltered reefs (atoll x reef F3,21 = 7.689 , p = 0.001). Bioerosion rates averaged 3.4 G across all reefs, with grouped-exposure/atoll averages ranging from −2.0 to −4.2 G (Fig. 2C), though bioerosion did not vary significantly with exposure (F1,21 = 0.213, p = 0.673). Bioerosion rates were significantly different between reefs (F24,82 = 249.580, p < 0.001), but not between atolls (F3,82 = 1.212, p = 0.326). Highest rates were measured at Petite Coquillage, Peros Banhos (7.4 G) and the lowest at East Island, Diego Garcia (1.4 G) (see Supplementary Table S1).

To understand which taxa are driving between-site variations in carbonate budgets we assessed net G as a function of coral taxa abundance, reef structure and exposure regime. As wave exposure increased the relative abundance of more robust taxa, but especially of Porites sp. and Pocillopora (mainly P. eydouxi), typically increased (Fig. 2D). These taxa thus dominate on most high wave exposure reefs (Fig. 1C), which generally have lower net G rates (Fig. 2D). In contrast, high net G rates are associated with sites defined by reduced wave exposure and an increased relative abundance of tabular and branched Acropora spp. (Fig. 2D). Whilst sites dominated by Porites spp. and Pocillopora spp. exhibit a wide range of net budget states, we note that high positive budgets are a defining feature of reefs where carbonate production is driven primarily by Acropora spp. (Fig. 2E). Furthermore, we note that whilst all Acropora-dominated sites are likely to retain net positive budgets unless coral cover falls below only a few %, that the transition into net negative states will occur at much higher coral cover levels where Porites and Pocillopora dominate (Fig. 2E), reflecting their lower calcification and extension rates17.


Our estimates of contemporary carbonate production and bioerosion across Chagos indicate that most reefs have responded positively to the climate-driven mortality of 1998 in terms of their carbonate budgets. The 1998 bleaching event resulted in the mortality of ~90% of corals down to ~15 m depth in the northern atolls and to >40 m depth around Diego Garcia18, a pattern repeated on many Indian Ocean reefs19,20. Shallow and mid-depth branching species, particularly Acropora palifera and table corals including Acropora cytherea, were especially impacted21,22. Since 1998, however, coral cover has recovered relatively rapidly at most sites and coral cover was restored to 1996 levels by 201023. At the time of the present study (early 2015) we found that this coral recovery was reflected in generally high positive carbonate budgets on most reefs, with a third of surveyed reefs having net budgets in excess of 5 G. In addition, we note that our measured high coral production rates, which average around 6.9 G across sites and especially those reported from the Acropora-dominated reefs (average 8.4 G), are close to the production rates (range ~5 to 9 G) reported as typical for undisturbed Acropora-dominated Indo-Pacific fore-reef settings24. Thus, whilst it is reasonable to assume that the 1998 event would have significantly diminished the budgets of most Chagos reefs and especially those previously dominated by Acropora spp., contemporary rates have now recovered to be close to optimal for Indian Ocean reefs. This contrasts directly with the fundamental budget changes that persist at post-disturbance sites across the Caribbean, such that average carbonate production and erosion rates are higher (28% and 40% respectively) in Chagos relative to the Caribbean and with particularly high coral production rates resulting in net G being twice as high compared to the Caribbean (Fig. 3).

Figure 3

Comparisons between Chagos and the Caribbean.

Box (median and 50% quantile) and whisker (95% quantile) plots showing regional differences in net G, coral G, bioerosion G, parrotfish G and in accretion rates (mm yr−1) between Chagos and the Caribbean. Caribbean data from Perry et al.8,11,12.

We also note that on most reefs around Chagos carbonate production is predominantly driven by the same suite of coral genera; Acropora, Porites and Pocillopora, that dominated prior to the 1998 bleaching22. The relative abundance of these genera differs among sites, largely as a function of exposure regime, but they collectively contribute >70% on average of the coral carbonate being produced. We thus find no evidence for the persistence of widespread coral community changes such as have occurred on reefs across the Caribbean and at other less remote Indo-Pacific sites25,26,27. In the Caribbean these changes have resulted in shifts towards coral species that were not historically important framework builders12, a change that has long-term implications for reef functionality because these “novel” community states may have a high probability of persisting into the future28,29,30 and thus of locking reefs into lower carbonate budget states. However, whilst such transitions have not widely occurred on Chagos, ecological models predict any increase in extensive mortality events would have the capacity to drive such transitions31. It is thus pertinent to note the recent reports of partial mortality of colonies of A. cytherea at some Chagos sites32, a fact noted in our own studies in 2015 and that some sites have also been impacted in recent years by COTS outbreaks33. Of most immediate concern however is the potential for another major bleaching-induced die-off, with the widespread bleaching reported during the mid-2015 sea-surface temperature anomaly event a clear indicator of the potential for such events to re-occur.

Arising from these observations are two important and inter-related questions about the maintenance of reef structures under future climate change. Firstly, what are the implications of the generally rapid coral community rebound around Chagos for reef growth potential? Secondly, what capacity does this instil in these reefs to respond positively to rising sea levels? Evidence from the Caribbean suggests that reef growth potential in that region has diminished, with accretion rates (mm yr−1) an estimated order of magnitude lower than that measured in regional Holocene core records for equivalent depth assemblages8. In contrast, maximum potential accretion rates around Chagos average 2.3 mm yr−1 across all sites, but are higher (mean: 4.2 mm yr−1) within Acropora-dominated sites, compared to Porites/Pocillopora dominated sites (mean: 0.9 mm yr−1) (Fig. 4). Considerable between-site/atoll variability is also evident, with highest rates occurring on reefs along the sheltered margins of Peros Banhos (4.30 mm yr−1) and Salomon (3.74 mm yr−1) and on the Brothers reefs (Gt. Chagos Bank; 3.36 mm yr−1) (Fig. 4). The lowest rates occur at those few sites (Nelson Island and along the western margins of the Gt. Chagos Bank) where localised COTS outbreaks have caused recent coral mortality33. Viewed in the context of Indian Ocean Holocene reef growth, where shallow water accretion rates have averaged ~3.1 mm yr−1 over the last ~6,500 years34, our datasets suggest that the current prognosis in terms of reef growth potential around Chagos and especially for the Acropora-dominated reefs, is positive.

Figure 4

Reef accretion potential around Chagos and sea level trends and projections.

Mean (black bar) and the maximum and minimum potential vertical accretion rates (mm yr−1) for each site in Chagos (sites are ranked by increasing wave exposure within atolls) and shown relative to global and regional sea-level rise rates as follows: (A) Holocene trend from ~7,500 − 3,000 yBP45; (B) Average global rise rate over last 50 years (Church et al. 2013)46; (C) Range of measured rates around Chagos 1993 to 201143,44; (D) Average global rise rate over last 20 years35; E. Average predicted rise rate for the central Indian Ocean by 2100 under RCP 4.535 and accounting for regional wind stress35. Site numbers as follows: 1. Cannon Pt, DG; 2. Middle Isld; DG, 3. Horsborough Bay, DG; 4. East Island, DG; 5. Barton Pt, DG; 6. Ile Diamante, PB; 7. Ile de la Passe, PB; 8. Ile Poule, PB; 9. Ile Gabrielle, PB; 10. Ile Fouquet, PB; 11. Grand Coquillage, PB; 12. Petite Coquillage, PB; 13. Ile Anglaise south, Sal; 14. Ile Anglaise middle, Sal; 15. Blenheim; 16. Ile Anglaise north, Sal; 17. Ile de Passe, Sal; 18. Ile du Sel, Sal; 19. Ile Takamaka, Sal; 20. Nelson, GCB; 21. Danger, GCB; 22. Eagle south, GCB; 23. Eagle middle, GCB; 24. Eagle north, GCB; 25. Egmont; 26. Middle Brother, GCB; 27. S. Brother west, GCB; 28. S. Brother east, GCB.

Predicting reef structural integrity and growth potential under present and future sea-level rise scenarios is more problematic and depends on the interaction between reef accretion potential (driven partly by reef ecology) and sea-level rise rates. A comparison of our accretion rate estimates against recent regional sea-level trends indicates that many Chagos reefs, including all those dominated by Acropora spp., should have the potential to accrete at rates above those measured using sea level altimetry data over the period 1950 to 2000 (Fig. 4). Projecting into the future, the IPCC AR5 report projects a global mean sea-level rise rate by 2081-2100 of a little above 4 mm yr−1 for the central Indian Ocean under scenario RCP 4.535 and accounting for regional wind-stress36. These rates are close to the average potential vertical accretion rates measured across our Acropora dominated sites (~4.2 mm yr−1), suggesting that even under these elevated rise rates that most Acropora-dominated reefs have the potential to closely track rising sea-levels over the coming century. However, higher rates predicted under RCP 6.0 and 8.5 scenarios would lead to a slight deepening (in the order of a few decimetres) over the fore-reef slope habitats by 2100.

There are, however, two important caveats that need consideration here. The first is that Acropora sp. tend to be highly susceptible to episodic disturbances26,27 and, as noted, localised partial mortality has recently impacted colonies of A. cytherea32. Thus carbonate budgets (and resultant accretion rates) may be inherently more dynamic over time on reefs dominated by such corals, compared to those where Porites and Pocillopora spp. drive carbonate production. Long-term potential accretion rates may therefore not be so different between the two, especially where coral cover and thus carbonate production (see Fig. 3E), is high. However, an additional contributing factor will be the rate of physical removal of framework which will, to varying degrees, reduce reef accretion. There is little data with which to parameterise models of physical reef framework removal but, using data on background rates from the Maldives38, albeit from a different reefal setting, a reasonable estimate is that along sheltered reef margins about 20% of annual framework produced may be lost (compared to >50% along exposed margins). Assuming similar attrition rates this would lower average accretion on Acropora-dominated reefs to ~2.9 mm yr−1 (range 2.3 to 4.5 mm yr−1). Thus, even accounting for framework removal the best available estimates would suggest that most ‘sheltered’ reefs will retain the capacity, providing Acropora cover is maintained, to accrete at rates above those measured across the region over the last ~50–60 years and within or close to the rates projected for the next 100 years (Fig. 4). In contrast, it seems reasonable to assume that a high proportion of the carbonate produced from the upper shelf areas along the exposed atoll margins will be removed by physical processes. Indeed, we note that all the exposed margin sites lack Holocene framework, suggesting a situation of long-term carbonate export dominance in these settings. However, we also note that this has not previously inhibited reef flat and reef island development on these high energy margins and thus conclude that continued coral health and carbonate productivity along these exposed margins will remain essential for supplying rubble and sediment39 to maintain these reef flats and islands.

Collectively, these findings highlight the capacity of the Chagos reefs, which are both geographically remote and isolated from compounding human impacts, to not only recover their ecological and geomorphic functions relatively rapidly following major past climate-driven perturbations, but also to retain the capacity to respond positively to future increases in sea level. Clear differences in accretion potential occur between sites, largely reflecting reef ecology and wave exposure regimes, but the highest accretion rates presently occur predominantly on those reefs where Acropora-drives carbonate production and which are mostly along sheltered atoll margins. A key implication of this is that the capacity of reefs to track projected sea-level rise is generally lost (and certainly threatened) in the absence of Acropora, although we must assume, given the higher susceptibility of Acropora spp. to episodic disturbance, that the accretion potential of such reefs may inherently fluctuate over time. This raises an important note of warning in relation to any increase in the magnitude and frequency of disturbance events, since these would most likely preferentially impact those coral taxa with the highest growth rates17 and which thus have the greatest capacity to maintain high reef accretion rates. The developing “third global bleaching event”40 provides a clear indication of the immediacy of such threats. Actions aimed at reducing the effects of local disturbances on reefs are thus critical to provide any buffering for reefs from climate-change and to instil any capacity to maintain their accretion potential that so critically underpins the provisioning of most ecosystem services.


Surveys were conducted during March/April 2015 on 28 reefs across the five islanded atolls of the Chagos Archipelago (numbers of survey sites in brackets): Diego Garcia (5); Peros Banhos (7), Salomon (6), Great Chagos Bank (8) and Egmont (1), as well as at one site on the submerged Blenheim Reef (Fig. 1C). A seasonally-shifting wind regime, with the predominant wind direction being from the south-east (Fig. 1B), results in marked spatial variations in wave energy around Chagos. Our site selection strategy was driven by a desire to survey sites on both the more sheltered (the south-west, western and northern margins of the atolls and those on the more exposed margins (the north-east, east and south-eastern margins), as well as integrating sites that had been the focus of earlier ecological surveys. To enable us to classify these sites on the basis of their wave exposure regime, spatially explicit estimations of wave exposure were modelled as a function of wind speed and direction and fetch length (i.e. the distance over open ocean that wind can travel in a specific direction unobstructed by land or reefs) (see SI Methods). Based on these model outputs (Fig. 1C) we thus classify our sites into ‘exposed’ (>1000 J m−3) or ‘sheltered’ (<1000 J m−3), this division being based on a natural break in the rank order of the data across all sites. We refer to these groupings in the text for descriptive purposes.

To quantify gross carbonate production and erosion and thus to determine net carbonate budgets (G, where G = kg CaCO3 m2 yr−1) we used a modified version of the Reef Budget41 methodology (see SI Methods). At each site, surveys were conducted at a depth of 8–10 m i.e., a little above the upper shelf break and with replicate transects established running parallel to the reef crest, with a spacing of ~5 m between transects. With only two exceptions we collected data along 4 replicate transects at each site (the exceptions being Middle Island (n = 5) and Cannon Point (n = 3) on Diego Garcia). At the same time these surveys allowed us to collect data on substrate composition and reef rugosity as a function of the 3-dimensional surface of the reefs (see SI Methods). Based on these data we define Acropora spp. dominated and Porites/Pocillopora spp. dominated reefs as those where these taxa contribute to >50% of coral carbonate production. To test for differences in net and gross production and erosion between sites and atolls ANOVA tests were run with, where appropriate, a Tukey post-hoc test. Principal Component Analysis (PCA) was used to explore the relationships between reef carbonate production rates and reef ecology, physical structure and exposure regime.

To assess the accretion potential of reefs and to explore their capacity to respond to future projected regional sea-level rise rates, we converted our net production rate estimates to potential accretion rates (mm yr−1). We used an approach previously applied to Caribbean reefs8 that accounts for both framework carbonate production and sediment reincorporation from reef bioeroding taxa, but was modified to also factor for variations in accumulating framework porosity as a function of between-site variations in reef community composition42 (see SI Methods). Resultant reef accretion rates were compared to recent rates of sea level rise based on satellite altimetry data from the central Indian Ocean region over the period 1950–200043 and 1950–200944 (see SI Methods). To compare contemporary reef accretion potential to future sea-level rise trajectories we used the IPCC AR5 report projections for the period 2081–210035, based on scenario RCP 4.5 but also accounting for the impacts of future wind-stress36.

Additional Information

How to cite this article: Perry, C. T. et al. Remote coral reefs can sustain high growth potential and may match future sea-level trends. Sci. Rep. 5, 18289; doi: 10.1038/srep18289 (2015).


  1. Hughes, T. P. et al. Climate change, human impacts and the resilience of coral reefs. Science 301, 929–933 (2003).

    CAS  ADS  Article  Google Scholar 

  2. Hoegh-Guldberg, O. et al. Coral reefs under rapid climate change and ocean acidification. Science 318,1737–1742 (2007).

    CAS  ADS  Article  Google Scholar 

  3. Hughes, T. P. Catastrophes, phase shifts and large-scale degradation of a Caribbean coral reef. Science 265, 1547–1551 (2003).

    ADS  Article  Google Scholar 

  4. Fabricius, K. E. Effects of terrestrial runoff on the ecology of corals and coral reefs: review and synthesis. Marine Pollution Bulletin 51, 125–146 (2005).

    Article  Google Scholar 

  5. Gardner, T. A., Côté, I. M., Gill, J. A., Grant, A. & Watkinson, A. R. Long-term region-wide declines in Caribbean corals. Science 301, 958–960 (2003).

    CAS  ADS  Article  Google Scholar 

  6. Alvarez-Filip, L., Dulvy, N. K., Gill, J. A., Côté, I. M. & Watkinson, A. R. Flattening of Caribbean coral reefs: region-wide declines in architectural complexity. Proceedings of Royal Society B 276, 3019–3025 (2009).

    Article  Google Scholar 

  7. Graham, N. A. J., Jennings, S., MacNeil, M. A., Mouillot, D. & Wilson, S. K. Predicting climate-driven regime shifts versus rebound potential in coral reefs. Nature 518, 94–97 (2015).

    CAS  ADS  Article  Google Scholar 

  8. Perry, C. T. et al. Caribbean-wide decline in carbonate production threatens coral reef growth. Nature Communications, doi: 10.1038/ncomms2409 (2013).

  9. Perry, C. T., Spencer, T. & Kench, P. Carbonate budgets and reef production states: a geomorphic perspective on the ecological phase-shift concept. Coral Reefs 27, 853–866 (2008).

    ADS  Article  Google Scholar 

  10. Eakin, C. Where have all the carbonates gone? A model comparison of calcium carbonate budgets before and after the 1982-1983 El Nino at Uva Island in the eastern Pacific. Coral Reefs 15, 109–119 (1996).

    ADS  Google Scholar 

  11. Perry, C. T. et al. Changing dynamics of Caribbean reef carbonate budgets: emergence of reef bioeroders as critical controls on present and future reef growth potential. Proceedings of the Royal Society B 281, 2014–2018 (2014).

    Article  Google Scholar 

  12. Perry, C. T. et al. Regional-scale dominance of non-framework building corals on Caribbean reefs affects carbonate production and future reef growth. Global Change Biology 21, 1153–1164 (2015).

    ADS  Article  Google Scholar 

  13. Veron, J. E. N. et al. The coral reef crisis: The critical importance of &lt;350 ppm CO2 . Marine Pollution Bulletin 58, 1428–1436 (2009).

    CAS  Article  Google Scholar 

  14. Kennedy, E. V. et al. Avoiding coral reef functional collapse requires combined local and global action. Current Biology 23, 912–918 (2013).

    CAS  Article  Google Scholar 

  15. Graham, N. A. J. & McClanahan, T. R. The last call for marine wilderness? BioScience 63, 397–402 (2013).

    Article  Google Scholar 

  16. Sheppard, C. R. C. et al. In coral reefs of the United Kingdom Overseas Territories, coral reefs of the World 4 (ed. Sheppard C. R. C. ), Ch. 17, 241–253 (Springer, 2013) coral reefs of the Chagos Archipelago, Indian Ocean.

  17. Pratchett, M. S. et al. Spatial, temporal and taxonomic variation in coral growth – implications for the structure and function of coral reef ecosystems. Oceanography and Marine Biology: An Annual Review 53, 215–295 (2015).

    Google Scholar 

  18. Sheppard, C. R. C. Coral decline and weather patterns over 20 year in the Chagos archipelago, central Indian Ocean. Ambio 28, 472–478 (1999).

    Google Scholar 

  19. Graham, N. A. J. et al. Climate warming, marine protected areas and the ocean-scale integrity of coral reef ecosystems. PLoS One 3, e3039 (2008).

    ADS  Article  Google Scholar 

  20. Ateweberhan, M., McClanahan, T. R., Graham, N. A. J. & Sheppard, C. R. C. Episodic heterogeneous decline and recovery of coral cover in the Indian Ocean. Coral Reefs 30, 739–752 (2011).

    ADS  Article  Google Scholar 

  21. Sheppard, C. R. C. Coral cover, zonation and diversity on reef slopes of Chagos atolls and population structures of the major species. Marine Ecology Progress Series 2, 193–205 (1980).

    ADS  Article  Google Scholar 

  22. Sheppard, C. R. C. In Ecology of the Chagos archipelago (eds Sheppard, C. R. C. & Seaward, M. R. D. ), Ch. 7, 91–100 (Linnean Society/Westburg, 1999), Changes in coral cover on reefs of Chagos over eighteen years.

  23. Sheppard, C. R. C. et al. Reefs and islands of the Chagos archipelago, Indian Ocean: why it is the world’s largest no-take marine protected area. Aquatic Conservation: Marine and Freshwater Ecosystems 22, 232–261 (2012).

    CAS  Google Scholar 

  24. Vecsei, A. A new estimate of global reefal carbonate production including the fore-reefs. Global and Planetary Change 43, 1–18 (2004).

    ADS  Article  Google Scholar 

  25. Loya, Y. et al. Coral bleaching: the winners and the losers. Ecology Letters 4, 122–131 (2001).

    Article  Google Scholar 

  26. McClanahan, T. R., Baird, A. H., Marshall, P. A. & Toscano, M. A. Comparing bleaching and mortality responses of hard corals between southern Kenya and the Great Barrier Reef, Australia. Marine Pollution Bulletin 48, 327–335 (2004).

    CAS  Article  Google Scholar 

  27. Pratchett, M. S., McCowan, D., Maynard, J. A. & Heron, S. F. Changes in bleaching susceptibility among corals subject to ocean warming and recurrent bleaching in Moorea, French Polynesia. PLoS One 8, e70443 (2013).

    CAS  ADS  Article  Google Scholar 

  28. Côté, I. M. & Darling, E. S. Rethinking ecosystem resilience in the face of climate change. PLoS Biol 8, e1000438 (2010).

    Article  Google Scholar 

  29. Graham, N. A. J., Cinner, J. E., Norström, A. V. & Nyström, M. Coral reefs as novel ecosystems: embracing new futures. Current Opinions in Environmental Sustainability 7, 9–14 (2014).

    Article  Google Scholar 

  30. Yakob, L. & Mumby, P. J. Climate change induces demographic resistance to disease in novel coral assemblages. Proceedings of National Academy of Science 108, 1967–1969 (2011).

    CAS  ADS  Article  Google Scholar 

  31. Riegl, B., Sheppard, C. R. C. & Purkis, S. J. Human impact on atolls leads to coral loss and community homogenisation: a modelling study. PLoS One 7, e36921 (2012).

    CAS  ADS  Article  Google Scholar 

  32. Pratchett, M. S., Pisapia, C. & Sheppard, C. R. C. Background mortality rates for recovering populations of Acropora cytherea in the Chagos Archipelago, central Indian Ocean. Marine Environmental Research 86, 29–34 (2013).

    CAS  Article  Google Scholar 

  33. Roche, R. C. et al. Localized outbreaks of Acanthaster planci at an isolated and unpopulated reef atoll in the Chagos Archipelago. Marine Biology 162, 1695–1704 (2015).

    Article  Google Scholar 

  34. Montaggioni, L. F. History of Indo-Pacific coral reef systems since the last glaciation: development patterns and controlling factors. Earth-Science Reviews 71, 1–75 (2005).

    ADS  Article  Google Scholar 

  35. Church, J. A. et al. In Climate Change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change. (eds Stocker, T. F. et al. ). Ch. 13, 1137–1216 (Cambridge University Press, 2013). Sea Level Change.

  36. Timmermann, A., McGregor, S. & Jin, F. F. Wind effects on pastand future regional sea level trends in the southern Indo-Pacific. Journal of Climate 23, 4429–4437 (2010).

    ADS  Article  Google Scholar 

  37. McClanahan, T. R. et al. Western Indian Ocean coral communities: bleaching responses and susceptibility to extinction. Marine Ecology Progress Series 337, 1–13 (2007).

    ADS  Article  Google Scholar 

  38. Morgan, K. M. & Kench, P. S. A detrital sediment budget of a Maldivian reef platform. Geomorphology 222, 122–131 (2014).

    ADS  Article  Google Scholar 

  39. Perry, C. T., Kench, P. S., O’Leary, M. J., Morgan, K. M. & Januchowski-Hartley, F. Linking reef ecology to island-building: Parrotfish identified as major producers of island-building sediment in the Maldives. Geology 43, 503–506 (2015).

    ADS  Article  Google Scholar 

  40. Witze, A. Corals worldwide hit by bleaching (October 2015) (Date accessed: 19/10/2015)

  41. Perry, C. T. et al. Estimating rates of biologically driven coral reef framework production and erosion: a new census-based carbonate budget methodology and applications to the reefs of Bonaire. Coral Reefs 31, 853–868 (2012).

    ADS  Article  Google Scholar 

  42. Kinsey, D. W. & Hopley, D. The significance of coral reefs as global carbon sink-response to greenhouse. Palaeogeography, Palaeoclimatology, Palaeoecology 89, 363–377 (1991).

    ADS  Article  Google Scholar 

  43. Palanisamya, H. et al. Regional sea level variability, total relative sea level rise and its impacts on islands and coastal zones of Indian Ocean over the last sixty years. Global and Planetary Change 116, 54–67 (2014).

    ADS  Article  Google Scholar 

  44. Dunne, R. P., Barbosa, S. M. & Woodworth, P. L. Contemporary sea level in the Chagos Archipelago, central Indian Ocean. Global and Planetary Change 82-83, 25–37 (2012).

    ADS  Article  Google Scholar 

  45. Camoin, G. F., Montaggioni, L. F. & Braithwaite C. J. R. Late glacial to post glacial sea levels in the Western Indian Ocean. Marine Geology 206, 119–146 (2004).

    ADS  Article  Google Scholar 

  46. Church, J. A., White, N. J. & Hunter, J. R. Sea-level rise at tropical Pacific and Indian Ocean islands. Global and Planetary Change 53, 155–168 (2006).

    ADS  Article  Google Scholar 

Download references


Field research was supported by DEFRA Darwin Initiative grant 19-027, ‘Darwin Initiative to strengthen the world’s largest Marine Protected Area, Chagos Archipelago’ and John Turner (Bangor) and Charles Sheppard (Warwick) are thanked for coordinating the 2015 research cruise. NAJG was additionally supported by Australian Research Council grant DE130101705, FAJ-H through an Ecosystem Services for Poverty Alleviation (ESPA) grant ‘Sustainable Poverty Alleviation from Coastal Ecosystem Services (SPACES)’ (project NE-K010484-1) and HKE by Natural Environment Research Council Studentship NE/K500902/1 . We acknowledgement the invaluable support of The Chagos Conservation Trust, the Foreign and Commonwealth Office BIOT section and the Captain and crew of the MV Pacific Marlin. Philip Woodworth (Southampton) is thanked for discussions on past sea-level trends.

Author information




C.T.P. initiated the study, collected and analysed the field data. G.M., N.A.J.G. and S.K.W. helped collect and analyse the field data. F.A.J.-H. contributed to field methodology development. H.E. developed the wave exposure model. All authors contributed to manuscript writing.

Ethics declarations

Competing interests

The authors declare no competing financial interests.

Electronic supplementary material

Rights and permissions

This work is licensed under a Creative Commons Attribution 4.0 International License. The images or other third party material in this article are included in the article’s Creative Commons license, unless indicated otherwise in the credit line; if the material is not included under the Creative Commons license, users will need to obtain permission from the license holder to reproduce the material. To view a copy of this license, visit

Reprints and Permissions

About this article

Verify currency and authenticity via CrossMark

Cite this article

Perry, C., Murphy, G., Graham, N. et al. Remote coral reefs can sustain high growth potential and may match future sea-level trends. Sci Rep 5, 18289 (2015).

Download citation

Further reading


By submitting a comment you agree to abide by our Terms and Community Guidelines. If you find something abusive or that does not comply with our terms or guidelines please flag it as inappropriate.


Quick links

Nature Briefing

Sign up for the Nature Briefing newsletter — what matters in science, free to your inbox daily.

Get the most important science stories of the day, free in your inbox. Sign up for Nature Briefing