Mass coral mortality under local amplification of 2 °C ocean warming

A 2 °C increase in global temperature above pre-industrial levels is considered a reasonable target for avoiding the most devastating impacts of anthropogenic climate change. In June 2015, sea surface temperature (SST) of the South China Sea (SCS) increased by 2 °C in response to the developing Pacific El Niño. On its own, this moderate, short-lived warming was unlikely to cause widespread damage to coral reefs in the region, and the coral reef “Bleaching Alert” alarm was not raised. However, on Dongsha Atoll, in the northern SCS, unusually weak winds created low-flow conditions that amplified the 2 °C basin-scale anomaly. Water temperatures on the reef flat, normally indistinguishable from open-ocean SST, exceeded 6 °C above normal summertime levels. Mass coral bleaching quickly ensued, killing 40% of the resident coral community in an event unprecedented in at least the past 40 years. Our findings highlight the risks of 2 °C ocean warming to coral reef ecosystems when global and local processes align to drive intense heating, with devastating consequences.

. In all panels, the data are derived from the single gridbox (2° resolution for ERRST and 1 °C resolution for OI) covering Dongsha Atoll. Red and blue shading corresponds to years that were warmer or cooler, respectively, than the 1940-1970 climatology calculated from ERSST. Anomalously warm SST often occurred in the South China Sea during strong El Niño events, especially pronounced during summertime in 1998, 2007, and 2015. The map in panel a was created with MATLAB2012a (http://www.mathworks.com/) using data sources described in the Methods.
as is characteristic of many coral atolls, and barrier and fringing reefs worldwide. In summer, water on the shallow reef is heated during the day by solar insolation, but is cooled via advection of offshore water across the reef flat by tidal and wave-driven currents (Fig. 3). Consequently, daily average temperatures on the reef flat typically resemble those of the surrounding open ocean. Indeed, mean temperature recorded by our in situ logger on the reef flat during June-July-August (JJA) of 2013-2015 was 29.7 °C, practically identical to that of the surrounding open ocean (29.6 °C in both NOAA-OI and NOAA Coral Reef Watch) ( Supplementary Fig. S1). However, in June 2015, an anomalous high-pressure system reduced wind speeds and surface wave height across the northern SCS ( Fig. 2b and Supplementary Fig. S3). As a result, current speeds on the reef flat decreased by 40-60% compared to the previous two years for which we have data ( Supplementary Fig. S3), disrupting the local heat budget (Fig. 3). For several days, heating from solar insolation exceeded the advective cooling that would otherwise keep the reef flat at open-ocean temperatures, adding up to 4 °C to the relatively modest 2 °C open-ocean anomaly. Reef-flat temperatures peaked in excess of 6 °C above the climatological mean June SST (Figs 2 and 3). We diagnosed the causes of this transient heating event using high-resolution physical measurements and a heat-budget analysis (Fig. 3). The extreme temperature (36 °C) reached in June 2015 was a result of global (El Niño warming superposed upon a global warming trend), regional (high pressure system and reduced winds), and local hydrodynamic (shallow reef, neap tide and unusually slow currents) factors aligning -at the right time -to drive intense heating (see Supplementary Information for additional details).
Ecological surveys conducted across the reef flat in early June prior to the bleaching event, and again in late July provide a rare quantitative characterization of the response of the benthic community to the extreme thermal stress 7 . In early June, live, healthy corals on the reef flat covered 22% of the benthic area. Mass coral bleaching was observed two weeks later, coincident with maximum temperatures. By late July, bleaching gave way to mass mortality and the cover of live, un-bleached coral was halved to 11% of the benthic area. Our ecological survey point-counts showed 33-40% of coral points recently dead and 10% still bleached (Fig. 4). The response of the benthic community was unusually rapid. Whereas corals typically bleach -and recover -in response to several months of accumulated heating or cooling 28,29 , corals on the Dongsha reef flat bleached within one week of peak temperatures and 90% of them were either recovered or dead less than six weeks later.
In contrast to the reef flat, no bleaching was observed on the upper fore reef slope or in the channel north of Dongsha Island, where local amplification of warming did not occur. Large-amplitude internal waves are generated on tidal frequencies in the Luzon Strait to the east of Dongsha Atoll and propagate along the thermocline (70-100 m depth) into the northern SCS 17,30 . When these internal waves collide with Dongsha Atoll, they deliver deep, cool water up the fore reef slope 17,30 . As a consequence, temperatures at 7 m depth on the fore reef decrease to the onset of bleaching in mid-June, relatively high air temperatures, insolation, and humidity; and low wind speeds created favorable conditions for high air-to-sea heat flux. However, while water temperatures increased > 4 °C between early and mid-June, the calculated air-sea heat flux maintained a consistent diurnal cycle of nearly constant amplitude, suggesting that the advective component of the heat budget was responsible for the warming between early and mid-June. Indeed, the calculated advective heat flux shows large cooling events that occur daily, but begin to diminish in strength and nearly disappear during neap tide on 11 June, coincident with the maximum rate of warming and the onset of bleaching.
as much as 8 °C for several hours each day 17 , and during 6-15 June 2015, eastern fore reef temperatures were on average 2.8 °C cooler than the surrounding open-ocean SST (Fig. 2e). Yet over the same time in the channel north of Dongsha Island, where the internal waves are absent, mean temperature was within 0.1 °C of the open-ocean SST (Fig. 2e). The lack of bleaching in the channel indicates that the 2 °C open-ocean anomaly was insufficient to drive bleaching on its own and that internal waves may not have been necessary to relieve thermal stress and prevent bleaching on the upper fore-reef slope. Rather, the synergy of global, regional, and local drivers of warming was necessary to drive mass bleaching and mortality on the reef flat.
We observed strong species-specific patterns in mortality as a result of bleaching on the reef flat (Fig. 4). Based on visual surveys conducted on 20 June, all colonies of Porites, Acropora, Pavona, and Stylophora, the four most common coral genera on the reef flat, appeared bleached. However, six weeks later, we found only 17% mortality of Porites in our ecological point-count data, compared with 56% for Acropora (Fig. 4). Contrasting bleaching responses have the potential to shift coral reef community composition in favor of the most resistant species 31,32 . Acropora, though vulnerable to bleaching, has relatively high growth rates and fecundity [32][33][34] . These traits enable recovery of partially depleted populations, but only over decades and in lieu of reoccurring thermal stress events 32 . Branching corals, including Acropora, create unique habitat for many other reef taxa 5,35,36 . Their selective demise, therefore, creates additional problems for the biodiversity of coral reef ecosystems 32 , which harbor an estimated one quarter of all marine species 37 . Mass bleaching-induced mortality of long-lived corals across the Dongsha reef flat suggests that an event of this magnitude is unusual, and perhaps unprecedented over the past several decades. Bleaching was reported in the waters immediately surrounding Dongsha Island in 1998 (ref. 38), but the larger lagoon and reef flat were not monitored at that time. To assess whether past high temperature events in the open ocean drove similar levels of ecological response, we examined skeletal cores from massive Porites corals for evidence of stress banding, discrete anomalously high-density bands of skeleton accreted during bleaching [39][40][41][42][43] . Colonies that bleach but survive and continue to grow, preserve within their skeleton a high-density stress band visible in computerized tomography (CT) scans [39][40][41][42] . Recent evidence suggests that Porites stress bands are reliable archives of past bleaching events because their prevalence scales proportionally to community-level bleaching 43 . Partial colony mortality, indicative of severe bleaching, is also visible in CT scans, and reductions in growth due to slow recovery can be quantified from CT images [39][40][41][42] .
We analyzed CT scans of cores from 22 Porites colonies on the reef flat ranging in height from 1 to 1.5 m. Each colony was alive and pigmented in early June, prior to the peak temperature anomaly, all appeared bleached by mid-June, and 11 (i.e., 50%) of these colonies died by late July. Average growth rate was 1.5 cm yr −1 (Supplemental Fig. S5), indicating that these colonies were 70-100 years old. This means that each colony had survived prior high temperatures associated with El Niño events in 1983, 1998, and 2007 (Figs 1 and 5). However, our analysis of the skeletal records shows that less than 50% of the colonies had bleached during these events, compared with 100% in 2015 (Fig. 5), and there were no signs of partial mortality and no significant declines in annual calcification rate (Supplementary Fig. S5). This implies that the 2015 bleaching event was the most severe to hit Dongsha Atoll in at least the past 40 years, and possibly much longer.
Reef-building corals typically live near the upper limits of their thermal tolerance 7,8 . Global climate models project that conditions on the majority of coral reefs will exceed these limits by the second half of this century 10,11 . Reducing greenhouse gas emissions in an effort to cap open-ocean warming to 2 °C could delay these impacts and may allow some corals time to acclimate and adapt [10][11][12] . However, most projections of coral reef futures under Scientific RepoRts | 7:44586 | DOI: 10.1038/srep44586 a 2 °C global warming scenario rely solely on estimates of open-ocean warming without considering the compounding effects of regional climate and local hydrodynamics. Our results indicate that these projections may be overly optimistic for many shallow coral reef ecosystems.

Methods
Climate data. Sea surface temperature (SST) data were acquired from the Extended Reconstructed SST (ERSST) product 44 , NOAA Optimum Interpolation (NOAA-OI) 45 , NOAA Coral Reef Watch 46 , and Moderate Resolution Imaging Spectroradiometer (MODIS) 47 . The different SST products possess a range of temporal coverage and spatial resolution. ERSST covers the entire 20 th century at relatively coarse (2° by 2°) resolution, NOAA-OI begins in 1982 at 1° resolution, Coral Reef Watch begins only in 2013 at high resolution (5 km), and MODIS covers only 2002-present but at very high spatial resolution (4 km). ERSST and NOAA-OI anomalies were calculated relative to the 1940-1970 ERSST mean. The NOAA Coral Reef Watch program calculated monthly climatologies for 1985-2012, and we used this as the climatology in our assessment of SST anomalies in the open ocean around Dongsha Atoll during June 2015. ERSST data were used to evaluate the centennial-scale warming trend in the northern South China Sea (Fig. 1). MODIS was used to plot the high-resolution distribution of SST in and around Dongsha Atoll for the eight-day period covering the onset of bleaching (i.e. MODIS data were used only to make Fig. 2c). Sea level pressure (SLP) data (2.5° resolution) were acquired from the National Centers for Environmental Prediction/National Center for Atmospheric Research (NCEP/NCAR) Reanalysis 48  Heat budget calculations. We used the Dongsha Island meteorological data to estimate the air-sea heat flux in June 2015 as the sum of latent, sensible, longwave radiation, and shortwave radiation fluxes (Fig. 3). Longwave radiation was estimated following Reed (1976) 50 , and latent and sensible fluxes were estimated using bulk-formula calculations with COARE 2.6 51 following the approach previously developed and validated on Red Sea reefs with similar bathymetry to the Dongsha reef flat 16 . Heat fluxes were converted to temperature (T) change by , where t is time, Q is heat flux in W m −2 , ρ is seawater density (kg m −3 ), c p is the heat capacity of seawater (W s kg −1 °C −1 ), and h is water depth (m). The total heat budget (in °C hr −1 ) on the reef flat was determined by taking the time-derivative of measured water temperature, and the advective component was estimated as the difference between total (observed) and air-sea (calculated) components (benthic and diffusive heat fluxes assumed negligible).
Ecological surveys. Ecological surveys were conducted at seven stations across the reef flat and two stations on the fore reef following a protocol similar to previously established methods for characterizing benthic cover on coral reefs 52 . Pre-bleaching surveys were conducted between 29 May and 7 June 53 , and post-bleaching surveys were conducted between 27 July and 2 August. At each station, 5 × 50 m transects were laid out and photographed every meter (0.5 m by 0.5 m image area), giving a total of 250 photographs per station. Transects were oriented N-S (along-shore) and spaced 5 m apart (cross-shore). Images were analyzed using the program Coral Point Count 54 with 5 randomly placed points per image identified to coral genera or benthic substrate type (Supplementary Table S1). The same survey methodology was repeated at the same locations pre-and post-bleaching for reef flat stations (E2-E5), while fore reef station E1 was surveyed only post-bleaching. The channel north of Dongsha Island was inspected visually for bleaching on 24 June and 29 July, but no photo surveys were conducted. In total, we made 22,500 point identifications in our study. All corals, whether alive and pigmented, bleached, or recently dead were identified to genera level. Bleached corals were identified based on lack of pigment and the presence of live polyps, whereas recently dead corals were distinguished based on structurally intact corallites without any live polyps present (see also Supplementary Information).
Bleaching histories and calcification rates. Coral skeletal cores were collected from massive Porites colonies using underwater pneumatic drills with 3 cm diameter drill bits. The cores were scanned at Woods Hole Oceanographic Institution Computerized Scanning and Imaging Facility and skeletal density was calculated by comparison to previously calibrated coral skeletal density standards 55 . Annual calcification rates were calculated using the software program coralCT 56 and the mean calcification rate was calculated for 2007-2012, the years that are overlapping among all colonies 57 . Stress bands were identified visually in 1983 (1/3 cores), 1998 (5/13 cores) and 2007 (6/22 cores) from coral CT scans following previous studies that linked observed bleaching with anomalous high-density band formation [40][41][42][43] .