Widespread coral bleaching events

From ClimateWiki

Jump to: navigation, search

From Climate Change Reconsidered, a work of the Nongovernmental International Panel on Climate Change


Relation to Global Warming

Hoegh-Guldberg (1999) concluded that “coral bleaching is due to warmer than normal temperatures” and that “increased sea temperature is the primary reason for why coral bleaching has occurred with increasing intensity and frequency over the past two decades.” As outlined in the preceding sections, there is some evidence that points toward these conclusions, but there is much other evidence that points to alternative possibilities.

Consider, for example, the persistence of coral reefs through geologic time, which provides substantive evidence that these ecological entities can successfully adapt to a dramatically changing global environment (Veron, 1995). What can their history tell us about bleaching and global warming in our day?

The earliest coral reefs date to the Palaeozoic Era, over 450 million years ago (Hill, 1956). The scleractinian corals, which are the major builders of the reefs of today (Achituv and Dubinsky, 1990), appeared in the mid-Triassic some 240 million years later (Hill, 1956), when the earth was considerably warmer than it is currently (Chadwick-Furman, 1996). Although reef-building ceased for a time following the extinctions at the end of the Triassic, the Scleractinia came back with a vengeance during the Jurassic (Newell, 1971; Veron, 1995); they continued to exhibit great robustness throughout the Cretaceous, even when temperatures were as much as 8-15°C higher (Chadwick-Furman, 1996; Veizer et al., 1999), and atmospheric CO2 concentrations two to seven times higher (Berner and Kothavala, 2001), than present.

At the end of the Cretaceous, 70 percent of the genera and one-third of the families of scleractinian corals disappeared (Veron, 1995) in the greatest biospheric extinction event in geological history, which may possibly have been caused by a large asteroid impact (Alvarez et al., 1980, 1984). They developed again, however, throughout the Cenozoic, particularly the Oligocene and Miocene (Chadwick-Furman, 1996). Finally, throughout the past two million years of the Pleistocene, they survived at least seventeen glacial-interglacial cycles of dramatic climate change and sea-level fluctuation, successfully adapting, over and over again, to these enormous environmental challenges (Pandolfi, 1999). In the words of Benzie (1999), this evidence suggests that “coral reef communities are relatively resilient, have survived previous global climate change, and appear likely to survive future changes.” This conclusion leads us to wonder why corals should be succumbing to global warming now.

To answer such an inquiry we must first address the question of what is “normal” for coral reefs in our day. Is it what they look like now? Or what they looked like 30 years ago? Or 300 years ago? Kinzie (1999) has emphatically stated that “it is clear that the definition of a healthy reef as ‘what it looked like when I started diving’ is fraught not only with hubris but strong temporal bias.” Indeed, as Greenstein et al. (1998a) have observed, “it must be demonstrated that the classic reef coral zonation pattern described in the early days of coral reef ecology, and upon which ‘healthy’ versus ‘unhealthy’ reefs are determined, are themselves representative of reefs that existed prior to any human influence.” Only when this criterion is met will we have, in the words of Greenstein et al. (1998b), a good replacement for “the temporally myopic view afforded by monitoring studies that rarely span a scientific career.” Clearly, therefore, there should be no argument over the key fact that we need a proper understanding of the past to correctly judge the present if we ever are to foretell the future.

In an attempt to obtain a true picture of pristine coral conditions in the western North Atlantic and Caribbean, Greenstein et al. (1998a, 1998b) conducted systematic censuses of “life assemblages” and “death assemblages” of corals on healthy modern patch reefs and compared the results with similar censuses they conducted on “fossil assemblages” preserved in Pleistocene limestones in close proximity to the modern reefs. The data revealed a recent decline in thickets of Acropora cervicornis, as evidenced by their abundance in the death assemblage, and a concurrent increase in Porites porites, as evidenced by their abundance in the life assemblage. In comparing these results with those obtained from the fossil assemblage, they found that the present Caribbean-wide decline of A. cervicornis is “without historical precedent” and that it is a dramatic departure from “the long-term persistence of this taxon during Pleistocene and Holocene Optimum time,” when “intensifying cycles in climate and sea level” recurred throughout a roughly one-million-year time period.

These observations, along with the similar findings of Jackson (1992) and Aronson and Precht (1997), suggest that if little change in coral community structure occurred throughout the Pleistocene—when it was often warmer than it is now (Petit et al., 1999)—the recent die-off of A. cervicornis cannot be due to global warming alone, or even primarily, for this particular coral has clearly weathered several major episodes of global warming and elevated water temperatures in the past with no adverse consequences. Neither can the coral’s die-off be due to the CO2-induced decrease in seawater calcium carbonate saturation state that might possibly be occurring at the present time (see the section later in this chapter on coral calcification); for the air’s CO2 content has not risen sufficiently to have caused this parameter to decline enough to significantly impact reef coral calcification rates (Gattuso et al., 1998, 1999), as is also demonstrated by the opportunistic replacement of A. cervicornis by P. porites. In addition, in their detailed reconstruction of the history of calcification rates in massive Porites colonies from Australia’s Great Barrier Reef, Lough and Barnes (1997) report that the mid-twentieth century had the second highest coral growth rate of the past 237 years. Hence, although A. cervicornis has indeed suffered an extreme decrease in abundance throughout the Caribbean in recent years (Hughes, 1994), its precipitous decline cannot be attributed to either global warming or the direct effects of rising CO2.

In light of these data-driven considerations, Greenstein et al. (1998a, 1998b) have attributed the increasing coral bleaching of the past two decades to a host of local anthropogenic impacts. This conclusion is accepted in a much wider context as well, as Buddemeier and Smith (1999) have noted that “reviews of the problems facing coral reefs have consistently emphasized that local and regional anthropogenic impacts are a far greater immediate threat to coral reefs than Greenhouse-enhanced climate change.”

An Alternative Hypothesis

The preceding considerations clearly indicate global warming cannot be the primary cause of the massive coral bleaching the earth has experienced in recent years. However, the IPCC tenaciously clings to this hypothesis because (1) no significant massive and widespread coral bleaching was reported in the 1970s and (2) the global warming hypothesis can account for this observation. Specifically, Hoegh-Guldberg (1999) has suggested that the reason “why mass bleaching events are not seen prior to 1980” is that “increases in sea temperatures have only become critical since in the 1980s, when El Niño disturbances began to exceed the thermal tolerances of corals and their zooxanthellae” as a result of global warming increasing the background temperature to which El Niño thermal effects are added.

This reasoning assumes no other theory is capable of accounting for the fact that modern mass bleaching events did not begin to occur until 1980. On the basis of this assumption, Hoegh-Guldberg (1999) concludes that the global warming hypothesis must be correct, even in light of the many problems associated with it. This assumption, however, is not true, for there are other ways of satisfying this critical criterion that do account for the lack of bleaching episodes before 1980, which we describe below.

The North Atlantic Oscillation (NAO) is responsible for multiannual to decadal variability in Northern Hemispheric climate that is numerically represented by the pressure difference between the Azores high and the Icelandic low (Dugam et al., 1997). It has been documented over the past 350 years in Greenland ice core reconstructions (Appenzeller et al., 1998) and explicitly quantified from 1864 through 1994 via actual pressure records (Hurrell, 1995), which have been updated through 1998 by Uppenbrink (1999).

Plots of these NAO datasets reveal a shift from strong negative index values in the 1950s and 1960s to what Hurrell (1995) describes as “unprecedented strongly positive NAO index values since 1980.” This observation is especially important, for during times of high NAO index values, there is a significant reduction in atmospheric moisture transport across southern Europe, the Mediterranean, and north Africa (Hurrell, 1995); and Richardson et al. (1999) note that this phenomenon has led to the development of prolonged drought in the Sahel region of Africa since the NAO shift to positive index values in 1980.

One consequence of this drought has been a gradual increase in the dust content of the atmosphere, which in some areas has grown to five-fold what was deemed normal prior to this climatic transition (Richardson et al., 1999). Of particular significance to corals is the fact that this airborne dust carries bacteria, viruses, and fungi that can kill them. Pearce (1999) notes that outbreaks of a number of coral diseases “have coincided with years when the dust load in the atmosphere was highest.” In 1983, for example—when the NAO index reached its highest value since 1864 (Hurrell, 1995) and the atmosphere was exceptionally dusty—a soil fungus of the Aspergillus genus appeared in the Caribbean, initiating an onslaught of soft coral sea fans that has now destroyed more than 90 percent of them. Pearce (1999) notes there are solid scientific reasons for concluding that “the speed and pattern of the fungus’s spread indicates that it could only have arrived on the trade winds from Africa.”

In addition to carrying its deadly biological cargo, the positive-NAO-induced airborne dust is rich in iron, which extra supply, in the words of R.T. Barber as quoted by Pearce (1999), “may have spurred the worldwide growth of a variety of invader organisms harmful to coral ecosystems.” Such iron-rich dust has the capacity to fertilize algae that compete with zooxanthellae for other scarce nutrients and reef living space. Abram et al. (2003), for example, reported that a massive coral bleaching event that killed close to 100 percent of the coral and fish in the reef ecosystem of the Mentawai Islands (located southwest of Sumatra, Indonesia, in the equatorial eastern Indian Ocean) in 1997-1998 was brought about by an anomalous influx of iron provided by atmospheric fallout from the 1997 Indonesian wildfires, which they describe as being “the worst wildfires in the recorded history of southeast Asia.” The enhanced burden of iron, in turn, spawned a large phytoplankton bloom that likely caused the coral and fish death via asphyxiation. In concluding their paper, Abram et al. warn that “widespread tropical wildfire is a recent phenomenon, the magnitude and frequency of which are increasing as population rises and terrestrial biomass continues to be disrupted,” and “reefs are likely to become increasingly susceptible to large algal blooms triggered by episodic nutrient enrichment from wildfires,” which phenomenon, in their words, “may pose a new threat to coastal marine ecosystems that could escalate into the 21st century.”

The timeline for the appearance and progression of these several related phenomena matches perfectly with the timeline of the historical buildup of modern coral reef bleaching throughout the 1980s and 1990s. This is not to say, however, that these aggregate phenomena comprise the entire answer to the problem to the exclusion of all other possible causes, even including global warming. We only suggest that they, too, must be seriously considered in attempts to identify the true cause or causes of this development in coral reef history.

Although one can make the case for coral bleaching being caused by global warming, there are too many pieces of evidence that contradict this hypothesis for it to be deemed the sole, or even primary, cause of this modern problem. There is at least one alternative explanation—the unprecedented, strongly positive NAO since 1980—during the past two decades.


Abram, N.J., Gagan, M.K., McCulloch, M.T., Chappell, J. and Hantoro, W.S. 2003. Coral reef death during the 1997 Indian Ocean Dipole linked to Indonesian wildfires. Science 301: 952-955.

Achituv, Y., and Dubinsky, Z. 1990. Evolution and zoogeography of coral reefs. Dubinsky, Z. (Ed.) Ecosystems of the world: Coral reefs. Elsevier, New York, NY.

Alvarez, L.W., Alvarez, W., Asaro, F. and Michel, H.V. 1980. Extraterrestrial cause for the Cretaceous-Tertiary extinction. Science 208: 1095-1108.

Alvarez, W., Alvarez, L.W., Asaro, F. and Michel, H.V. 1984. The end of the Cretaceous: Sharp boundary or gradual transition? Science 223: 1183-1186.

Appenzeller, C., Stocker, T.F. and Anklin, M. 1998. North Atlantic Oscillation dynamics recorded in Greenland ice cores. Science 282: 446-449.

Aronson, R.B. and Precht, W.F. 1997. Stasis, biological disturbance, and community structure of a Holocene coral reef. Paleobiology 23: 326-346.

Benzie, J.A.H. 1999. Genetic structure of coral reef organisms: Ghosts of dispersal past. American Zoologist 39: 131-145.

Berner, R.A. and Kothavala, Z. 2001. GEOCARB III: A revised model of atmospheric CO2 over phanerozoic time. American Journal of Science 301: 182-204.

Buddemeier, R.W. and Smith, S.V. 1999. Coral adaptation and acclimatization: A most ingenious paradox. American Zoologist 39: 1-9.

Chadwick-Furman, N.E. 1996. Reef coral diversity and global change. Global Change Biology 2: 559-568.

Climate Change Reconsidered: Website of the Nongovernmental International Panel on Climate Change. http://www.nipccreport.org/archive/archive.html

Dugam, S.S., Kakade, S.B. and Verma, R.K. 1997. Interannual and long-term variability in the North Atlantic Oscillation and Indian summer monsoon rainfall. Theoretical and Applied Climatology 58: 21-29.

Gattuso, J.-P., Allemand, D. and Frankignoulle, M. 1999. Photosynthesis and calcification at cellular, organismal and community levels in coral reefs: A review on interactions and control by carbonate chemistry. American Zoologist 39: 160-183.

Gattuso, J.-P., Frankignoulle, M., Bourge, I., Romaine, S. and Buddemeier, R.W. 1998. Effect of calcium carbonate saturation of seawater on coral calcification. Global and Planetary Change 18: 37-46.

Greenstein, B.J., Curran, H.A. and Pandolfi, J.M. 1998a. Shifting ecological baselines and the demise of Acropora cervicornis in the western North Atlantic and Caribbean Province: A Pleistocene perspective. Coral Reefs 17: 249-261.

Greenstein, B.J., Harris, L.A. and Curran, H.A. 1998b. Comparison of recent coral life and death assemblages to Pleistocene reef communities: Implications for rapid faunal replacement on recent reefs. Carbonates & Evaporites 13: 23-31.

Hill, D. Rugosa and Moore, R.D. 1956. (Eds.) Treatise on invertebrate paleontology, Volume F, Coelenterata. Lawrence, KS: Geological Society of America/University of Kansas Press, pp. 233-323.

Hoegh-Guldberg, O. 1999. Climate change, coral bleaching and the future of the world’s coral reefs. Marine and Freshwater Research 50: 839-866.

Hughes, T.P. 1994. Catastrophes, phase shifts, and large-scale degradation of a Caribbean coral reef. Science 265: 1547-1551.

Hurrell, J.W. 1995. Decadal trends in the North Atlantic Oscillation: Regional temperatures and precipitation. Science 269: 676-679.

Jackson, J.B.C. 1992. Pleistocene perspectives on coral reef community structure. American Zoologist 32: 719-731.

Kinzie III, R.A. 1999. Sex, symbiosis and coral reef communities. American Zoologist 39: 80-91.

Lough, J.M. and Barnes, D.J. 1997. Several centuries of variation in skeletal extension, density and calcification in massive Porites colonies from the Great Barrier Reef: A proxy for seawater temperature and a background of variability against which to identify unnatural change. Journal of Experimental Marine Biology and Ecology 211: 29-67.

Newell, N.D. 1971. An outline history of tropical organic reefs. Novitates 2465: 1-37.

Pandolfi, J.M. 1999. Response of Pleistocene coral reefs to environmental change over long temporal scales. American Zoologist 39: 113-130.

Pearce, F. 1999. Coral grief: The cause of reef health problems may be blowing in the wind. New Scientist 163 (2193): 22.

Petit, J.R., Jouzel, J., Raynaud, D., Barkov, N.I., Barnola, J.-M., Basile, I., Bender, M., Chappellaz, J., Davis, M., Delaygue, G., Delmotte, M., Kotlyakov, V.M., Legrand, M., Lipenkov, V.Y., Lorius, C., Pepin, L., Ritz, C., Saltzman, E. and Stievenard, M. 1999. Climate and atmospheric history of the past 420,000 years from the Vostok ice core, Antarctica. Nature 399: 429-436.

Richardson, L.L., Porter, J.W. and Barber, R.T. 1999. Status of the health of coral reefs: An update. U.S. Global Change Research Program Seminar Series, http://www.usgcrp.gov.

Uppenbrink, J. 1999. The North Atlantic Oscillation. Science 283: 948-949.

Veizer, J., Ala, D., Azmy, K., Bruckschen, P., Buhl, D., Bruhn, F., Carden, G.A.F., Diener, A., Ebneth, S., Godderis, Y., Jasper, T., Korte, C., Pawellek, F., Podlaha, O. and Strauss, H. 1999. 87Sr/86Sr, δ13C and δ18O evolution of Phanerozoic seawater. Chemical Geology 161, 59-88.

Veron, J.E.N. 1995. Corals in space and time. Comstock/Cornell, Ithaca, NY.

Related Links

Coral reefs

Coral bleaching

Coral reef adaptation

Symbiont shuffling

Coral reefs and sea level rise

Coral reefs and ocean acidification

External Links

Personal tools