Abstract
On 28 March 2005, the Indonesian islands of Nias and Simeulue experienced a powerful Mw 8.6 earthquake and coseismic uplift and subsidence. In areas of coastal uplift (up to ~ 2.8 m), fringing reef coral communities were killed by exposure, while deeper corals that survived were subjected to habitats with altered runoff, sediment and nutrient regimes. Here we present time-series (2000–2009) of Mn/Ca, Y/Ca and Ba/Ca variability in massive Porites corals from Nias to assess the environmental impact of a wide range of vertical displacement (+ 2.5 m to − 0.4 m). High-resolution LA-ICP-MS measurements show that skeletal Mn/Ca increased at uplifted sites, regardless of reef type, indicating a post-earthquake increase in suspended sediment delivery. Transient and/or long-term increases in skeletal Y/Ca at all uplift sites support the idea of increased sediment delivery. Coral Mn/Ca and Ba/Ca in lagoonal environments highlight the additional influences of reef bathymetry, wind-driven sediment resuspension, and phytoplankton blooms on coral geochemistry. Together, the results show that the Nias reefs adapted to fundamentally altered hydrographic conditions. We show how centuries of repeated subsidence and uplift during great-earthquake cycles along the Sunda megathrust may have shaped the modern-day predominance of massive scleractinian corals on the West Sumatran reefs.
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Introduction
Tectonic activity along subduction zones produces the most powerful earthquakes observed on Earth. A foremost example of these megathrust earthquakes is the 2004 Great Boxing Day earthquake in Indonesia which devastated infrastructure and human lives in 14 countries. Beyond the impact on society, these events have sudden and lingering impacts such as vertical crustal displacement (i.e., uplift, subsidence) and tsunamis which heavily impact coastal zones and coral reef systems. Within the life-span of coral reefs, these abrupt coseismic disturbances and concomitant environmental changes play a major role in shaping coasts and the speciation and distribution of reef-building scleractinian corals. For example, subduction zone earthquakes can raise shallow coral reef communities above sea level and lead to their demise by aerial exposure with loss in range of suitable habitat1,2,3,4,5,6. Shifts to distinct new reef zones with altered environmental conditions (i.e., light, turbidity) can encourage colonization by filamentous algae and physiological stress1,7,8. Coseismic landslides and tsunami-related effects associated with earthquakes increase sediment delivery to coastal reefs and alter biogeochemical conditions9,10,11,12,13,14. Long-term impacts result in recolonization of impacted habitats and shifts in marine foundation species and species community structure15,16,17,18. Indeed, long-term patterns in tropical Indo-Pacific coral reef biodiversity are tied to tectonic activity19,20,21.
The Sunda megathrust, a 5500-km-long subduction zone fault west of Sumatra, Indonesia, produces great-earthquakes about every two centuries22 with the potential to shape the coastal environment and coral reef communities across large spatial scales (Fig. 1). Powerful megathrust earthquakes occurred in December 2004 (Mw 9.1), and three months later in March 2005 (Mw 8.6), centered near the offshore islands of Simeulue and Nias, resulting in significant coseismic uplift (+ 2.8 m) and tsunami damage2,3. Uplift during both earthquakes led to extensive reef mortality and corals from deeper habitats colonized the reef flat zone altering the ecological dynamics of fringing reef ecosystems3. Vertical displacement altered the coastal geomorphology and distribution and movement of sediment in the nearshore environment, including loss of intertidal habitats minimizing the buffering capacity of this ecosystem3.
Despite the potential impact of earthquakes on coral reef systems there is a lack of information on relevant spatial and temporal scales. Instrumental data documenting these instantaneous events and their impacts are limited to continuous global positioning station (GPS) data to document coseismic crustal motion2. Also, most environmental assessments to date are visual and provide only a snapshot of coral reef conditions, water quality and health post-earthquake3,9,12. Longer-term observations, spanning years, are needed to provide knowledge of environmental change pre- and post-earthquake and potential interaction between land displacement, coastal hydrographic conditions, and coral reef communities.
Long-lived Porites spp. corals inhabit tectonically active regions and experience recurring amounts of uplift and subsidence and associated environmental stress over time. Porites corals can live for hundreds of years, and those that remain submerged after large earthquakes provide an archive of earthquake-induced environmental change and coral physiological response. For instance, the growth response of Porites microatolls has provided a record of interseismic and coseismic crustal motion with a ~ 200 years recurrence cycle along the Sunda megathrust22,23,24,25,26. Although the isotopic and elemental compositions of Porites skeletons have been shown to track past environmental change27,28,29, their application in earthquake prone regions is limited. Recent work has shown that shifts in skeletal carbon-isotope ratios in Porites reflect changes in light exposure following coseismic vertical displacements during the 2005 Nias-Simeulue earthquake8,30. Also, skeletal Mg/Ca in Porites has been linked to tsunami-induced algal blooms and/or presence of endolithic algae8. However, to date, there are no coral records that characterize post-earthquake marine geochemical change in coral reef settings.
Records of Mn, Y and Ba in coral skeletons have the potential to provide information on earthquake related changes in sediment delivery to nearshore areas and associated shifts in sediment dynamics within reef environments. Delivery of sediments via runoff to the coastal zone is the primary source for these elements in nearshore regions, and coral proxy records have been widely used to reconstruct terrigenous runoff on seasonal and longer timescales in the tropics29. For instance, Ba/Ca in corals reflects changes in Ba in the surface-ocean reef environment related to a range of processes such as upwelling31,32, river discharge33,34,35, wind/wave associated sediment resuspension36 and primary productivity and barite formation37,38. Mn/Ca in corals has been shown to track Mn cycling associated with large erosive events and delivery of suspended particulate matter through riverine discharge39,40,41. The residence time of Y in the estuarine zone is longer and gradual release and recycling of Y implies coral Y/Ca will record longer-term changes in dissolved Y concentrations related to environmental perturbations42,43,44,45,46,47, such as major terrestrial runoff changes or episodes of large scale erosion.
Here, we present the first records of coral Mn/Ca, Y/Ca and Ba/Ca as evidence of environmental shifts in reef systems in the aftermath of the great Nias-Simeulue earthquake of 28 March 2005. Maximum vertical displacement was centered on the northwest coast of Nias (+ 2.8 m), while a trough of subsidence (to − 1.1 m) occurred between the island and mainland Sumatra2 (see Fig. 1b). We explore ~ 9-year-long geochemical records for six massive Porites corals positioned along a transect of vertical displacement from + 2.5 m uplift to − 0.4 m subsidence (Fig. 1, Table 1), and across different reef environments (e.g., lagoonal, fringing). We showcase the potential for Mn/Ca, Y/Ca and Ba/Ca to geochemically fingerprint shifts in sediment dynamics and reef environments following the earthquake. The new geochemical records, along with information about great-earthquake recurrence intervals in West Sumatra, allow us to assess the long-term environmental impact of vertical tectonic motion on coral reef expansion and retreat in earthquake prone regions.
Study site and coral drilling
Nias is located ~ 125 km offshore of the west Sumatran coast (1° N, 97.5° E) and experiences an equatorial climate with abundant rainfall year-round (~ 4000 mm annual average). Situated in the Indo-Australian monsoon region, Nias experiences associated shifts in surface winds, generally from the northwest in boreal winter and southeast in boreal summer. Aperiodic variations in the Indian Ocean Dipole (IOD) drive climate variability, with the positive mode marked by enhanced southeast winds, coastal upwelling and cooler SSTs, and reduced local rainfall48. The island’s terrain encompasses a mountainous inland area up to ~ 800 m in elevation surrounded by lowlands with dense vegetation. Rivers are perennially inundated leading to terrestrial discharge along coastal areas. A small concentration of rivers outflow along the northwest coast of Nias into the study area (Fig. 1). The dominant river is the Muzoi, with catchment headwaters extending ~ 40 km inland. Two smaller rivers, the Lafau and an unnamed river, have localized coastal plain catchments.
Continuous GPS data and records of microatoll elevation were used to construct a contour map of coseismic uplift and subsidence along the Nias coastline produced by the 2005 earthquake2. Four years after the earthquake, we used the pattern of tectonic deformation to guide the drilling of submerged, dome-shaped Porites corals in May 23–29, 2009 at three sites30; two near the coast with strong uplift (+ 2.5 m, + 1.8 ± 0.18 m) and one offshore island control site with minor subsidence of − 0.42 ± 0.18 m (Fig. 1, Table 1). The + 2.5 m collection site (2.5A) is located within a broad fringing reef lagoon on the northwest corner of Nias, with large areas of the reef exposed post-earthquake (Fig. 2), proximal to the small river outlet. The + 1.8 m collection site (1.8A) is located 9 km to the east on the south side of Hilimakora Island, one of a series of small nearshore islands exposed to nearby runoff from the Muzoi and Lafau rivers. The control site, Sarangbaung Island (M0.4A), is located 20 km northeast of Nias, far from the influence of coastal rivers. The semi-diurnal tidal envelope along the coast of northwest Nias is microtidal with a maximum range of 1.2 m (Ref.8).
We analyzed cores from healthy coral colonies drilled vertically to a depth of 50–70 cm from the upper growth surface in close proximity to each other at the 2.5A (two corals) and 1.8A (three corals) uplift sites, and from one coral at the M0.4A control site offshore (Fig. 1, Supplementary Fig. 1). Previous work has shown that average annual coral extension rates, based on annual cycles of δ13C in coral skeleton that grew after the earthquake, and density band widths in x-radiographs, range from 16 to 23 mm/year at the 1.8A and M0.4A sites30, which is typical for massive Porites colonies growing in warm tropical settings49. In this study, we use annual cycles of Ba/Ca in coral skeleton that grew after the earthquake to estimate similar annual extension rates of 14–17 mm/year at the 2.5A and M0.4A sites (see “Methods”, Table 1, Supplementary Figs. 2–5).
Results and discussion
Behaviour of coral Ba, Mn and Y in the aftermath of the 2005 earthquake
Here, we explore the nature of post-earthquake changes in the new coral skeletal Mn/Ca, Y/Ca and Ba/Ca records and their links to altered environmental drivers, including terrestrial sediment delivery and reef-specific hydrographic factors (lagoonal reef versus fringing reef). Due to the pervasive year-round rainfall and lack of strong climatic events in northwest Nias, we attribute sustained shifts (> 1 year) in coral geochemistry across the time window of the coral cores (2000–2009.5) to earthquake-related environmental changes (see “Methods”). However, further validation of the coral geochemical response to earthquakes requires in situ records of the effect of river discharge on the water quality of the northwest Nias reefs, which are currently not available.
Post-earthquake enhancement of sediment delivery
Average coral Mn/Ca values are highest at the 1.8A uplift site (1.2 μmol/mol) under the influence of runoff from the Muzoi and Lafau rivers (Fig. 3). By comparison, Mn/Ca values are much lower at the 2.5A uplift site (0.6 μmol/mol), proximal to the relatively small river, and lowest at the offshore subsidence site M0.4A (0.4 μmol/mol) with no riverine influence. Mn/Ca values for these corals fall within the range for Porites observed at other locations45,50. At the 2.5A uplift site, Mn/Ca shows sustained post-earthquake increases in both coral cores (2.5A-1, 2.5A-3) of 0.43 and 0.20 μmol/mol, respectively (Fig. 3, p < 0.0001 in Supplementary Table 1). Coral Mn/Ca at the 1.8A uplift site shows similar significant increases; 0.45 μmol/mol in coral 1.8A-6 and smaller increases of 0.17 and 0.18 μmol/mol in corals 1.8A-2 and 1.8A-5, respectively. Significant change points between 2004.9 and 2005.4 CE were identified across all five coral records for both uplift sites, in good alignment with the tsunami and earthquake (Fig. 3). In contrast, the M0.4A site shows negligible change in Mn/Ca (0.01 μmol/mol). Overall, these results indicate that coral Mn/Ca shows a significant step-change increase at the uplift sites ranging from ~ 0.17 to 0.45 μmol/mol, regardless of reef environment.
We propose that the increase in Mn/Ca is driven by a post-earthquake increase in sediment transport from land to sea. Earthquake and tsunami associated slope failure can remove vegetation and facilitate increased erosion, sediment transport, and discharge during high rainfall events. Previous work in wet sub-tropical Taiwan has documented increases in sediment delivery to coastal environments following large earthquakes10,14. The 2004 Boxing Day tsunami, which preceded the 2005 earthquake by three months, delivered waves up to 3.9 m in height at northwest Nias and left debris behind in trees11, and would have made the land surface susceptible to erosion. Indeed, the 2005 earthquake mobilized sediment from the mountainous regions to the coast, so much so that alterations in beach profile led to an increase in available nearshore sediment supply3. Furthermore, long-term shifts in coral Mn/Ca have been linked to mobilization of Mn associated with enhanced sediment delivery related to exposure and erosion of land surfaces associated with cyclone events and also catchment clearing40,43. Together, these findings indicate that earthquakes can abruptly alter nearshore reefs by enhancing sediment delivery to coastal regions, and coral Mn/Ca provides a useful proxy to monitor earthquake-induced changes in suspended sediment load.
In addition to the changes in coral Mn/Ca, we document variations in coral Y/Ca associated with increased sediment delivery (Fig. 4). Corals A-2 and A-5 from the 1.8A uplift site, proximal to two rivers, have the highest mean Y/Ca values (136 nmol/mol), in contrast to M0.4A (91 nmol/mol) with no riverine influence (Supplementary Table 1), in line with other studies showing gradients in Y/Ca with increasing riverine influence39,44. The range of Y/Ca values at these sites is similar to that reported for Porites in the Great Barrier Reef45 (83 nmol/mol) and Puerto Rico40 (40 nmol/mol).
Y/Ca at the 1.8A uplift site shows a statistically significant step-change increase in corals A-2 (74 nmol/mol) and A-5 (25 nmol/mol) (Fig. 4, p < 0.0001 in Supplementary Table 1). Also, raised corals 1.8A-6, 2.5A-1 and 2.5A-3 show a prominent transient increase in Y/Ca around the time of the earthquake (Fig. 4). Furthermore, change point analysis reveals a transient increase in coral 1.8A-2 superimposed on the step-change increase in mean Y/Ca, with an initial rise in Y/Ca at 2004.9 CE and return to the post-earthquake mean at 2005.4 CE. Shared change points identified in corals 1.8A-6 and 1.8A-2 indicate that the transient increase in Y/Ca for two of the three cores at this site occurred between 2004.9 CE and 2005.7 CE. The subsidence site coral M0.4A-3 shows no transient peak associated with the earthquake, but rather a decrease in Y/Ca (26 nmol/mol) marked by a change point and step-change in post-earthquake mean.
Taken together, the results for the two uplift sites show either a sustained post-earthquake step-change increase in Y/Ca, or a transient increase in Y/Ca around the time of the earthquake. We suggest that these signals are linked to increased sediment availability, as Y/Ca has been shown to record changes in suspended sediment on annual to longer timescales related to large erosion events39,45,47. Indeed, during our initial visit to northwest Nias in June 2006, about 14 months after the earthquake, turbidity was particularly high in the + 2.5 m raised-reef lagoon offshore of Lahewa. Therefore, the tendency for transient increases in Y/Ca at the 2.5A lagoonal reef site could be due to tsunami, initially, followed by transient post-earthquake activation of the localised river sediment supply and wind-driven sediment resuspension in the shallow lagoon. Also, in June 2006 the Porites corals in the high uplift area were coated with green–brown algae. Post-earthquake decomposition of algal mats and development of reducing conditions could contribute to the pulse-like Y/Ca signature in coral cores at the 1.8 m and 2.5 m uplift sites, similar to changes observed in western Sumatra during a massive red tide51. The different nature of responses in coral Y/Ca, either transient or long term, suggests that within-reef differences in sediment availability and/or coral-colony specific factors could play a role in coral Y/Ca variability. The absence of an increase in Y/Ca at the offshore subsidence site supports the idea of increased sediment activation specific to raised-reef sites. In sum, the Mn and Y records both suggest that nearshore suspended sediment availability expands in the aftermath of coseismic uplift and alters the geochemical inventory of raised-reef environments in proximity to land.
Reef-specific earthquake-induced environmental changes
In addition to changes in sediment delivery associated with uplift, we propose that different types of reefs (fringing versus lagoonal) experience divergent patterns of post-earthquake environmental change, as evident from the Nias coral Mn/Ca and Ba/Ca records (Fig. 5). Skeletal Ba/Ca values for lagoonal reef sites (2.5A, M0.4A) show a seasonal cyclicity with average values (4.5–4.8 umol/mol) similar to those in Porites exposed to upwelling of Ba-enriched waters32. In contrast, the coral Ba/Ca values for the 1.8A fringing reef site are lower on average (2.8–4.2 umol/mol), with annual peaks of varying intensity, similar to Ba/Ca records for sites proximal to rivers in Singapore with high suspended sediment loads52 (2–14 umol/mol). At the lagoonal sites, with uplift (2.5A) and subsidence (M0.4A), post-earthquake Ba/Ca increased by only 0.18–0.24 umol/mol (Supplementary Table 1). On the other hand, coral Ba/Ca at the fringing reef site (1.8A) shows a wide range of responses, including a particularly large increase in coral 1.8A-2 and a significant post-earthquake decrease in coral A-6. While the change point analysis highlights Ba/Ca responses occurring within the earthquake interval in individual records, they are not replicated by other records at the same site, or across sites, indicating a variable response of Ba/Ca to the 2005 earthquake.
These observations suggest that coral Ba/Ca has the potential to provide additional information about reef-specific impacts caused by earthquakes. In the wake of the 2004 tsunami, short-term increases in primary productivity53,54 could lead to pulse-like increases in Ba/Ca prior to the 2005 earthquake, followed by long-term increases in sediment resuspension and nutrients. Additionally, the 2.5A lagoonal reef site is proximal to a small river outlet, thus the long-term increase in coral Ba/Ca at this locality could be primarily driven by a mechanism specific to that reef. Distinct green–brown banding is present in the post-earthquake section of the site 2.5A drill-cores providing a visual indicator of earthquake-induced environmental stress and changes in primary productivity (Supplementary Figs. 3 and 4). Extensive shallowing of the raised-reef lagoon made the lagoon floor more susceptible to wind-induced sediment resuspension, and previous research has shown that accompanying release of sediment porewater nutrients drives algal blooms55,56,57. This increase in primary production would alter the Ba2+ inventory in the reef waters by barite formation, and resuspension of Ba-rich particles, as shown in previous studies37,38. Therefore, we propose that the post-earthquake increase in coral Ba/Ca at the + 2.5 m uplift site is related to increased lagoonal Ba2+ via wind-driven resuspension of Ba-rich particles, and partially to an increase in sediment delivery.
The sediment resuspension mechanism also could partly explain the increase in coral Mn/Ca at the 2.5A lagoonal site given that decaying organic matter produces reducing conditions leading to increases in porewater Mn2+ .39,42. Thus the post-earthquake increase in Mn/Ca might be related to northwest wind-driven remobilization of sediment porewater Mn2+, leading to seasonal increases in Mn2+ 50,58. Along the same lines, we attribute the post-earthquake increase in coral Ba/Ca at the offshore subsidence site (M0.4A) to increased wave-penetration across the lowered reef-crest and sediment resuspension in the deepened lagoon. The variable response of Ba/Ca at the 1.8A fringing reef site also indicates that coral Ba/Ca is influenced by local variations (i.e., sediment delivery) and/or coral-colony specific factors. The results highlight the need for multiple coral Ba/Ca records for each reef location to provide composite records that resolve changes in sediment delivery35.
Overall, these findings suggest that coral Mn/Ca, Y/Ca and Ba/Ca records can provide information on sediment delivery and reef-specific environmental change associated with earthquake events. In the case of the 2005 earthquake in Nias, the sediment load of rivers in the coseismically uplifted area evidently increased, and lagoonal reef settings, both raised and submerged, were impacted by wind- and wave-driven sediment resuspension and phytoplankton blooms. The results for the 2005 earthquake event, together with current knowledge about the history of great-earthquakes along the Sunda megathrust, raise the possibility that recurring cycles of interseismic subsidence and coseismic uplift could set the pace of reef growth and retreat on the outer-arc islands west of Sumatra.
Coral reef response to great-earthquake cycles
Detailed studies of the growth-response of abundant massive Porites spp. microatolls to vertical crustal displacement during great-earthquake cycles have illustrated the influence of neotectonics on the natural dynamics of the West Sumatran coral reefs22,23,24,25,26,59,60,61,62,63. The new Nias coral geochemical records demonstrate that distinct environmental changes occurred in raised coral reef environments in the aftermath of the 2005 Nias-Simeulue earthquake. Here, we explore the potential role of recurrent earthquake-induced environmental impacts in shaping the coral community structure and species composition of the outer-arc island fringing reefs. Notable in this regard, the diversity of scleractinian coral species along the west coast of Sumatra is the lowest in Indonesia64. Also, recent surveys show that the island fringing reefs offshore at Nias, Simeulue, and the Mentawai Islands are dominated by stress-tolerant coral species such as Porites, Pavona and Psammocora with massive and sub-massive growth forms65.
The available observational data on the pattern of coral damage in the aftermath of the 2005 earthquake at raised-reef sites along the northwest coast of Nias, including our study area, illustrate how earthquakes can alter the species composition of coral reefs. Post-earthquake surveys found a 50% decrease in live coral cover and a shift from branching to massive growth-forms as the dominant surviving coral group due to the vulnerability of the branching morphology to physical damage66. Our observations in May 2009 confirm that massive Porites colonies were the dominant survivors at our three study sites. Only partial recovery of coral cover had occurred on submerged sections of the Nias raised reefs by December 2015, ~ 10.5 years after the earthquake, in part because of further loss of live branching coral caused by seismic shaking during two massive strike-slip earthquakes (Mw 8.6 and 8.2) centred ~ 450 km west of Nias on 11 April 2012 67. This post-seismic pattern of species-specific survival is analagous to well-documented reef damage associated with hurricanes, which destroy shallow-water branching corals and increase the relative abundance of encrusting and massive-shaped colonies68,69.
Coral reproduction and recruitment following abrupt disturbances is critical in setting the course of recovery for coral reef systems69,70,71. Availability of coral larvae and successful settlement and survival of recruits are critical factors governing this process71. The initial life stages of scleractinian corals can be negatively impacted by water quality; changes in sediment, salinity and dissolved inorganic nutrients can reduce gamete production, fertilisation, and embryo development71,72. Furthermore, the density of spawning adult coral colonies, specific to each species, is important for fertilisation success71. Low densities of reproductive branching corals post-earthquake can constrain fertilization success since the majority of viable larval recruitment occurs close to the reproductive source71,73. Additionally, any potential larval recruitment from undamaged reefs outside the earthquake rupture zone may be limited due to competiton for space by pioneering massive corals70. Consequently, the size of a surviving massive coral population may be enhanced by local larval input and preferential recruitment following an earthquake, thus increasing the likelihood of their presence in successive generations74.
Based on these results, we suggest that the great-earthquake cycle in West Sumatra could serve to scale-up the localized environmental and ecological effects of neotectonics on coral reefs to the regional level (Figs. 6, 7). Studies of the growth-response of Porites microatolls to tectonic motion have revealed the repetition of great-earthquake cycles along the Sunda megathrust over the last ~ 700 years, with century-scale periods of interseismic subsidence terminated by coseismic uplift22,23,24,25,26. Our photographs of the raised reefs of northwest Nias following the 2005 earthquake show that tectonic subsidence, and reef expansion via coral colonization of new seafloor, was well underway during the decades prior to the 2005 earthquake (Figs. 2, 6). This observation is consistent with microatoll elevation data for northwest Nias showing interseismic subsidence leading-in to 2005, and also before the 1861 Nias earthquake25 (Fig. 6). These long intervals of interseismic quiescence provide stable environmental conditions for coral reef expansion before the system abruptly switches to post-seismic adaptation.
Figure 7 provides an overview of the spatial and temporal histories of interseismic subsidence and coseismic uplift along the Sunda megathrust. In general terms, we propose a three-phase coral reef response within each great-earthquake cycle: (1) post-earthquake reef contraction and adaptation; (2) slow century-scale subsidence and ecological equilibrium; and (3) reef expansion leading up to the final major earthquake. However, the spatial and temporal characteristics of each great-earthquake cycle are influenced by the tectonic status of different sectors along the Sunda megathrust. For instance, the Mentawai Islands and Nias-Simeulue sectors have broadly aligned and regular earthquake cycles lasting about 200 years22,23,24,25,26 (see Fig. 7). In contrast, the Batu Islands sector exhibits subdued tectonic activity compared to neighbouring sectors60,63. The records also indicate that the massive 2004 and 2005 earthquakes marked the culimination of the most recent earthquake cycle in the northernmost Sumatra–Andaman Island sector24,25, where the reef adaptation process is presumably well underway. However, the ensuing rupture sequence in the Mentawai Islands sector remains incomplete, increasing the likelihood of further coseismic uplift and reef adaptation22. Consequently, the current scenario is one of disparate tectonic and ecological backdrops, the net effect of which is to create a heterogeneous mosaic of reef responses across the region.
Among the implications, our findings highlight the need to consider the evolving tectonic, environmental and ecological status of the Sunda megathrust in assessments of anthropogenic degradation on the outer-arc island fringing reefs of West Sumatra. The integrated coral geochemical records and great-earthquake time-series indicate that most of the coral communities are currently at an unsual adaptational juncture. While the immediate loss of coral cover following coseismic upheaval is clear, the post-seismic environmental impacts could alter coral reef community structures for years. For instance, prolonged periods of elevated turbidity reduce light availability and suppress coral growth via reduced photosynthetic rates, with species-specific tolerance responses75. And shifts in primary productivity can lead to infestation of corals by endolithic algae, further affecting coral growth and survival1,7,8. Understanding the interplay between earthquakes and the variable baseline of coral reef health will be critical to quantify the broader impacts of human agency.
Conclusions
New coral geochemical records for the 2005 Nias-Simeulue earthquake in West Sumatra provide valuable archives of earthquake-induced shifts in coral reef environmental conditions. Specifically, skeletal Mn/Ca reflects changes in sediment delivery at uplifted reef sites, regardless of reef type. The increase in sediment delivery associated with the earthquake is tied to changes in riverine geomorphology and reef-specific changes brought about by vertical displacement. Additionally, skeletal Y/Ca and Ba/Ca support the idea of changes in sediment delivery to reef environments in the aftermath of earthquakes. Raised-reef lagoonal Mn/Ca and Ba/Ca records highlight the role of shoaling and changes in local hydrography on resuspension of sediments and primary productivity. Our analysis of the 2005 event indicates that abrupt shifts in coral reef environments can alter the community structure of coral reefs, and raises the possibility that recurrent great-earthquake cycles along the Sunda megathrust have played a role in shaping the low species diversity of corals on the West Sumatran reefs. While our focus here is on the outer-arc island fringing reefs along the Sunda megathrust, the earthquake cycle reef-response concept could be applied to improve our understanding of the community status of coral reefs along subduction zone margins elsewhere in the tropics.
Methods
Coral sample preparation and trace element analysis
Coral cores were longitudinally slabbed into 7-mm thick slices and X-rayed in order to identify a maximum growth axis and develop a basic chronology for each coral record (Supplementary Figs. 2–5). The slabs were cleaned using a hand-held ultrasonicator probe in Milli-Q water and dried overnight in an oven at 40 °C. After removal of material for stable isotope analysis30, a 25 × 95 mm (maximum) section was cut from the coral slice to fit within the sampling cell for analysis by laser ablation inductively coupled plasma mass spectrometry (LA-ICP-MS) at the Research School of Earth Sciences, the Australian National University. Each section was vigorously cleaned using a hand-held ultrasonicator in Milli-Q water and placed in an oven overnight to dry at 40 °C. Laser scan-paths were selected to parallel the major growth axis of the coral and the stable isotope sampling path across at least nine years of coral growth to capture pre- and post-earthquake elemental variability.
The LA-ICP-MS laboratory procedures for analysis of trace elements in corals have been described in detail42,76,77. Briefly, the LA-ICP-MS system uses a 193 nm ArF excimer laser coupled to a Varian 820 ICP-MS to quantify trace element intensities. Ablated material was delivered to the ICP-MS via a mixed stream of Ar and He (Ref.78). Prior to analysis, laser tracks were pre-ablated to remove surface contaminants using a large 100 um × 700 um rectangular spot, with the laser set at 20 Hz and 100 mJ. For the analytical work, ablation analysis was conducted in two consecutive traverses of the sample: major trace element analysis (Ba, Mn) using a 50 × 500 um spot size followed by trace element analysis (Y) using a 100 × 500 um spot size, as outlined in Ref.42. The ablation analyses were carried out at a 40 um/s scan speed, 5 Hz repetition rate, 50 mJ energy, and using a 50% partially reflecting mirror. Measurements on standards were made at the beginning and end of each analysis section; the NIST 614 silicate glass certified reference material and an in-house pressed coral powder standard were used to normalize Y and Mn, and Ba, respectively42,79. The normalized data were smoothed with a 10-point averaging box filter to remove high frequency variation due to instrumental instability and counting statistics (Supplementary Figs. 6–8). All reported Y/Ca values are at least one order of magnitude greater than the instrument detection limit42.
We note that in some studies a stepwise pretreatment with intensive cleaning procedures (i.e., hydrogen peroxide rinses) has been employed for coral trace element analyses to ensure that the measured Mn and Y has substituted for Ca in the aragonite lattice, rather than reflecting organic phases or Mn oxide coatings41,43,80. We follow the method of Ref.42, which incorporates several pre-ablation steps to ensure minimal surface contamination. To assess the Mn signal we acquired Mn data from both analyses (major and trace element) along the same track in coral core 2.5A-1. We see similar post-earthquake increases in Mn in both analyses, which suggests the Mn signals are lattice bound (Supplementary Fig. 6). Also, there is a steep rise in Mn/Ca at the end of both records that is mostly restricted to skeletal elements that were surrounded with live coral tissue at the time of collection.
Coral core chronologies
We use the approach of Gagan et al.30 to generate age models for the elemental records for three previously published coral cores at the 1.8A uplift site. In this earlier study, the position of the step-change in skeletal δ13C due to uplift marks the position (and date) of the earthquake within each coral core at the 1.8A site. This chronological ‘anchor point’ was then used to estimate average annual coral extension rates. In most cases, the position of the earthquake signal within the coral cores is also marked by a slight change in skeletal density evident in X-radiographs. The methodology indicates reasonable growth rates of 16–18 mm/year for the three 1.8A corals anaysed for the present study (Table 1).
While this approach is valid for the 1.8A site, there is no clear signal in coral δ13C at the 2.5A uplift site, presumably due to higher water column turbidity post-earthquake, which masked the effect of increased light intensity due to uplift30. Additionally, the juvenile coral M0.4A-3 does not show a distinct change (decrease) in δ13C associated with subsidence and a decrease in light intensity, possibly due to ontogenetic effects81. In these cases, we use coral Ba/Ca cyclicity alongside skeletal density patterns in x-radiographs and coral core features to constrain the earthquake window. At the 2.5A and M0.4 sites, coral Ba/Ca shows a distinct seasonal cyclicity, linked in other regions to seasonal upwelling31,32 (Supplementary Figs. 3–5). We align high Ba/Ca peaks in the records to mid-October, around the end of the southeast monsoon when wind-driven upwelling and low sea surface temperatures reflect maximum shoaling of the thermocline82, and low Ba/Ca peaks to mid-April, when upwelling is weak near the end of the northwest monsoon season.
Using this approach, the March 2005 earthquake event is at 59–63 mm depth within the 2.5A and M0.4A coral cores (Table 1), which equates to reasonable growth rates of 14–17 mm/year over the post-earthquake interval (with the core-top set to May 2009). At the 2.5A site, the depth of the Ba/Ca-assigned earthquake event within the coral cores aligns with the base of a distinctive green–brown discoloration, distinctive high-density bands, and a shift to higher mean Ba/Ca (Supplementary Figs. 3, 4). We note that the juvenile coral M0.4A-3 grew more slowly after the earthquake (59 mm) compared to the other three M0.4A corals analyzed by Gagan et al.30, where a step-change decrease in skeletal δ13C due to coseismic subsidence occurs at 82–86 mm depth within the cores.
The primary goal of our study is to examine broad geochemical changes before and after the 2005 earthquake, thus basic age models are suitable for application to the ~ 9-year coral records. To quantify the post-earthquake geochemical response, averages were calculated for the coral growth intervals before (2000–2004.9) and after the earthquake (2005.25–2009) at each site. For site 1.8A, we show the extended dataset for coral core 1.8A-2 (Supplementary Fig. 7; 150–180 mm) to demonstrate the longer-term stability of the geochemical baseline prior to the earthquake, but only present the 0–150 mm interval in Fig. 3 to be consistent with other cores from this site. We performed t-tests to determine the significance of any post-earthquake geochemical shift using pre- and post-earthquake averages based on 4–5 years of coral growth (Supplementary Table 1). The t-test calculations exclude elevated Ba/Ca and Mn/Ca values that occur within (or immediately below) skeleton surrounded by live coral tissue at the time of collection. Specifically, at site 1.8A we see significantly elevated Ba/Ca values proximal to the tissue layer (Supplementary Fig. 7), which is consistent with previous studies of coral Ba/Ca (tenfold higher below tissue layer45. The t-test analysis examines long-term shifts in geochemical records and thus does not include the Y/Ca records for corals 2.5A-1, 2.5A-3 and 1.8A-6 as they show transient increases with the earthquake.
In addition to the t-tests, a Bayesian change point algorithm83 was applied to the coral datasets to statistically test for the occurrence of change points associated with the December 2004 tsunami and 2005 earthquake. The algorithm is applied to normalized Mn/Ca, Y/Ca, and Ba/Ca records for each coral across all three sites. Analyses exclude data from within the tissue layer (upper 10 mm) of each coral. A piecewise constant regression model is inferred by the algorithm to determine the posterior probability of a change point. Input parameters for the change point analysis include a minimum of 35 data points between change points (dmin), as well as a maximum number of change points permitted per solution (kmax), where 1000 independently sampled soutions are performed on each record. To define step-change earthquake signals, kmax was set to two for the Mn/Ca and Ba/Ca records. To allow for identification of the onset and termination of transient earthquake signals in the Y/Ca records, kmax was set to three. The change point probability density curves represent the probability of a change point occurring at each point in time—a result of the 1000 Bayesian solutions for each record. The presence of an earthquake signal is defined by change points that occur within the age-range of 2004.5–2005.8 CE. This 15-month window, including both the December 2004 tsunami and the March 2005 earthquake, allows for an estimated uncertainty of ± 0.5 years in the coral core chronologies, and the observation that coseismic shifts in the geochemical records are not ‘knife sharp’ when plotted as a function of time. The smoothing effect may reflect the duration of environmental change and the attenuation of geochemical signals in corals by skeletogenesis throughout the depth of the living coral tissue layer84.
Data availability
The coral geochemical data presented in this study are archived at the NOAA-NCEI World Data Service for Paleoclimatology.
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Acknowledgements
We thank Dr Heri Harjono at the Indonesian Institute of Sciences (LIPI) for essential administrative and logistical support in Sumatra under LIPI research permit 3564/IV/KS/2009 and Kementerian Negara Riset dan Teknologi (RISTEK) research permit 04/TKPIPA/FRP/SM/IV/2009. We are grateful to the captain and crew of our research vessel, the Andalas, for support for the coral drilling in Nias, and Les Kinsley, Steve Eggins, Joe Cali and Joan Cowley for laboratory support at RSES, ANU. We thank Jennie Mallela and Michele Lavigne for helpful discussions on an early draft of the manuscript. This work was supported by Australian Research Council Discovery Grants DP0663227, DP110101161 and DP180103762 to M.K.G., W.S.H. and D.H.N., and an American Australian Association Postdoctoral Fellowship to S.M.S. S.M.S. also acknowledges financial support provided by the Welsh Government and Higher Education Funding Council for Wales through the Sêr Cymru National Research Network for Low Carbon, Energy and Environment.
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S.M.S.: conceptualization, methodology, fieldwork, laboratory analysis, visualisation, writing – original draft, writing – review and editing, data curation. M.K.G.: conceptualization, methodology, fieldwork, resources, visualisation, writing – original draft, writing – review and editing, project administration, data curation. D.H.N.: fieldwork, resources, visualisation, writing – review and editing. A.K.K.: formal analysis, visualisation, writing – review and editing. B.W.S.: fieldwork, resources, writing – review and editing. H.R.: fieldwork, writing – review and editing. H.S-G.: investigation, visualisation, writing – review and editing. D.P.: underwater coral drilling, writing – review and editing. I.S.: underwater coral drilling, writing – review and editing. W.S.H.: resources, project administration, writing – original draft.
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Sosdian, S.M., Gagan, M.K., Natawidjaja, D.H. et al. Coral geochemical response to uplift in the aftermath of the 2005 Nias–Simeulue earthquake. Sci Rep 14, 8686 (2024). https://doi.org/10.1038/s41598-024-57833-1
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DOI: https://doi.org/10.1038/s41598-024-57833-1
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