More accurate global volumetric estimations of shallow-water reef deposits are needed to better inform climate and carbon cycle models. Using recently acquired datasets and International Ocean Discovery Program (IODP) Expedition 325 cores, we calculated shallow-water CaCO3 volumetrics and mass for the Great Barrier Reef region and extrapolated these results globally. In our estimates, we include deposits that have been neglected in global carbonate budgets: Holocene Halimeda bioherms located on the shelf, and postglacial pre-Holocene (now) drowned coral reefs located on the shelf edge. Our results show that in the Great Barrier Reef alone, these drowned reef deposits represent ca. 135 Gt CaCO3, comparatively representing 16–20% of the younger Holocene reef deposits. Globally, under plausible assumptions, we estimate the presence of ca. 8100 Gt CaCO3 of Holocene reef deposits, ca. 1500 Gt CaCO3 of drowned reef deposits and ca. 590 Gt CaCO3 of Halimeda shelf bioherms. Significantly, we found that in our scenarios the periods of pronounced reefal mass accumulation broadly encompass the occurrence of the Younger Dryas and periods of CO2 surge (14.9–14.4 ka, 13.0–11.5 ka) observed in Antarctic ice cores. Our estimations are consistent with reef accretion episodes inferred from previous global carbon cycle models and with the chronology from reef cores from the shelf edge of the Great Barrier Reef.
The role of calcium carbonate deposits in the carbon cycle, and the influence on climate change during the late-Quaternary is poorly constrained. The fifth assessment report of the Intergovernmental Panel on Climate Change1 identifies the major contributors for atmospheric CO2 (atm-CO2) concentration changes from the last glacial maximum (LGM) to present. The authors assigned a medium degree of confidence to the current estimates of atm-CO2 contributions from coral reef accretion and carbonate compensation depth changes. This uncertainty derives not just from the use of proxy data and their limited availability, but from the complex relationships between the carbon and other biogeochemical cycles. Such uncertainty is reflected in the range of the contributions to postglacial atm-CO2 attributed to shallow-water reefs in global carbon models (− 9 to 30 ppm2,3,4,5).
The role that coral reefs may have played in this process has been termed the coral reef hypothesis 5,6,7. This hypothesis proposes that the increase of the atm-CO2 is at least partly due to the enhanced shallow-water CaCO3 accretion by corals. This hypothesis relies on the availability of new areas of marine flooded shelf during the last transgression and on the consequent increase in coral reef development. This would have changed the alkalinity balance, at least locally, and ultimately increasing the transfer of CO2 to the atmosphere6,8. Because of the reduced marine shelf area during glacial times and the subsequent increase in reef area from glacial to Holocene times, it is assumed that the coral reefs acted as secondary amplifiers—not precursors—of a climatic change that had already initiated9,10 with early atm-CO2 rise generally preceding global surface temperature increase11.
The coral reef hypothesis is supported by the extensive coral reefs of Holocene age worldwide12,13,14,15,16. Moreover, a possible lower contribution from terrestrial sources in this same period3,17 argues in favour of alternative carbon sources, such as that represented by reef accretion. Simplified box models6,7 have suggested that the activity of the coral reefs can explain a significant rise of the atm-CO2 during postglacial times. However, the dissolution ratios, accretion rates and calcite saturation depth informing these models are poorly constrained and they possibly overestimate the total carbon derived from corals.
More complex models have considered the effect of coral reefs in postglacial atm-CO22,3,4,5,18,19. Notably, Ridgwell et al.5 inferred two possible minor episodes of global reef growth from 17.0 to 13.8 ka BP and from 12.3 to 11.2 ka BP. With no conclusive evidence available at that time for such global reef growth episodes20, they attributed the increase in CO2 to changes in the biogeochemical properties of the Southern Ocean surface.
Interestingly, recent evidence in Tahiti and the Great Barrier Reef (GBR) has revealed glacial and early-postglacial (30 to 10 ka BP) coral reef episodes in line with those inferred intervals (IODP Expeditions 310 & 32521,22). Globally, drowned reefs may constitute an important fraction of postglacial carbonate21,23,24 and an alternative earlier source of postglacial carbon. Halimeda bioherms are another contributing component, with recent investigations from the GBR suggesting they are volumetrically relevant in postglacial carbonate budgets25,26,27.
Estimations of global and regional reef carbonate area and volume have been attempted using a range of assumptions13,15,28 and applying parameters (e.g. reef area) with large associated uncertainties. New datasets are, however, providing valuable constraints to these parameters within the GBR region. For example, new GIS datasets of reef boundaries29 have the potential to improve the estimations of reef area. Additionally, the recent surveys and investigations on the drowned shelf edge reefs of the GBR represent the most complete dataset investigating drowned reefs: IODP Exp. 325 well-dated fossil reef cores30,31, seismic lines32,33, multibeam bathymetry34, and surface sediment and rock dredge samples35,36. New detailed bathymetry and interpretations are also providing new constraints on the spatial distribution and volume of Halimeda bioherms in the northern GBR26,27.
In this paper we investigate the impact of drowned coral reefs and Halimeda deposits on regional (GBR shelf, northeastern Australia) and global postglacial shallow-water CaCO3 budgets. Our scientific objectives are to: (1) estimate the volume, mass and timing of postglacial shallow calcium carbonate deposition across the entire GBR using the most recent GIS datasets, data from two IODP Exp. 325 control zones from the shelf-edge reef system and the regional volume of the Halimeda bioherms; (2) extend the resulting volumetric and mass estimates globally based on assumptions ground-truthed in the GBR; and (3) compare our results with past regional and global volumetric and mass estimates.
The GBR shelf along the northeastern coast of Australia (Fig. 1) accommodates a thick succession of reef deposits over the last 600 ± 280 ky37,38 controlled by major glacial-interglacial sea-level fluctuations. The last glacial-interglacial fluctuation initiated during the LGM21,30 when sea level was approaching minimum levels (120–130 m below present)31,39.
As the glaciation ended and sea level rose during the postglacial, extensive fringing- and barrier-reef structures developed along the shelf edge of the GBR until ca. 10 ka BP21,40. These reefs currently lie between 40 and 130 m below present sea level and extend for more than 2000 km from the northern to the southern central GBR and possibly farther34,41,42 (Fig. 2). Beyond the 130 m depth contour, the shelf edge fore-reef sediments give way to hemipelagic sediments of carbonate and terrigenous origin on the upper continental slope43,44,45. Evidence suggests that the inter-reef areas of the shelf edge are covered by a relatively thin (0–5 m) layer of carbonate sands and mud, dominated by Halimeda fragments, foraminifera, mollusks and bryozoans35,36,46,47.
The shallower structures of the modern GBR were colonized after ca. 9 ka BP following the demise of the shelf-edge reefs. Since then, extensive reef development has occurred along the whole GBR from the vicinity of Fraser Island in the south, to Cape York in the north20,48. Both Pleistocene and Holocene reef deposits in the GBR display local and regional variations that are the expression of broader physiographic trends and of the physical processes linked to the postglacial marine flooding34,40,49.
Results and discussion
Holocene carbonate deposits
We estimated the areal trends of the Holocene reefs in the GBR. Reef area was estimated from GIS layers containing polygons representing the outline of the Holocene reefs (Figs. 1 and 2). This layer was obtained from a detailed interpretation of recently available satellite images and shallow bathymetry29,50, and excluding continental islands and shelf-edge reefs. These features were sliced into latitudinal 50 km wide slices to assess latitudinal variations. We assumed that the reef area polygons represented the main reef and bioclastic deposits directly related to Holocene reef growth. However, unaccounted fore- and back-reef aprons may constitute a significant portion of the reefal carbonate volume15,51.
We estimated the mass of the Holocene CaCO3 deposits by multiplying the area derived from the interpreted GIS layer by the thickness derived from historical reef cores that have drilled through the Holocene (Appendix 1) and petrophysical parameters (Aragonite density, ρA = 2930 kg m−3 and formation porosity, ΦR = 35%30). The volumetric and mass calculations were also performed at a sub-regional level in 50 km wide latitudinal slices that allowed reconstruction of latitudinal trends (Fig. 3e, Appendix 2).
Our area estimations show that Holocene reefs occupy approximately 10% of the total GBR shelf area, following a latitudinal trend that correlates with the total shelf area, especially in the central GBR (R2 = 0.84) between 14° and 21° S (Figs. 1, 3e). This reflects the direct relationship between substrate availability on the shelf and carbonate accumulation. Interestingly, in the northern GBR (near 12° S) the proportion of Holocene reef area-to-shelf area increases due to the wide (up to 30 km) reef structures. The seemingly obvious relationship is, however, a complex one and highly dependent on environmental variables (terrigenous flux, circulation, antecedent substrate, etc.) that can determine the spatial distribution of the carbonate deposits40,49,52,53,54.
Our new GBR Holocene CaCO3 mass estimates (Table 1) fall between the figures by Rees13 and Kinsey and Hopley55. The Rees13 reef area estimate of 44,920 km2, based on Spalding et al.56 dataset, is larger than the area presented in this study (26,290 km2, Table 2). Their Holocene CaCO3 estimate is consequently higher (1709 Gt CaCO3) than our best estimate of 751 Gt CaCO3. However, Rees13 include reefs in the Australian region that are not part of the GBR system sensu stricto. The Kinsey and Hopley55 estimated reef area value is more in agreement with our figure: ca. 20,000 km2. A more recent estimate places the GBR’s shallow-water reef area at 16,110 km250, but they do not include sediment wedges associated with these reefs, which are found at greater depths and constitute up to the double of the reef framework volume15,51. If we calculate the mass areal accumulation (MAA) using Rees13 estimates (Table 1) the resulting MAA is much higher (38,045 kg m−2) than even the highest MAA in Hydrographers Passage (27,648 kg m−2, Table 2), which seems unlikely. Even applying matching reef areas to Rees13 and Kinsey and Hopley55 results, these past estimates probably overestimate the Holocene carbonate deposits in the GBR.
Shelf edge reef CaCO3 accumulation
The volume and mass of the shelf edge deposits at a regional scale were ground-truthed in two control zones along the shelf edge of the GBR: Hydrographers Passage and Noggin Passage (Fig. 2). Here, extensive IODP drilling, bathymetric and seismic surveys30,34,40,47 provided valuable data for the calibration of the parameters required for the regional reconstruction of volumetrics and mass: reef area ratio, formation volume from seismic imaging, mass areal accumulation (MAA), vertical accretion rate, the maximum cumulative thickness and petrophysical parameters. A regional bathymetric dataset57 provided the basis for the reconstruction for the postglacial marine flooded area in the GBR (analogous to Hinestrosa et al.49).
Two methods were applied to obtain the volumetrics and mass of the shelf-edge deposits: (1) the mass areal accumulation method and (2) the postglacial thickness method. The former is a bulk calculation of volume based on flooded area and the accumulation represented by the MAA, scaled back by the proportion of bathymetric surface covered by reefs (reef area ratio) without considering any temporal evolution. The latter, the postglacial-thickness method, attempts to reconstruct the temporal evolution of the reef accretion by considering the change in flooded area since the LGM. It is layer-based, with each layer corresponding to a 5 m sea-level step in which data-derived thickness constraints (Fig. 4a, Appendix 3) are applied in such a way that vertical reef accumulation does not exceed observed thicknesses (Fig. 4b). It relies on the assumption that the reef area ratio, vertical accretion rate and maximum cumulative thickness values observed in the control zones can be extended to other locations along the GBR shelf edge. A composite sea-level curve based on Lambeck et al.39 and Yokoyama et al.31 (Fig. 5, Appendix 6) enabled the translation between past sea levels and geological ages to reconstruct the temporal evolution of the deposits.
The estimates obtained applying the mass areal accumulation method are lower than those estimated by applying the postglacial thickness method but are within the same order of magnitude. Not surprisingly, the application of both methods results in similar latitudinal trends (Fig. 3e) because in both the flooded area is a direct factor in the calculations.
In the control zones, Noggin Passage and Hydrographers Passage (Fig. 2), ca. 20% of the shelf edge is covered in reef structures (i.e., reef area ratio = ca. 20%). This proportion is almost twice the reef area ratio estimated at a regional scale for the shallower, Holocene reefs when considering the whole of the GBR shelf.
In both control zones (Table 2) we found that reef areas have MAA values above 10,000 kg m−2, whilst inter-reef areas display MAA values that are an order of magnitude lower (7767–8406 kg m−2). The southern control zone (Hydrographers Passage) has a higher average MAA (e.g., 20,393–35,003 kg m−2 in the outer barrier) than the northern site (Noggin Passage) in all the geomorphic areas assessed (e.g., 14,726–19,586 kg m−2 in the outer barrier). This is consistent with a thinner reef veneer (< 10 m) in the terrace and outer geomorphic areas and less distinguishable barrier structures found at Noggin Passage40.
Shelf edge trends
Volumetrically, the carbonate deposits of the shelf edge wane in the northern GBR when compared to the central and southern GBR (Fig. 3d, e). In the northern GBR, the Holocene and the shelf edge pre-Holocene reef trends are also contrasting: the Holocene reef deposits increase dramatically near 12° S, whereas the shelf edge deposits at those latitudes diminish, possibly due to limited substrate availability40. On the contrary, in the southern-central GBR (e.g. Hydrographers Passage control zone) wider and a more gentle gradient provides more substrate availability34.
It is useful to establish some comparisons to appreciate the magnitude of the shelf edge deposits. At the shelf edge, our estimates suggest that the area covered by reef formations is between 3000 and 11,000 km2 (Table 1), which would represent 8% (minimum case) to 30% (maximum case) of the total area occupied by all the banks in Harris et al.50, and between 12% (minimum case) and 48% (maximum case) of the area occupied by banks with no Holocene cover in that same study. Kleypas58 inferred that the global area available for reef growth during the LGM lowstand was approximately 20% of that available today. In the GBR, that figure is at least within the same order of magnitude of our estimations: a maximum shelf edge flooded area of ca. 29,523 km2 (best estimate, Table 1) representing 12% of the whole GBR shelf (ca. 249,762 km2).
Other carbonate deposits in the GBR
Halimeda bioherms are a significant component of the region’s postglacial carbonate budget. A comparison of the most up-to-date morphometric data27 shows that the postglacial Halimeda deposits are equivalent in mass to 5.5–10.5% of the Holocene reef mass on the GBR shelf (Table 1). Halimeda can form mounds in inter-reef areas of the GBR up to a thickness of 20 m25,26,27,59,60. Recent reviews of published and new high-resolution bathymetry have revealed that at least 6000 km2 of the northern and central GBR are covered by Halimeda bioherms26,27. This is a considerable increase from the ca. 2000 km2 from previous estimations59.
Halimeda-like morphologies have also been detected on the shelf edge in seismic profiles47 and Halimeda floatstones recovered in dredges from the shelf edge dated to 11.8–7.2 ka (D24B, D22, D11B in Abbey et al.36). Despite these new constraints, questions remain about the extent of pre-Holocene Halimeda deposits, particularly at the shelf edge.
Global and regional estimates
We extrapolated the estimates and trends of CaCO3 deposits for the GBR to the entire globe using the reef area estimate of Spalding et al.56. Using this area, we applied the parameters ground-truthed in the GBR dataset. The global reef area (RAGLOBAL) was multiplied by average thickness and petrophysical parameters (ρA, ΦR) to obtain global postglacial CaCO3 deposits. We accounted for the drowned postglacial reefs by applying two factors to the global Holocene estimates: a factor based in the ratio of shelf edge-to-Holocene reef area (area adjustment factor, AFA) and a factor based in the mass ratio (mass adjustment factor, AFM) (Table 3). These factors and the global extrapolation as such, have large associated uncertainties given the gaps in knowledge of total global extent, accretion trends and morphology of the less accessible postglacial drowned reefs. We also calculated the global volumetrics and mass globally using the reef areas from past studies (Tables 4, 5; Appendix 4).
We found that the reef area ratio at the shelf edge (ca. 20%) is twice the reef area ratio estimated for the whole GBR shelf (ca. 10% for Holocene reefs, Table 1). The structures with Holocene reefs occupy more absolute area but are sparse and separated by large extensions of flat sediment-covered submarine topography. At a global scale, previous studies suggest lower reef area ratio values: reef area (584 to 746 × 103 km2) and shelf area in low latitudes (11,686 × 103 km2) as reported in Kleypas58, suggesting a global reef area ratio of 5 to 6%. This percentage would be even lower if we apply the global reef areas of 300 × 103 km261, 255 × 103 km216 or 284 × 103 km256. The lower value of the global reef area ratio (5–6%) compared to the GBR values of this study (ca. 10%) could be partly explained by uncertainties in the topographic/bathymetric datasets used by Kleypas58 (e.g., ETOPO562), and by difficulties in predicting reef habitat using the ReefHab model58, or by the inclusion of shelf areas that are not potential reef habitats. It is also possible that the GBR had more favourable regional conditions for reef development compared to other global locations.
The global reef area estimate of 284,000 km2 by Spalding et al.56 is lower than estimates from other authors (Table 5), but it is based on a more comprehensive dataset compared to other studies. However, this dataset originates from a collection of data from different origins and scales which brings uncertainty, especially at a local scale. Their estimates refer mainly to the area occupied by modern coral reefs and would only represent a proxy for Holocene deposits rather for than the entire postglacial reef system, which should include early- and mid-postglacial drowned reefs.
Applying the global reef area above and the parameters ground-truthed on the GBR shelf, we obtain a global Holocene reef deposits estimate of ca. 8100 Gt CaCO3 in the best-case scenario (Table 3). This is very similar to past estimates reported in Rees et al.63 (Table 6). However, we must also consider other calcium carbonate deposits: inter-reef carbonates, Halimeda bioherms and drowned reefs. Applying a similar Halimeda-to-reef ratio to the one estimated in the GBR (Table 1) an extra 592 Gt CaCO3 would be added to the global carbonate budget of the last 8 ky (Table 3). The choice of the global reef area as a parameter is critical: a simple comparison of the same calculations but using areas from other studies (Table 5) reveals a large variation in total postglacial CaCO3 (Holocene + drowned reefs + Halimeda deposits) ranging from 4073 Gt CaCO364 to a maximum of 54,550 Gt CaCO365 (Table 4).
Incorporating the drowned reefs in global CaCO3 budgets
The role of coral reefs in postglacial oceanic alkalinity changes and atmospheric CO2 input is poorly constrained and partly relies on CaCO3 deposits estimates that are uncertain. The estimates of area covered by shallow-water carbonates, from which some global estimates are derived, are mainly associated with Holocene reefs13,16,61 (Table 5) and ignore the more elusive (now) drowned, deeper deposits. The submerged reefs discovered in different parts of the world21,23,24 should be incorporated into updated postglacial CaCO3 deposits estimates.
In the GBR, there is strong evidence of almost continuous shallow reef accretion from ca. 30 until ca. 9.5 ka BP along the shelf edge, albeit characterised by ~ five brief demise events21. We estimate that the total net CaCO3 deposits of the submerged shelf-edge reefs are equivalent to ca. 16 to 20% of the Holocene reef deposits mass in our best-estimate scenario, and up to ca. 40% if we consider higher values of reef area ratio, postglacial reef thickness or mass areal deposits (Table 1).
If we extend the shelf edge-to-Holocene reef ratios estimated in the GBR to global scales (mass adjustment factor AFM and areal adjustment factor AFA), we obtain a global value of 1460–1785 Gt CaCO3 accumulated in the drowned reefs from 19 to 10 ka BP. These results are modest compared to the combined Holocene reef deposits (ca. 8100 Gt CaCO3). However, given the direct evidence on large-scale pre-Holocene shelf edge reef systems in the GBR (only surveyed at scale in the last decade30) and past evidence of other large-scale drowned reefs in global locations23,24, the question of the impact of drowned reefs on the LGM-to-postglacial global CaCO3 budgets remains relevant.
The impact of the global reef area applied can be assessed by looking at average CaCO3 fluxes for the whole postglacial period (Table 3), which can vary from a minimum of 0.2 Gt CaCO3 y−1 (using area in De Vooys64) to a maximum of 3.2 Gt CaCO3 y−1 (using area in Copper65). However, if we split the averages between Holocene and pre-Holocene, we find the differences are of one order of magnitude (1.0 vs 0.2 Gt CaCO3 y−1; Table 3). This can be compared to some recent estimates of reef productivity of 1.9 Gt CaCO3 y−1 for the Holocene and 2.5–4.5 Gt CaCO3 y−1 for the late deglacial19, which were hard to reconcile with common carbon cycle models18. Our results are more in line with Vecsei and Berger66 who considered postglacial drowned reefs and reported values of 0.29–0.51 Gt CaCO3 y−1 for the Holocene and 0.15 Gt CaCO3 y−1 for the mid-late postglacial.
The timing of the shelf edge carbonate deposits
The timing of the CaCO3 deposits in the GBR, as approximated by the postglacial thickness method, suggests a possible concurrence between periods of maximum accumulation and rapid accretion rate (at ca. 12 and ca. 15.5 ka BP21). These were periods of high substrate availability and favourable environmental conditions for reef growth, as influenced by shelf physiography and sea-level rise21,49.
The postglacial thickness method cannot establish a precise chronology for CaCO3 mass accumulation at regional level, but it can provide a broad temporal trend. The periods of higher CaCO3 accumulation in the shelf edge (15.1–13.7 ka BP and 13.3–11.3 ka BP applying the 20 m maximum reef thickness assumption, Fig. 3b, Appendix 5) envelope at least two of the three episodes of increased slope of the atm-CO2 curve since the LGM (ca. 14.9–14.4 ka and ca. 13.0–11.5 ka BP67) (Fig. 3a,b). These periods of higher CaCO3 accumulation at the shelf edge also coincide with the episodes inferred by Ridgwell et al.5 in their models (17.0–13.8 ky and 12.3–11.2 ky BP). These findings are consistent with a more recent analysis of all available postglacial vertical reef accretion data (including IODP Exp. 325), which shows rapid accretion rates (9.6 to more than 20 mm yr−1) during these periods of higher CaCO3 accumulation (see Fig. S6 in Webster et al.21).
Our new estimates of postglacial, pre-Holocene carbonate deposits in the GBR (ca. 130 Gt CaCO3) and their global extrapolations (1500 Gt CaCO3) suggest that pre-Holocene reef accretion is likely to be more relevant to the global CaCO3 budgets (hence in the global carbon cycle) than currently recognized. The impact of these deposits in the atm-CO2 should be assessed by global process-based carbon models that reflect the full complexity of the atmosphere–ocean–land biogeochemical cycles (Fig. 6).
The assembled dataset provides new constraints on Holocene reef deposits in the GBR: 751 Gt CaCO3 as per our best estimate, varying between 520 and 1001 Gt CaCO3, distributed latitudinally with a strong correlation to the available shelf area.
The shelf-edge reefs of the GBR constitute an important portion of the postglacial shallow reef deposits: these (now) drowned reefs occupy an area of between 3000 and 12,000 km2, equivalent to ca. 10–45% of the total Holocene reef area in the GBR. In the GBR, these drowned reefs accumulated ca. 135 Gt of reefal CaCO3, equivalent to ca. 18% of the mass estimated for the more recent Holocene deposits (best estimate). The latitudinal distribution of the shelf edge reefs is also strongly correlated to shelf availability.
By globally extrapolating the GBR constraints, we estimate a total accumulation of 8100 Gt CaCO3 from Holocene reefs (best estimate), which is consistent with previously published estimates. Following from recently published results in the GBR, a minimum of ca. 590 Gt CaCO3 from Halimeda deposits should be added to the global Holocene CaCO3 mass, representing a 4–8% increase in the budget.
Global extrapolations supported by recent surveys suggest that a significant proportion of postglacial, pre-Holocene shallow-water carbonate deposits can be attributed to now drowned postglacial reefs. These deposits of ca. 1500 Gt CaCO3 represent 16–20% more mass in the global postglacial budget than if considering the Holocene reef deposits alone. Their inclusion in global carbon models could provide new constraints on postglacial global atmospheric and climate models.
Our results support a more prominent role in the postglacial carbon cycle for pre-Holocene shallow-water coral reefs. Significantly, the timing of higher CaCO3 deposition in the GBR is broadly coeval with two distinct episodes of postglacial atm-CO2 increase (ca. 14.9–14.4 ka and ca. 13.0–11.5 ka BP67). Any causal relationship must be confirmed by more complex, process-based models of the global carbon and other biogeochemical cycles and global surveys of drowned reefs and reef areas.
We estimated the carbonate volume in the GBR for: (1) early postglacial reef deposits (21–10 ka); and (2) Holocene reef deposits. We also attempted a global extrapolation of these carbonate deposits based on these new and well-constrained regional GBR estimates.
Data were available across the whole GBR: bathymetry at ~ 100 m resolution57, GIS layers with reef locations and extensions50; previous GBR Holocene drill cores (see Appendix 1 for summary and Hopley et al.68 for data sources). We distinguished the areas at the shelf edge (defined here between the modern outer GBR reef front and the 130 m isobath) from the other areas of the shelf and extracted the corresponding bathymetric subset.
More locally, data were available for two densely surveyed control zones at the shelf edge (Noggin Passage and Hydrographers Passage; Fig. 2) where reef volumetrics and mass accumulation were estimated with a high degree of confidence for Quaternary reefs. This was possible due to: (1) availability of seismic-derived three-dimensional reconstructions of the reef patterns and volumetrics40,47; (2) extensive and precise chronologic database (> 580 published U-Th and 14C ages), lithological and petrophysical properties directly measured from the IODP Exp. 325 drill holes and cores30,31; (3) high-resolution (5 m) bathymetric coverage in these sites34; and (4) extensive knowledge on the development history and age structure of the shelf-edge reef system21.
For all calculations, we assumed:
Aragonite density (ρA) = 2930 kg m−3
Reef formation porosity (ΦR) = 35%30.
To estimate the postglacial Pleistocene carbonate deposits, we first produced the following input for both of the estimation methods we applied:
Reef area ratio [%] at the shelf-edge control zones: the percentage of reef formation area extension compared to total shelf edge area (Fig. 2). This value was obtained by digitising the area occupied by reef banks and comparing it to the total shelf-edge area. The identification of the banks was supported by the bathymetry, backscatter, seismic and GIS data34,40,47,50. The results of both control zones were averaged and rounded to the nearest ten to obtain a best estimate of 20%. To capture plausible uncertainties, arbitrary minimum and maximum values were set: a minimum reef area ratio of 10% equivalent to the proportion of Holocene reef area ratio in the whole GBR shelf; and a maximum value of twice the best estimate.
Formation volume [m3] at the shelf-edge control zones: the volume contained between the present day, seafloor bathymetry and the antecedent basal substrate (Reflector 1) as obtained from the seismic interpretations40,47. The three different velocity scenarios (1700–3300 m s−1) to convert from seismic time to true depth47 were considered to obtain a minimum, best estimate, and maximum values for each set of maps.
Mass areal accumulation (MAA) [kg m−2] at the shelf-edge control zones: these values were calculated for each control zone by transforming each formation volume estimate to carbonate mass (CaCO3 mass = formation volume × ρA × (1—ΦR)) and subsequently dividing the mass by the total shelf edge area of the control zones (MAA = mass · [shelf edge area]−1). The calculations were also applied for each of the main geomorphic zones47: inner barrier, outer barrier, terrace and shelf break combined, and inner and outer platforms combined. Three values were applied to account for plausible minimum, best and maximum scenarios: the average MAA value of all reef locations, and the minimum and the maximum MAA value in any reef location (Table 2).
Vertical accretion rate [m ky−1] at the shelf-edge control zones: the glacial-postglacial boundary recognized in the cores and the radiometric ages measured in the Exp. 325 core samples21 allowed the estimation of the vertical accretion gradients (m ky−1) for the entire postglacial Pleistocene time period (21–10 ka) (Fig. 4, Appendix 3).
Maximum cumulative thickness [m], at the shelf-edge control zones: we estimated the maximum reef thickness for the different stages of postglacial shelfedge reef development from the vertical accretion rate plots. For one of the estimation methods (postglacial thickness method), this became a necessary constraint to avoid unrealistic cumulative reef thickness as sea-level rise progressed (Fig. 4).
Postglacial shelf margin flooded area, for each 5 m increment [km2]: we calculated the marine cover corresponding to past postglacial sea levels by performing surface operations in GIS software. We used the 100 m bathymetric dataset57 comprising the whole GBR, from northern Fraser Island to north of Cape York. We extracted the shelf-edge areas defining them as the areas between the outer GBR and the 130 m depth contour (Appendix 7). The bathymetric surface was sliced into thirty-three 50 km wide latitudinal zones after Hinestrosa et al.49. Each of the zones was flooded using sea levels ranging from 130 to 0 m in 5 m steps to obtain marine-flooded area in km2. To represent the timing of the flooded area at each sea-level increment, we applied a composite relative sea-level curve to the results in Hinestrosa et al.49 (Fig. 5, Appendix 6). The relative sea level was reconstructed from data in Lambeck et al.39, Yokoyama et al.31 and Webster et al.21 The flooded areas in each 5 m step were then matched to geological time according to sea levels represented in the relative sea-level curve (125–0 m).
The Holocene reef CaCO3 accumulation was calculated using the following parameters:
Reef area [m2] from the Queensland coast to the outer GBR: the reef area was estimated from GIS layers containing polygons representing the outline of the Holocene reefs (Figs. 1 and 2, Supplementary data). This layer was obtained from a detailed interpretation of recently available satellite images and shallow bathymetry29,50. Continental islands and reefs belonging to the shelf edge were excluded to better approximate Holocene reef area. These features were sliced into thirty-three latitudinal zones 50 km wide to capture the latitudinal variations (Figs. 1, 3e). We assumed that the reef area polygons represent the main reef and bioclastic deposits directly related to Holocene reef growth. However, unaccounted fore- and back-reef aprons may constitute a significant portion of the reefal carbonate volume15,51. There are of course, uncertainties inherent to the original sources (satellite imagery and bathymetric mapping) and their interpretation, which could result in an overestimation of the reef area in the northern GBR, the under or overestimation of the extent of the bioclastic cover, or the misrepresentation of some locations as Holocene reefs when they might be older Pleistocene outcrops50.
Reef thickness from Holocene GBR drill cores [m]: a dataset of Holocene reef thicknesses was used to estimate minimum, average and maximum thickness values for the Holocene reef thickness68 (Appendix 1). These drilling results show a Holocene reef veneer varying from less than 5 m to more than 25 m depending on location, with the thickest reefs recorded at around 18° S.
For the global extrapolations, we also considered the following parameters:
Area adjustment factor [%]: defined as the ratio of shelf-edge reef area to the Holocene reef area. According to our estimates in the GBR, this corresponds to 22% (Table 1).
Mass adjustment factor [%]: defined as the ratio of CaCO3 mass at the shelf edge to the CaCO3 mass of the Holocene reef. According to our estimates in the GBR, this corresponds to 18% (Table 1).
Postglacial pleistocene carbonate deposits
We followed two approaches. The postglacial-thickness method attempts to reconstruct the temporal evolution of the reef accretion by considering the change in flooded area since the LGM. The mass areal accumulation method does not consider the change in marine flooding area and outputs the cumulative postglacial volume and CaCO3 mass.
Shelf edge carbonate deposits—mass areal accumulation method
The mass areal accumulation method is based on one key assumption: that the reef area ratio and mass areal accumulation variables calculated locally at the Exp. 325 control zones are valid along the entire extension of the shelf edge.
For each latitudinal zone in the shelf edge bathymetric subset, the maximum highstand flooded area (FA) was multiplied by the reef area ratio (RAR) and mass areal accumulation (MAA) values to obtain CaCO3 accumulation values in the GBR shelf margin (Table 1).
Pleistocene CaCO3 mass = FA × RAR × MAA
Shelf edge carbonate deposits—postglacial-thickness method
The postglacial-thickness method relies on the assumption that reef area ratio, vertical accretion rate and maximum cumulative thickness values observed in the control zones can be extended to other locations along the GBR shelf edge. It also assumes that the parameters remain constant through time. By considering accretion rates and maximum thickness, this method allows us to approximate the temporal evolution of the shelf-edge deposits.
Firstly, the vertical accretion rate for each reef development episode (Webster et al., 2018) was converted to an equivalent rate relative to past sea-level steps. This allowed us to associate an incremental reef thickness to each of the 5 m sea-level steps considered. Conversion from geological age to equivalent sea level was performed using a simplified relative sea-level curve based on Lambeck et al.39 for ages more recent than 10 ka BP, and based on Webster et al.21, Yokoyama et al.31 for ages before 10 ka BP (Fig. 5, Appendix 6).
To obtain an estimate of reef volume at each sea-level step, we first estimated reef thickness by multiplying the converted postglacial vertical accretion rate (VASL) by each sea-level step (5 m). Subsequently, the product of this thickness and the flooded area at each flooding stage (FASL) gave us the formation volume for each one of the thirty-three latitudinal zones and for each sea-level step. The volume was scaled down by the reef area ratio (RAR) values (minimum, best estimate, maximum; Table 1) to obtain a measure representative of the shelf edge geomorphology as observed at the control zones. In the calculations, each flooded area had a cap on cumulative reef thickness: the maximum cumulative thickness (Fig. 4). The CaCO3 accumulated mass for each sea-level increase was obtained by multiplying these volumes by formation net volume (1-ΦR) and density (ρA):
Pleistocene CaCO 3 mass for each sea level (SL) between 130 and 0 m:
Incremental reef volume = VA SL × 5 m × FA SL × RAR
Incremental CaCO 3 mass = Incremental reef volume × ρ A × (1—Φ R )
Cumulative CaCO 3 mass = Σ (Incremental CaCO 3 mass)
Holocene veneer carbonate accumulation estimates
To obtain values of total CaCO3 mass of Holocene carbonate in the GBR, the reef thickness (RT) values were multiplied by the reef area (RA) to obtain cumulative Holocene carbonate volumes for the GBR as a whole and for each one of the thirty-three latitudinal zones (Fig. 1). Mass values were obtained by multiplying these volumes by formation net volume (1-ΦR) and density (ρA) (Table 1), as summarised below:
Holocene reef volume = RA × RT
Holocene reef CaCO3 mass = Holocene reef volume × ρA × (1 − ΦR)
We consider the contribution of drowned postglacial reefs in global CaCO3 budgets. We extrapolated the estimates and trends of CaCO3 deposits for the GBR to the entire globe. We used published estimates of global reef area and parameters ground-truthed by the GBR dataset. The global reef area (RAGLOBAL) was multiplied by average thickness (RT) and petrophysical parameters (ρA, ΦR) to obtain global postglacial CaCO3 deposits.
We accounted for the drowned Pleistocene reefs by applying two assumptions in our calculations to obtain two equivalent results.
Assumption 1: on average, the proportion of postglacial drowned reefs areas corresponding to a given Holocene reef area is similar across all reef provinces. We expressed this assumption as a ratio of shelf margin area to total Holocene reef area, the area adjustment factor (AFA),
Assumption 2: on average, the postglacial drowned reefs mass corresponding to a given Holocene reef mass is similar across all reef provinces. We expressed this assumption as a ratio of shelf margin CaCO3 mass to Holocene reef CaCO3 mass, the mass adjustment factor (AFM).
The values for global reef area (RAglobal) have a large range of uncertainty as demonstrated by the range of values proposed by different authors (Table 5). We consider those by Spalding et al.56 more accurate given the ground-truthing datasets. The factors that we applied on the global area (AFA, AFM) have a large associated uncertainty: despite the evidence for drowned reefs in other geographical locations, the exact global extension and morphology of drowned reefs is not well constrained. Other carbonate provinces might differ in morphology, in accretion trends and in the proportion of Pleistocene reefs present along their margins compared to the more recent Holocene deposits of those provinces.
Global postglacial CaCO3 accumulation = RAglobal × RTGBR × ρA × (1—ΦR)
Area-adjusted global postglacial CaCO3 mass = RAglobal × RTGBR × ρA × (1—ΦR) × (1 + AFA)
Mass-adjusted global postglacial CaCO3 mass = RAglobal × RTGBR × ρA × (1—ΦR) × (1 + AFM).
On CO2 and total C estimates
According to the coral reef hypothesis6,71, reefal CaCO3 accretion provides CO2 to the environment by increasing the concentration of CO2 in the ocean water. The equivalent CO2 and C mass based on the stoichiometry of the chemical reaction: Ca2+ + 2HCO3− = => CaCO3 + CO2 + H2O6,66 gives an incomplete picture because the exact proportion would depend on physical conditions that would have varied during the postglacial period. Experimentally, it has been demonstrated that for each mole of CaCO3 precipitated in seawater only a fraction of a mole of CO2 is fed to the surrounding waters due to the buffering effect of marine water8,72. It is then unclear how much of this carbon is released into the atmosphere, especially at centennial timescales66,72. The pathways for the released CO2 molecules are varied—they can be absorbed into inorganic or organic marine carbon cycles, or they can also be transferred into the atmosphere by the balancing of the partial pressure of CO2. We have not attempted to quantify the corresponding postglacial CO2 contribution to the surrounding waters and to the atmosphere. This would require more complex carbon models which are beyond the scope of this study.
Ciais, P. et al. Climate change 2013: The Physical Science Basis. Contribution of Working Group I to the Fifth Assessment Report of the Intergovernmental Panel on Climate Change. (Cambridge, United Kingdom, 2013).
O’Neill, C. M., Hogg, A. M., Ellwood, M. J., Opdyke, B. N. & Eggins, S. M. Sequential changes in ocean circulation and biological export productivity during the last glacial–interglacial cycle: A model–data study. Climate Past 17, 171–201. https://doi.org/10.5194/cp-17-171-2021 (2021).
Brovkin, V. et al. Comparative carbon cycle dynamics of the present and last interglacial. Quatern. Sci. Rev. 137, 15–32. https://doi.org/10.1016/j.quascirev.2016.01.028 (2016).
Kohfeld, K. E. & Ridgwell, A. Glacial-interglacial variability in atmospheric CO2. Surf. Ocean-lower Atmos. Process. 187, 251–286. https://doi.org/10.1029/2008GM000845 (2009).
Ridgwell, A. J., Watson, A. J., Maslin, M. A. & Kaplan, J. O. Implications of coral reef buildup for the controls on atmospheric CO2 since the last glacial maximum. Paleoceanography 18, 7–1. https://doi.org/10.1029/2003PA000893 (2003).
Berger, W. H. Deglacial CO2 buildup: Contraints on the coral reefs. Palaeogeogr. Palaeoclimatol. Palaeoecol. 40, 235–253. https://doi.org/10.1016/0031-0182(82)90092-X (1982).
Opdyke, B. N. & Walker, J. C. G. Return of the coral reef hypothesis: Basin to shelf partitioning of CaCO3 and its effect on atmospheric CO2. Geology 20, 733–736. https://doi.org/10.1130/0091-7613(1992)020%3c0733:Rotcrh%3e2.3.Co;2 (1992).
Ware, J. R., Smith, S. V. & Reaka-Kudla, M. L. Coral reefs: Sources or sinks of atmospheric CO2?. Coral Reefs 11, 127–130. https://doi.org/10.1007/BF00255465 (1992).
Broecker, W. S. & Henderson, G. M. The sequence of events surrounding Termination II and their implications for the cause of glacial-interglacial CO2 changes. Paleoceanography 13, 352–364. https://doi.org/10.1029/98pa00920 (1998).
Sowers, T., Bender, M., Raynaud, D., Korotkevich, Y. S. & Orchardo, J. The δ18O of atmospheric O2 from air inclusions in the Vostok Ice Core: Timing of CO2 and ice volume changes during the penultimate deglaciation. Paleoceanography 6, 679–696. https://doi.org/10.1029/91pa02023 (1991).
Shakun, J. D. et al. Global warming preceded by increasing carbon dioxide concentrations during the last deglaciation. Nature 484, 49–54. https://doi.org/10.1038/nature10915 (2012).
Milliman, J. D. & Droxler, A. W. Neritic and pelagic carbonate sedimentation in the marine environment: Ignorance is not bliss. Geol. Rundsch. 85, 496–504. https://doi.org/10.1007/BF02369004 (1996).
Rees, S. A. Coral reefs of the Indo-Pacific and changes in global Holocene climate PhD thesis, University of Southampton (2006).
Rees, S. A., Opdyke, B. N., Wilson, P. A. & Fifield, L. K. Coral reef sedimentation on Rodrigues and the Western Indian Ocean and its impact on the carbon cycle. Philos. Trans. R. Soc. Math. Phys. Eng. Sci. 363, 101–120. https://doi.org/10.1098/rsta.2004.1481 (2005).
Ryan, D. A., Opdyke, B. N. & Jell, J. S. Holocene sediments of Wistari Reef: towards a global quantification of coral reef related neritic sedimentation in the Holocene. Palaeogeogr. Palaeoclimatol. Palaeoecol. 175, 173–184. https://doi.org/10.1016/S0031-0182(01)00370-4 (2001).
Spalding, M. D. & Grenfell, A. M. New estimate of global and regional coral areas. Coral Reefs 16, 225–230. https://doi.org/10.1007/s003380050078 (1997).
Brovkin, V. et al. Carbon cycle, vegetation, and climate dynamics in the Holocene: Experiments with the CLIMBER-2 model. Global Biogeochem. Cycles 16, 86-1-86–20. https://doi.org/10.1029/2001gb001662 (2002).
Köhler, P. & Munhoven, G. Late Pleistocene carbon cycle revisited by considering solid Earth processes. Paleoceanogr. Paleoclimatol. https://doi.org/10.1029/2020PA004020 (2020).
Husson, L. et al. Reef carbonate productivity during quaternary sea level oscillations. Geochem. Geophys. Geosyst. 19, 1148–1164. https://doi.org/10.1002/2017gc007335 (2018).
Montaggioni, L. F. History of Indo-Pacific coral reef systems since the last glaciation: Development patterns and controlling factors. Earth Sci. Rev. 71, 1. https://doi.org/10.1016/j.earscirev.2005.01.002 (2005).
Webster, J. M. et al. Response of the Great Barrier Reef to sea-level and environmental changes over the past 30,000 years. Nat. Geosci. 11, 426–432. https://doi.org/10.1038/s41561-018-0127-3 (2018).
Camoin, G. F. et al. Reef response to sea-level and environmental changes during the last deglaciation: Integrated Ocean Drilling Program Expedition 310, Tahiti Sea Level. Geology 40, 643–646. https://doi.org/10.1130/g32057.1 (2012).
Woodroffe, C. D. & Webster, J. M. Coral reefs and sea-level change. Mar. Geol. 352, 248–267. https://doi.org/10.1016/j.margeo.2013.12.006 (2014).
Rovere, A. et al. Submerged reef terraces in the Maldivian Archipelago (Indian Ocean). Geomorphology 317, 218–232. https://doi.org/10.1016/j.geomorph.2018.05.026 (2018).
Rees, S., Opdyke, B., Wilson, P. & Henstock, T. Significance of Halimeda bioherms to the global carbonate budget based on a geological sediment budget for the Northern Great Barrier Reef Australia. Coral Reefs 26, 177–188. https://doi.org/10.1007/s00338-006-0166-x (2007).
McNeil, M. A., Webster, J. M., Beaman, R. J. & Graham, T. L. New constraints on the spatial distribution and morphology of the Halimeda bioherms of the Great Barrier Reef, Australia. Coral Reefs 35, 1343–1355. https://doi.org/10.1007/s00338-016-1492-2 (2016).
McNeil, M., Nothdurft, L., Dyriw, N. J., Webster, J. M. & Beaman, R. J. Morphotype differentiation in the Great Barrier Reef Halimeda bioherm carbonate factory: Internal architecture and surface geomorphometrics. Depos. Rec. https://doi.org/10.1002/dep2.122 (2020).
Smith, S. V. Coral-reef area and the contributions of reefs to processes and resources of the world’s oceans. Nature 273, 225. https://doi.org/10.1038/273225a0 (1978).
GBRMPA. Great Barrier Reef Features (Reef boundaries, QLD Mainland, Islands, Cays and Rocks). (Great Barrier Reef Marine Park Authority, 2013).
Webster, J. M., Yokoyama, Y., Cotterill, C. & Expedition 325 Scientists. in Proceedings of the Integrated Ocean Drilling Program (Integrated Ocean Drilling Program Management International, Inc., for the Integrated Ocean Drilling Program, 2011).
Yokoyama, Y. et al. Rapid glaciation and a two-step sea level plunge into the Last Glacial Maximum. Nature 559, 603–607. https://doi.org/10.1038/s41586-018-0335-4 (2018).
Tilbrook, B. & Matear, R. RV Southern Surveyor—Voyage Summary SS09/2008: Carbon Geochemistry of the Great Barrier Reef (Marine National Facility, 2008).
Webster, J. M., Davies, P. J., Beaman, R. J, William, S. & Byrne, M. RV Southern Surveyor—Voyage Summary SS07/2007. 18 (Marine National Facility 2008).
Abbey, E., Webster, J. M. & Beaman, R. J. Geomorphology of submerged reefs on the shelf edge of the Great Barrier Reef: The influence of oscillating Pleistocene sea-levels. Mar. Geol. 288, 61–78. https://doi.org/10.1016/j.margeo.2011.08.006 (2011).
Renema, W., Beaman, R. J. & Webster, J. M. Mixing of relict and modern tests of larger benthic foraminifera on the Great Barrier Reef shelf margin. Mar. Micropaleontol. 101, 68–75. https://doi.org/10.1016/j.marmicro.2013.03.002 (2013).
Abbey, E. et al. Deglacial mesophotic reef demise on the Great Barrier Reef. Palaeogeogr. Palaeoclimatol. Palaeoecol. 392, 473–494. https://doi.org/10.1016/j.palaeo.2013.09.032 (2013).
Alexander, I. et al. New constraints on the origin of the Australian Great Barrier Reef from an international project of deep coring. Geology 29, 483–486. https://doi.org/10.1130/0091-7613(2001)029%3c0483:NCOTOO%3e2.0.CO;2 (2001).
Humblet, M. & Webster, J. M. Coral community changes in the Great Barrier Reef in response to major environmental changes over glacial-interglacial timescales. Palaeogeogr. Palaeoclimatol. Palaeoecol. 472, 216–235. https://doi.org/10.1016/j.palaeo.2017.02.003 (2017).
Lambeck, K., Rouby, H., Purcell, A., Sun, Y. & Sambridge, M. Sea level and global ice volumes from the Last Glacial Maximum to the Holocene. Proc. Natl. Acad. Sci. U.S.A. https://doi.org/10.1073/pnas.1411762111 (2014).
Hinestrosa, G., Webster, J. M. & Beaman, R. J. Postglacial sediment deposition along a mixed carbonate-siliciclastic margin: New constraints from the drowned shelf-edge reefs of the Great Barrier Reef, Australia. Palaeogeogr. Palaeoclimatol. Palaeoecol. 446, 168–185. https://doi.org/10.1016/j.palaeo.2016.01.023 (2016).
Beaman, R. J., Webster, J. M. & Wust, R. A. J. New evidence for drowned shelf edge reefs in the Great Barrier Reef, Australia. Mar. Geol. 247, 17–34. https://doi.org/10.1016/j.margeo.2007.08.001 (2008).
Doblin, M. A. et al. RV Southern Surveyor—Voyage Summary T03/SS2013 (Marine National Facility, 2013).
Bostock, H. C., Opdyke, B. N., Gagan, M. K. & Fifield, L. K. Late Quaternary siliciclastic/carbonate sedimentation model for the Capricorn Channel, southern Great Barrier Reef province, Australia. Mar. Geol. 257, 107–123. https://doi.org/10.1016/j.margeo.2008.11.003 (2009).
Dunbar, G. B., Dickens, G. R. & Carter, R. M. Sediment flux across the Great Barrier Reef Shelf to the Queensland Trough over the last 300 ky. Sed. Geol. 133, 49. https://doi.org/10.1016/S0037-0738(00)00027-0 (2000).
Harper, B. B. et al. Mixed carbonate-siliciclastic sedimentation along the Great Barrier Reef upper slope: A challenge to the reciprocal sedimentation model. J. Sediment. Res. 85, 1019–1036. https://doi.org/10.2110/jsr.2015.58.1 (2015).
Beaman, R. J. et al. in Seafloor Geomorphology as Benthic Habitat: GeoHab Atlas of Seafloor Geomorphic Features and Benthic Habitats (ed P.T. Harris, Baker, E.K.) 425–434 (Elsevier, 2011).
Hinestrosa, G., Webster, J. M., Beaman, R. J. & Anderson, L. M. Seismic stratigraphy and development of the shelf-edge reefs of the Great Barrier Reef, Australia. Mar. Geol. 353, 1–20. https://doi.org/10.1016/j.margeo.2014.03.016 (2014).
Davies, P. J. & Hopley, D. Growth fabrics and growth rates of Holocene reefs in the Great Barrier Reef. BMR J. Aust. Geol. Geophys. 8, 237–251 (1983).
Hinestrosa, G., Webster, J. M. & Beaman, R. J. Spatio-temporal patterns in the postglacial flooding of the Great Barrier Reef shelf, Australia. Cont. Shelf Res. 173, 13–26. https://doi.org/10.1016/j.csr.2018.12.001 (2019).
Harris, P. T. et al. Submerged banks in the Great Barrier Reef, Australia, greatly increase available coral reef habitat. ICES J. Mar. Sci. 70, 284–293. https://doi.org/10.1093/icesjms/fss165 (2012).
Heap, A. D., Harris, P. T. & Fountain, L. Neritic carbonate for six submerged coral reefs from northern Australia: Implications for Holocene global carbon dioxide. Palaeogeogr. Palaeoclimatol. Palaeoecol. 283, 77–90. https://doi.org/10.1016/j.palaeo.2009.08.003 (2009).
Seard, C., Borgomano, J., Granjeon, D. & Camoin, G. Impact of environmental parameters on coral reef development and drowning: Forward modelling of the last deglacial reefs from Tahiti (French Polynesia; IODP Expedition #310). Sedimentology https://doi.org/10.1111/sed.12030 (2013).
Camoin, G. et al. in EGU General Assembly 2009 Conference Abstracts. 1994.
Montaggioni, L. F. & Braithwaite, C. J. R. in Developments in Marine Geology Vol. 5 550 (Elsevier, 2009).
Kinsey, D. W. & Hopley, D. The significance of corals reefs as global carbon sinks—Response to Greenhouse. Palaeogeogr. Palaeoclimatol. Palaeoecol. 89, 363–377. https://doi.org/10.1016/0031-0182(91)90172-N (1991).
Spalding, M. D., Ravilious, C. & Green, E. World Atlas of Coral Reefs (University of California Press, Berkeley, 2001).
Beaman, R. J. 3DGBR: A high-resolution depth model for the Great Barrier Reef and Coral Sea. 12 (2010).
Kleypas, J. A. Modeled estimates of global reef habitat and carbonate production since the Last Glacial Maximum. Paleoceanography 12, 533–545. https://doi.org/10.1029/97pa01134 (1997).
Drew, E. A. & Abel, K. M. in Proceedings of The Fifth International Coral Reef Congress. 15–20.
Orme, G. R. & Salama, M. S. Form and seismic stratigraphy of Halimeda banks in part of the northern Great Barrier Reef Province. Coral Reefs 6, 131–137. https://doi.org/10.1007/BF00302009 (1988).
Vecsei, A. A new estimate of global reefal carbonate production including the fore-reefs. Global Planet. Change 43, 1–18. https://doi.org/10.1016/j.gloplacha.2003.12.002 (2004).
Sloss, P. W. (Marine Geology and Geophysics Division, N.G.D.C. (Ed.), Boulder, Colorado., 1986).
Rees, S., Opdyke, B., Wilson, P., Keith Fifield, L. & Levchenko, V. Holocene evolution of the granite based Lizard Island and MacGillivray Reef systems, Northern Great Barrier Reef. Coral Reefs 25, 555–565. https://doi.org/10.1007/s00338-006-0138-1 (2006).
De Vooys, C. in Scientific Committee on Problems of the Environment (SCOPE) Series (1979).
Copper, P. Ancient reef ecosystem expansion and collapse. Coral Reefs 13, 3–11. https://doi.org/10.1007/BF00426428 (1994).
Vecsei, A. & Berger, W. H. Increase of atmospheric CO2 during deglaciation: Constraints on the coral reef hypothesis from patterns of deposition. Global Biogeochem. Cycles https://doi.org/10.1029/2003gb002147 (2004).
Bauska, T. K., Marcott, S. A. & Brook, E. J. Abrupt changes in the global carbon cycle during the last glacial period. Nat. Geosci. 14, 91–96. https://doi.org/10.1038/s41561-020-00680-2 (2021).
Hopley, D., Smithers, S. G. & Parnell, K. E. The Geomorphology of the Great Barrier Reef (Cambridge, 2007).
Honisch, B. et al. The geological record of ocean acidification. Science 335, 1058–1063. https://doi.org/10.1126/science.1208277 (2012).
Ridgwell, A., Zondervan, I., Hargreaves, J. C., Bijma, J. & Lenton, T. M. Assessing the potential long-term increase of oceanic fossil fuel CO2 uptake due to CO2-calcification feedback. Biogeosciences 4, 481–492. https://doi.org/10.5194/bg-4-481-2007 (2007).
Andersson, A. J. & Mackenzie, F. T. Shallow-water oceans: a source or sink of atmospheric CO2?. Front. Ecol. Environ. 2, 348–353. https://doi.org/10.1890/1540-9295(2004)002[0348:Soasos]2.0.Co;2 (2004).
Wollast, R., Garrels, R. M. & Mackenzie, F. T. Calcite-seawater reactions in ocean surface waters. Am. J. Sci. 280, 831–848. https://doi.org/10.2475/ajs.280.9.831 (1980).
Newell, N. D. An outline history of tropical organic reefs. Am. Mus. Novit. 2465, 1–37 (1971).
Milliman, J., Mueller, G. & Foerstner, U. Marine Carbonates. Recent Sedimentary Carbonates, Part 1 (Springer-Verlag, 1974).
Hillis, L. Coralgal reefs from a calcareous green algal perspective and a first carbonate budget. In: Proceedings of the 8th International Coral Reef Symposium (eds. Lessios, H.A., & Macintyre, I.G.,) Vol. 1. 761–766. (Smithsonian Tropical Research Institute, Panama, 1997).
Thanks to Thomas Felis for the insights on the carbon isotopic cycle and its relation to Quaternary coral reef growth. Financial support was provided by the Australian Research Council (grant no. DP1094001) and ANZIC (Australian and New Zealand International Ocean Discovery Program). Research supported by a grant of sea time on RV Southern Surveyor from the CSIRO Marine National Facility.
The authors declare no competing interests.
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The original online version of this Article was revised: The Supplementary Information 3 file published with this Article contained an error where irrelevant data samples, incorrect or out-of-date references, and inconsistent notations obscured the results of the postglacial accretion trends and affected their reproducibility.
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Hinestrosa, G., Webster, J.M. & Beaman, R.J. New constraints on the postglacial shallow-water carbonate accumulation in the Great Barrier Reef. Sci Rep 12, 924 (2022). https://doi.org/10.1038/s41598-021-04586-w