Climate plays a central role in coral-reef development, especially in marginal environments. The high-latitude reefs of southeast Florida are currently non-accreting, relict systems with low coral cover. This region also did not support the extensive Late Pleistocene reef development observed in many other locations around the world; however, there is evidence of significant reef building in southeast Florida during the Holocene. Using 146 radiometric ages from reefs extending ~ 120 km along Florida’s southeast coast, we test the hypothesis that the latitudinal extent of Holocene reef development in this region was modulated by climatic variability. We demonstrate that although sea-level changes impacted rates of reef accretion and allowed reefs to backstep inshore as new habitats were flooded, sea level was not the ultimate cause of reef demise. Instead, we conclude that climate was the primary driver of the expansion and contraction of Florida’s reefs during the Holocene. Reefs grew to 26.7° N in southeast Florida during the relatively warm, stable climate at the beginning of the Holocene Thermal Maximum (HTM) ~ 10,000 years ago, but subsequent cooling and increased frequency of winter cold fronts were associated with the equatorward contraction of reef building. By ~ 7800 years ago, actively accreting reefs only extended to 26.1° N. Reefs further contracted to 25.8° N after 5800 years ago, and by 3000 years ago reef development had terminated throughout southern Florida (24.5–26.7° N). Modern warming is unlikely to simply reverse this trend, however, because the climate of the Anthropocene will be fundamentally different from the HTM. By increasing the frequency and intensity of both warm and cold extreme-weather events, contemporary climate change will instead amplify conditions inimical to reef development in marginal reef environments such as southern Florida, making them more likely to continue to deteriorate than to resume accretion in the future.
Climate and subtropical coral-reef development
Anthropogenic climate change is now considered to be the primary cause of coral-reef degradation globally1,2. Although the rate and magnitude of coral loss over the last 50 years may be without precedent in recent millennia3, climate has been a primary control on the rate, duration, and spatial extent of reef development throughout geologic history4,5,6,7,8,9,10. Coral-reef development is generally most extensive and most rapid in tropical environments, where temperatures are warm and stable11,12. Although recent coral-reef degradation has been driven primarily by elevated ocean temperatures1,2, many declines in the past have been attributed to cooling trends4,5,9,13,14,15,16. In environments where thermal conditions are marginal, even minor cooling has the potential to suppress or even shut down reef-building by species that evolved in the tropics4,9,11,14,17,18. Whereas a number of recent studies have suggested that marginal environments—high-latitude habitats, mesophotic reefs, and locations with elevated turbidity or upwelling—could serve as refugia from warming for thermally sensitive coral taxa19,20,21,22, most of these ecosystems do not support reef accretion at present20. An important question, therefore, is whether and how the response of marginal reefs to climatic trends in the past can be used to project the future development of today’s degrading reef ecosystems6,7 in response to anthropogenic warming trends and the impact of those recent trends on both warm and cold thermal extremes.
Climatic variability during the Holocene was moderate compared with changes over longer geologic intervals4,5,23. The Holocene epoch was nonetheless characterized by significant thermal variability over multidecadal to millennial timescales23,24. Average global temperatures peaked ~ 10–6 thousand years ago (ka)—an interval known as the Holocene Thermal Maximum (HTM)—before declining significantly over the Middle to Late Holocene24,25. Whereas tropical environments are buffered from the most extreme thermal variability, subtropical habitats are sensitive to broad-scale climatic oscillations26,27,28. For example, the relatively warm climate of the HTM drove temporary poleward expansions of corals in Florida29, the northern Gulf of Mexico30, and the high-latitude Pacific (e.g., in Japan17, China16, and the Tasman Sea15).
Florida’s subtropical reefs currently exist near the thermal minimum for reef development9,11,31,32,33, and periodic winter cold events frequently push them below this threshold18,31,32,34,35. As a result, contemporary reef growth throughout southern Florida is negligible9,36; however, recent range expansions of reef-building corals in Florida and other high-latitude locations have led to the suggestion that subtropical environments may serve as refugia for these corals in a future, warmer world19,20,29,30. It is unclear whether such range expansions would translate into expansions of reef-building in subtropical habitats. Here, we test the hypothesis that the latitudinal limits of reef-framework construction on Florida’s subtropical reefs were controlled primarily by climate during the Holocene. We track the changing geography of reef accretion along the northern extent of the Florida reef tract over the last ~ 10,000 years and compare the climatic drivers of Holocene and Anthropocene reef development to project the future of reef-building in marginal environments such as southern Florida.
Reconstructing Holocene reef development on the SFCRT
The Florida Reef Tract extends more than 500 km along Florida’s Atlantic coast from Dry Tortugas National Park to northern Palm Beach County (Supplementary Fig. S1). It can be divided into two subregions based on their distinct geomorphology and geologic histories: the Florida Keys reef tract (FKRT) and the Southeast Florida Continental Reef Tract (SFCRT). Fowey Rocks reef in Biscayne National Park marks the northern extent of the FKRT (25.6° N)31,33, which extends southwest along the Florida Keys to the Dry Tortugas9,37. Whereas the FKRT has recently supported abundant populations of reef-building corals, the SFCRT to the north is a ‘relict’ reef system38, characterized by low-relief, hardbottom habitats with low coral cover32,39,40 (Fig. 1). The presence of extensive, shore-parallel reef-ridge structures or ‘terraces’ extending along much of the SFCRT38,40,41 is suggestive, however, of reef development during some periods of the Holocene38 (Fig. 1a; Supplementary Fig. S2; https://maps.ngdc.noaa.gov/viewers/bathymetry/).
The SFCRT extends ~ 120 km along Florida’s southeast coast from just north of Fowey Rocks to northern Palm Beach County (Fig. 2, Supplementary Fig. S1). Although the continental shelf of southeast Florida is relatively narrow at just 3–4 km wide38,40, new mapping efforts have demonstrated that the SFCRT includes five discrete, parallel reef terraces (Supplementary Fig. S1; https://maps.ngdc.noaa.gov/viewers/bathymetry/). Listed in order of distance from shore (after Walker et al.40), these habitats are the Nearshore Ridge Complex (NRC; 3–5 m depth), Inner Reef (IR; ~ 8 m depth), Middle Reef (MR; ~ 15 m depth), Outer Reef (OR; ~ 16 m depth), and Deep Ridge (DR; > 25 m depth). Whereas all five reef habitats are present south of Hillsboro Inlet, the IR is absent north of the inlet, the MR terminates in southern Palm Beach County, and the OR only extends to central Palm Beach County40 (Supplementary Fig. S1). (Note Banks et al.38 suggested that the IR may actually extend slightly north of the Hillsboro inlet, as its northern limit could be obscured by seaward progradation of Florida’s shoreline.) The DR, which is a low-relief, hardbottom habitat rather than a true reef terrace, extends the furthest north, terminating near the boundary between Palm Beach and Martin Counties40. The distance between these habitats also varies with latitude, with the IR, MR, and OR converging in south Miami, just north of Fowey Rocks. The best developed habitats on the SFCRT are the OR and IR38,42, which are the focus of this study (Fig. 2). Previous geological characterizations of those reef ridges off Broward County suggest that they accumulated at least 10.0 and 3.7 m of reef framework during the Holocene, respectively38,41,42.
In shallow-water environments of the western Atlantic, including southern Florida, the elkhorn coral Acropora palmata was until recently the dominant reef-building coral during the late Quaternary31,43,44 (Fig. 1, Supplementary Fig. S3) and the presence of A. palmata reef framework is generally associated with periods of active reef accretion in the past9,31,44,45,46. We therefore used the ages of sub-fossil A. palmata to determine the timing and spatial extent of reef-building along the IR and OR of the SFCRT during the Holocene (Fig. 2). Data from the less-developed MR38 and from other coral species are included for comparison, but were not used to draw major conclusions about the history of reef development.
We collected and radiometrically dated 62 new samples, including 52 A. palmata, from several previously unsampled locations along the SFCRT: 16 from the reef-surface in central and northern Palm Beach County and 46 from the reef-surface and reef framework in southern Miami-Dade County. We combined these data with 64 previously published ages from reefs in Broward County38,41,42,47,48. We also included 15 ages from the deep-water ‘Outlier Reef’ off Fowey Rocks, in south Miami, which grew contemporaneously with the OR49 and is structurally analogous, even though it is considered to be part of the FKRT38. The full dataset of radiometric ages is provided in Toth et al.50 (https://coastal.er.usgs.gov/data-release/doi-P9Z21NMU/) and the data used in this study are summarized in Table S1. Although we describe the specific locations where samples were collected in the following sections, our results focus on summarizing the history of reef development on the IR and OR within three subregions of the SFCRT: Palm Beach County (“Palm Beach”), Broward County (“Broward”), and Miami-Dade County (“Miami”). The aggregated data form an extensive dataset of Holocene reef development across a latitudinal gradient spanning the full ~ 120 km of the SFCRT.
Expansion and contraction of the SFCRT
Unlike the FKRT, which largely grew atop antecedent, late-Pleistocene reef framework31,37,51, there is no evidence of significant Pleistocene reef growth along the SFCRT. Indeed, the northern end of the FKRT is the limit of both contemporary reef development in southern Florida and of Late Pleistocene reefs31 (~ 400–125 ka). From Fowey Rocks north, a combination of coquina ridges and mixed carbonate/siliciclastic sandstones serve as the bedrock for the Holocene SFCRT9,38,42,51. The absence of Pleistocene reef deposits within the bedrock of the SFCRT suggests that reef growth was largely restricted to the lowest latitudes of southern Florida for much of the late Quaternary.
Beginning ~ 10 ka, however, the latitudinal range of reefs dominated by A. palmata expanded into shallow-water environments from south Miami to central Palm Beach County (Fig. 2; see Supplementary Discussion). Reef-accretion rates during the Early Holocene (~ 11.7–8.2 ka) ranged from 5.0 to 14.8 m per thousand years (m ky−1) and averaged 8.3 m ky−1 (± 3.8 standard error [SE]; Table 1), rivaling the most rapid rates of reef growth in the western Atlantic12,45,46. This pace of reef accretion would have been sufficient for the reefs to keep up52 with rapid Early Holocene sea-level rise47,53 (Supplementary Fig. S4), suggesting that environmental conditions in the nearshore habitats of southeast Florida were favorable for reef development at the time.
During the Middle to Late Holocene (8.2–4.2 ka and 4.2 ka–present, respectively) the SFCRT backstepped inshore and contracted to the south (Fig. 2). We used a non-parametric Kernel Density Estimate analysis (KDE; see “Methods”) to construct probability distributions of the surface ages from the IR and OR in each subregion. We interpret the peaks of those distributions to represent the last period of reef development at each location before reef accretion terminated. Reef accretion on the OR ceased throughout the SFCRT by the beginning of the Middle Holocene (Fig. 3a); however, the peak of the last period of reef growth on the OR in Miami, at 7.9 ka (95% confidence interval (CI) of KDE: 8.5–5.1 ka), occurred significantly later than in Broward (8.2 ka; 95% CI of KDE: 9.8–7.7 ka) or Palm Beach (9.0 ka; 95% CI of KDE: 9.8–7.5 ka; Kruskal–Wallis test: H2 = 18.47, p < 0.001; Nemenyi test: p < 0.001). The youngest ages for this final period of reef growth at each location were 7.2, 8.1, and 7.8 ka, respectively. There was a second peak of A. palmata ages on the OR in Miami at ~ 5.5 ka (± 0.2 SE; Fig. 3a), but it is not clear whether this represents a resumption of reef development or a short-lived, isolated population.
By the beginning of the Middle Holocene, rising sea level had flooded new shallow-water habitats throughout southeast Florida53, allowing the IR to initiate 1–2 km inshore of the OR in some locations40,42; however, the extent and duration of the inshore expansion of the SFCRT varied by latitude (Fig. 2). The most complete records of IR development, from central Broward, suggest that accretion initiated on the IR by ~ 8 ka42. The average accretion rate of A. palmata reefs there was ~ 3.5 m ky−1 (± 0.8 SE; Fig. 2; Table 1), which is comparable to average Holocene accretion rates elsewhere in the western Atlantic12,45,46.
We were only able to collect reef-surface samples from the Miami IR and cannot directly evaluate when A. palmata reefs established there; however, the similarity of the depth of the Pleistocene bedrock in this subregion (− 10 m MSL51) to the depths of the initiation surfaces on the IR of Broward (− 9 to − 12 m MSL)38,42, suggests that the IR likely established around the same time in both locations (see Supplementary Discussion). In contrast, the IR in Miami continued growing significantly longer—nearly 3 ky longer—after the Broward IR had shut down (Fig. 3b; youngest ages: 3.1 versus 5.7; peak of KDE: 3.2 versus 6.1, 95% CIs of KDE: 5.5–2.5 and 7.4–5.5 ka, respectively ; Mann–Whitney U test: U = 112, p < 0.001).
The IR is absent north of the Hillsboro Inlet in northern Broward County (Fig. 2; Supplementary Fig. S1)40, likely because of the lack of hardbottom antecedent substrata and abundance of unconsolidated sediments inshore of the OR at the northern limits of the SFCRT38. Indeed, a seismic profile off Delray Beach (26.5° N) in southern Palm Beach County interpreted by Finkl et al.54 suggested that the shallowest antecedent substrate available inshore of the OR there is at a depth of approximately 25 m. That would have been too deep for A. palmata reefs to establish during the Middle Holocene (i.e., ~ 13–20 m paleodepth from 8.2–6 ka)53. The only shallower inshore, consolidated substrate is the NRC, which is presently at a depth of around -4 m MSL40, but this feature would not have flooded until ~ 5 ka40,53.
Sea-level change and reef development
Before high-resolution data from the Broward IR were available, some researchers55,56 suggested that the > 500-yr gap and difference in elevation between published ages from the OR41,47 and IR48 of the SFCRT indicated that rapid, 6- to 7-m sea-level rise at ~ 8 ka shut down the development of the OR by reef-drowning. We revaluate this hypothesis in the context of our expanded dataset of A. palmata ages from southern Florida and recent sea-level reconstructions for the region53,57. The data we present on sea level in south Florida during the Holocene (Fig. 4A) are from a high-resolution (~ 50-y) output of the empirical statistical model of Holocene relative sea-level variability developed by Khan et al.53 (outputs published in Toth et al.58). Although we present the predictions of this model for the south Florida subregion, the model incorporates spatial correlations in sea level and, therefore, is reflective of regional trends from sea-level proxy data collected throughout the tropical western Atlantic53.
Several recent studies of Holocene sea level from the western Atlantic support the conclusion that sea level rose gradually over the transition from the Early to Middle Holocene49,53,57 (Fig. 4A), with modeled rates of sea-level rise of ~ 4.2 m ky−1 from ~ 8.5 to 7.5 ka in south Florida53. The empirical data are also consistent with the trends in sea-level rise predicted by regional geophysical models57. There is some evidence based on sea-level reconstructions from the northern Gulf of Mexico of an abrupt, centennial-scale rise in sea level associated with the draining of glacial Lake Agassiz during the 8.2 ka cooling event60. Although it is possible that this period of rapid sea-level rise may not have been detected in the existing sea-level models, the predicted magnitude of sea-level change in the tropical western Atlantic associated with that event would have been on the scale of decimeters rather than meters (i.e., only 20–40 cm in south Florida)60. Together, these reconstructions suggest that although high rates of sea-level rise at ~ 8.2 ka have been implicated as a driver of reef demise in a number of locations around the world15,55,56, the evidence for an abrupt sea-level jump at this time that would have been large enough to cause reef drowning is not robust in many locations59, including southern Florida49.
New data demonstrate that the early phases of IR growth in Broward were contemporaneous with the final period of reef growth on the OR42 (Fig. 2), suggesting that the gap in ages used to hypothesize a sea-level jump was a sampling artifact49. The elevations of the youngest A. palmata samples from the OR were ~ 4.5 and 2.2 m deeper than the oldest samples from the IR in Broward and Miami, respectively; however, the paleodepths of the OR would still have been within the 0 to ~ 5 m depth range preferred by the species47 in all three subregions (~ 4.1 m in Palm Beach at 7.8 ka , ~ 5.0 m in Broward at 8.1 ka, and ~ 2.7 m in Miami at 7.2 ka based on the Khan et al.53 sea-level reconstruction) and growth of the OR was keeping pace with sea level at the time of its shutdown (Table 1; Fig. 4A; Supplementary Fig. S3). There is also no evidence on the OR of a deepening-upward transition from A. palmata to massive corals that would have been characteristic of a reef-drowning event52. Instead, the upper surfaces of the OR were dominated by A. palmata, indicating their continued position near sea level47 (see “Methods”; Supplementary Fig. S3). Together, this evidence suggests that a driver other than sea-level change is needed to explain the termination of reef development on the OR of the SFCRT.
Similarly, although rising sea level promoted the initiation of the IR in some locations by flooding antecedent surfaces inshore of the OR, sea level cannot explain the demise of the IR. Accretion during the Middle Holocene on the IR was significantly slower than during the Early Holocene on the OR in Broward (Table 1; t-test: t11 = 2.96, p = 0.013), because of the relatively lower rates of sea-level rise after ~ 8 ka (3.9–2.1 m ky−1 from 8.1–5.8 ka)53; however, rates of A. palmata accretion on the IR continued to keep pace with sea level throughout the Middle Holocene (Supplementary Fig. S3). This, combined with the fact that many of the records from the Broward IR show a shallowing-upward transition from massive corals to A. palmata42, precludes the possibility of reef drowning38. The mean depth of the surface of the IR ranges between ~ 8 and 10 m at present40, suggesting that reef growth on the IR also has not been suppressed by a lack of accommodation space (cf. Toth et al.9).
Another hypothesis for the shutdown of Early Holocene reefs in the western Atlantic was that resuspension of terrigenous sediments from sea-level flooding of inshore areas caused reef drowning due to light limitation and eutrophication41,52,61,62. By the time the offshore reefs stopped growing, however, reef growth had initiated in inshore environments, where turbidity and nutrient loading would have been highest, which negates this hypothesis42,46,62 (Fig. 3). Although reef backstepping can certainly occur as a result of either rapid sea-level rise15,55,56 or an inimical offshore environment52,61, our data from the SFCRT support the conclusion that it can also occur in the absence of these drivers. In many cases, backstepping may simply be a part of the natural evolution of reef ecosystems as rising sea level creates new habitats inshore46,62,63. It is unclear what ultimately caused the OR in Broward and Miami to be abandoned when reef development continued on the IR in those locations, but similar scenarios of unexplained reef demise in other western Atlantic locations (e.g., the U.S. Virgin Islands and Puerto Rico) suggests a common, yet unidentified, driver46,62.
Climate and the latitudinal shutdown of the SFCRT
Whereas A. palmata reef growth off Miami was continuous from ~ 10–3 ka, in Broward, reef development ceased by ~ 5.7 ka. At the northern limits of the SFCRT in Palm Beach, reefs only grew until ~ 7.8 ka (Figs. 2, 3). This produced a latitudinal gradient in the timing of reef shutdown (Supplementary Fig. S4; linear regression: F1,36 = 247.4, p < 0.001, r2 = 0.87, Termination Age = 5515.1*Latitude − 138024.5). Although the development of the SFCRT was controlled by the interaction between antecedent geomorphology, sea-level rise, and climate, we argue that climate was the primary driver of its contraction and eventual demise.
The global distribution of coral reefs is generally limited to locations where minimum seawater temperatures exceed ~ 18 °C 11. In southern Florida, temperatures typically remain above this minimum, but winter cold-fronts periodically push reefs below that threshold31, limiting modern reef development in the region29. For example in January of 1977 and 2010, Florida’s reefs experienced two of the most extreme cold events on record, with prolonged low-temperature excursions causing significant coral mortality throughout much of the region32,34,35. Because A. palmata is particularly cold-sensitive, even more moderate cold fronts would have been sufficient to limit its historic distribution to habitats south of the SFCRT31,33 and suppress significant reef accretion over millennial timescales29. Currently, extreme cold fronts impact southern Florida with a period of ~ 20 years18; however, it is likely that climate modulated the periodicity and geography of cold-front impacts during the Holocene.
The primary control on the frequency of winter cold fronts reaching southern Florida is the intensity of meridional versus zonal atmospheric circulation over North America (Fig. 5), with strong meridional flow forcing increased penetration of cold fronts to the south18,26 (see Supplementary Discussion). Because these subregional patterns of atmospheric circulation are produced by broader-scale drivers of regional climate27, changes in meridional flow are reflected in various paleoclimate records25,27,64. For example, a more southerly position of the inter-tropical convergence zone (ITCZ) is associated with increased meridional circulation and a southerly shift of the polar jet stream25,27. Conversely, a more northerly position of the ITCZ is associated with increased zonal circulation and a northerly shift of the polar jet stream25,27. High-resolution reconstructions of local, millennial-scale temperature variability from the marine environments of southeast Florida are not available at present and we were unable to directly reconstruct climate variability in this study due to limited sampling of the western Atlantic corals that have been shown to produce high-fidelity paleoclimate data: Orbicella faveolata and Siderastrea siderea28. For these reasons, and because our A. palmata ages only record the timing of reef shutdown rather than the full history of reef development in many locations, we were not able to statistically evaluate the relationship between climate and reef-building. Instead, for the following discussion we rely on broad correlations between reef development and Holocene variability in global-scale temperature23,24 (Fig. 4B), the mean position of the ITCZ25 (Fig. 4C), and other paleorecords indicative of changes in meridional circulation over the eastern United States64,65 (see Supplementary Discussion) to evaluate the likely role of cold-front variability on the latitudinal contraction of reef-building in south Florida. We acknowledge that there is some debate about the timing and spatial fingerprint of temperature changes related to the HTM; however, the general trend of Early to Middle Holocene warming followed by Late Holocene cooling suggested by the composite record we rely on here24 (Fig. 4B), was reproduced by an updated, more comprehensive (but lower-resolution) reconstruction66 (Supplementary Fig. S5), validating the occurrence of a global HTM. Furthermore, recent studies have demonstrated that oceanographic and climatic variability in the subtropical habitats of south Florida are strongly linked to broader-scale changes in Northern-Atlantic climate28,67 (see Supplementary Discussion), which is the primary driver of the global signature of the HTM in those records. These lines of evidence suggest that the global trends in Holocene temperature reflected in Fig. 4B provide a reasonable proxy for mean temperature variability in south Florida.
The expansion of the Florida Reef Tract throughout southeast Florida during the Early Holocene coincided with the onset of warmer global temperatures associated with the HTM beginning ~ 10 ka23,24,29 (Fig. 4B; Supplementary Fig. S5). The ITCZ also occupied its northernmost position of the Holocene during this interval25 (Fig. 4C), which would have constrained the polar jet stream to high latitudes27. Furthermore, records of marine aerosol flux to the Greenland ice sheet indicate that by ~ 10 ka meridional circulation was weak64 (see Supplementary Discussion). All this suggests that the HTM was likely a time of warmer average temperatures and fewer cold fronts in southeast Florida. We hypothesize that this more tropical climate allowed for the northern expansion of A. palmata reef development throughout the SFCRT.
The termination of reef development at the northernmost limit of the SFCRT in Palm Beach between ~ 9.0 and 7.8 ka (Figs. 2, 3; peak of KDE and youngest age; see “Methods”), coincides with an interval of enhanced meridional circulation inferred from the Greenland record (8.8–7.8 ka)64, a brief southerly excursion of the ITCZ25 (Fig. 4C), and moderate cooling of the North Atlantic23 (the 8.2-ka event; Fig. 4B). Although the occurrence and magnitude of lower-latitude cooling associated with the 8.2-ka event is debatable (Supplementary Fig. S5), the changes in atmospheric circulation at this time would likely have produced cooler winters at the northernmost extent of the SFCRT (Fig. 5c). That winter cooling, we argue, extirpated cold-sensitive A. palmata populations18,29. By the time conditions once again became favorable for A. palmata to recolonize the Palm Beach OR, sea levels would have risen by nearly 5 m (from 9.0 to 7.8 ka; Fig. 4A)53, pushing those habitats beyond the preferred depth range of the species47. With no suitable shallower inshore habitats available in this subregion38, Acropora-dominated reefs would have been unable to reestablish after 7.8 ka (see Supplementary Discussion).
Reef growth continued further south on the IR of Broward until 6.1–5.7 ka (Figs. 2, 3), when a second major period of enhanced meridional circulation was recorded in Greenland64 (6.1–5.0 ka) and the ITCZ had continued to move south25 (Fig. 4C). Whereas the record from Greenland is suggestive of a short-term increase in the frequency and/or intensity of cold-fronts reaching south Florida, the longer-term shift in the position of the ITCZ may suggest that the frequency at which cold fronts were reaching lower latitudes was also gradually increasing over time. Thus, whereas Broward’s reefs were not critically affected by the period of colder winters that suppressed reef development in Palm Beach between ~ 9.0 and 7.8 ka, we hypothesize that by 6.1–5.7 ka severe cold fronts were reaching the lower-latitude reefs in Broward with high enough frequency to impair reef development (Fig. 5c). By this time, the global climate had also begun to cool following the peak of the HTM24 (Fig. 4B; Supplementary Fig. S5). A cooler mean climate in southeast Florida by the Middle Holocene may have brought average temperatures in Broward closer to the lower thermal threshold for reef development, making them more vulnerable to the later increase in cold-front frequency, leading to their shutdown by 5.7 ka.
Global temperatures cooled substantially during the Late Holocene24 (Fig. 4B; but see Supplementary Fig. S5), which would have likely brought reefs at the lowest latitudes of southeast Florida near their lower thermal threshold. The beginning of the Late Holocene was also characterized by a phase shift in atmospheric circulation from zonal to meridional dominance27, suggesting cold-front frequency in the lowest latitudes of southern Florida would have increased substantially relative to the Middle Holocene26 (Fig. 5c). This inference is supported by another interval of enhanced marine-aerosol flux in Greenland64 (3.1–2.4 ka), a negative North Atlantic Oscillation18,26,65 (4.5–2.0 ka), and extreme southern excursions and high variability in the position of the ITCZ25 (Fig. 4C). We hypothesize that these changes were responsible for the termination of reef building on the southernmost reefs of the SFCRT by 3.2–3.1 ka (Figs. 2, 3). The demise of reefs on the SFCRT around 3.0 ka also coincides with the shutdown of reef building on the FKRT further south9, suggesting that climate has been suppressing reef growth throughout southern Florida for at least the last three millennia.
Although reef communities established on the less-developed MR habitats38 and inshore of the IR on the NRC50 during the Late Holocene, there is no evidence of significant reef accretion at these locations (Supplementary Table S2; Supplementary Fig. S3). Whereas lower accommodation space as a result of minimal Late Holocene sea-level rise53 may have contributed to the lack of vertical reef accretion on the NRC, populations of reef-building corals were also extirpated from those reefs by 2 ka, which was is also likely a result of cooling. The depth of the MR is intermediate to that of the IR and OR and the average elevation of the MR is between -14.1 and -16.9 m MSL at present40, suggesting that accommodation space would not have been limiting there. Based on the limited data available, there is no evidence that A. palmata reefs ever formed on the MR, and the rates of reef accretion by massive corals there during the Middle to Late Holocene were significantly lower than on the IR (t-test: t6 = 3.34, p = 0.008). The two Late-Holocene ages we obtained from the MR in Miami (1.4 and 0.5 ka50) were from unattached Mancinia areolata colonies that are commonly found in sea grass habitats, suggesting that the MR may represent a back-reef habitat that formed when the OR was accreting, rather than a well-developed fore-reef like the IR and OR.
Most modern reefs throughout southern Florida are dominated by generalist or weedy corals44, primarily Siderastrea siderea, Porites astreoides, Millepora alcicornis, Stephanocoenia intersepta, and Montastraea cavernosa in southeast Florida68; however, most of these species have relatively low capacity for carbonate production and they have not contributed significantly to the construction of Florida’s reefs44. Furthermore, in southeast Florida, recent cold-stress events were associated with increases in the abundance of non-calcifying organisms including gorgonians and fleshy macroalgae32. It is likely that the same suite of taxa would have colonized the relict reefs of the SFCRT during the Holocene following cold-related mortality of A. palmata, but unlike A. palmata, these non-reef-building taxa would have made little if any subsequent contribution to the reef framework.
Lessons from marginal reef environments
Most reefs in the tropical western Atlantic grew more-or-less continuously during the Holocene, and reef development in many parts of the world was more strongly influenced by sea level than by climate45,46,59,69. In the marginal, high-latitude environments of southeast Florida, sea-level rise facilitated backstepping of reefs into inshore habitats during the Middle Holocene, but latitudinal expansion and contraction of Florida’s reefs appears to have been most strongly modulated by climatic variability9,29. The relatively warm, stable climate of the HTM allowed reefs in Florida and other high-latitude locations15,16,17,29,30 to expand their ranges poleward during the Early Holocene. As the climate cooled and the frequency of winter cold fronts increased, however, the SFCRT contracted equatorward. The shutdown of reef-building at the southernmost limits of the SFCRT at ~ 3 ka coincides with the termination of reef-building throughout the FKRT, which also appears to have occurred as a result of cooling9. A recent reconstruction of reef development from subtropical reefs in southeastern China16 likewise implicated cooling following the HTM as a likely cause of declines in development, which, in combination with the records from southern Florida, suggests that subtropical reefs may generally be more sensitive to climatic variability than those in more tropical locations. In addition, marginal reefs in the eastern tropical Pacific that experienced strong, seasonal, cold-water upwelling were more vulnerable to millennial-scale climatic perturbations during the Holocene than reefs with more stable annual temperatures (i.e., in the Gulf of Panama8 and the Gulf of Papagayo, Costa Rica13). Whereas moderate levels of thermal variability can increase the resilience of reefs to modern climatic extremes21,22,70,71, these studies of Holocene reef development suggest that in marginal habitats, where variability in the physical environment is especially high, periodic disturbances may be more likely to push reefs past critical environmental thresholds for continued survival and reef-building9,11,22,71.
Although populations of thermally sensitive acroporid corals have periodically expanded their ranges north to the SFCRT in recent decades in response to contemporary warming29, and historic records suggest that many reefs on the FKRT had high coral cover as recently as the early 1970s31, carbonate production and reef accretion have remained negligible in most locations throughout southern Florida9,36. Furthermore, recent thermal- stress events and the devastating outbreak of stony coral tissue loss disease have significantly reduced the abundance of reef-building corals throughout the SFCRT32,72. As a result, the reef framework constructed over millennia is now rapidly eroding9,73,74. Active management and the restoration of reef-building corals has the potential to re-establish some key ecological processes and mitigate the problem of erosion on Florida’s reefs43,44, but a resumption of reef-building on the SFCRT is unlikely, at least on decadal to centennial scales. Whereas coral populations have the potential to respond to favorable conditions in the short-term, the geological process of reef-building is more vulnerable to environmental variability and more difficult to restore once it is lost9.
Although the return to a warmer mean climate could be favorable for high-latitude reef development7,15,16,17,19,29,30, analogizing future climate to the HTM may be a false comparison. Anthropogenic climate change is not simply driving global warming: it is amplifying changes in the frequency, intensity, and geography of extreme-weather events19,75,76. For example, the increasing frequency and severity of high-temperature extremes will continue to cause widespread coral bleaching and outbreaks of infectious coral disease around the world1,2,69,72,76, and even putative cooler-water coral refugia such as high-latitude reefs, mesophotic reefs, and upwelling zones are not immune to these impacts20. Because the coral assemblages in these marginal environments are already depauperate and are isolated from the diminishing source populations elsewhere in the Caribbean, they may be even less resilient to climate change and other anthropogenic impacts than most ‘mainstream’ reefs20. Additionally, as a result of the disproportionate contemporary warming of the high-latitude northern Hemisphere (i.e., Arctic Amplification), climate change may be amplifying the trend of suppressed zonal circulation77,78, favoring meridional flow patterns that are reminiscent of the longer-term shift that occurred during the Middle to Late Holocene27,77,78 (Fig. 5). These changes have produced a weaker and more “wobbly” jet stream and have been linked to increases in the frequency of extreme winter cold events in the mid-latitudes and subtropics since the 1990s77,78. Many models suggest that climate change will continue to increase the frequency of winter extremes in a number of locations, including the southeastern United States in the future75. The impacts of increased thermal variability—in both directions—may, therefore, be most keenly felt in subtropical environments like southeast Florida19, although more work is needed to assess the generality of this pattern. We conclude that climate change will likely be more limiting to framework-building corals in subtropical environments than in tropical environments, negating the potential for subtropical habitats to support renewed reef development.
Samples from previous studies
The earliest data from the SFCRT reef subsurface were provided by Lighty et al.41,47 from a 450-m-long trench excavated through the OR for construction of a wastewater pipeline off northern Broward County. Five distinct facies were recognized within the internal structure of the OR, clearly demonstrating that it possessed a classical Caribbean-reef zonation dominated at the reef-crest by A. palmata. Ten A. palmata samples of Early Holocene age were collected from − 16.5 to − 27.0 m MSL41,47. Similarly, Shinn et al.51 described massive-coral facies of Middle Holocene age from offshore northern Miami-Dade County in outcrop from a dredge excavation through an “intermediate ridge” at − 13.7 m MSL (i.e., between the MR and OR, sensu Banks et al.38) and from a wastewater-pipe excavation through the IR at − 9.8 m MSL (samples MD-IR-BH-16.1 and MD-IR-ST-9.8, respectively in Toth et al.50).
A series of more recent studies from reefs off central and southern Broward County38,42 detailed the internal composition of the IR. A trench caused by the grounding of the submarine USS Memphis79,80 afforded yet another opportunity to observe and date intact reef framework (Supplementary Fig. S2c). Researchers reported that the IR was at least 3 m thick at this location and consisted of mixed A. palmata and massive-coral framework42. Ten samples collected from the trench created by the grounding of the USS Memphis at − 7.8 to − 9.5 m MSL48,80, and an additional three samples from the same location dated by Stathakopoulos and Riegl42, were all of Middle Holocene age. Follow-up studies from several nearby locations on the IR using core-drilling techniques yielded similar results38,42.
Collection of reef-surface samples
Between August and November 2013, ABM and AEO collected a total of 12 reef-surface samples from four randomly selected sites on the OR offshore of Boynton Beach in Palm Beach County (26.51° N, 80.03°W). At each site, exposures of internal reef framework were haphazardly sampled within two randomly selected 10 × 10 m quadrats using a hammer and chisel. Eight representative samples from the site were selected for radiometric dating in this study. On 7 July 2019, ABM and AEO collected eight additional A. palmata samples from the upper surface of the OR offshore of West Palm Beach, Florida, ~ 20 km north of the Boynton Beach location. Three samples were collected from a dome-shaped reef with ~ 4.5 of m vertical relief called Turtle Rocks (26.72° N, 80.03°W), which marks the northernmost extent of the OR in Palm Beach County. Five samples were collected just south of that location from a 2-m-deep trench in the reef surface that had previously been dredged for a sewage outfall (26.70° N, 80.02°W; Supplementary Fig. S2d). The samples were collected using an underwater Nemo handheld drill with a 4-cm-diameter diamond-tipped drill bit. The water depth of each sample was recorded in the field using a digital dive computer and later tide-corrected to MSL using data obtained from the NOAA tide station at the Lake Worth Pier in Lake Worth, Florida (Station ID: 8722670; https://tidesandcurrents.noaa.gov/).
During the Fall of 2013, 17 permanent monitoring sites were established on the IR and OR off Miami Beach, Florida (25.75° N, 80.11°W) as part of the compliance monitoring for the Port Miami (Government Cut) Deepening Project81. There were nine stations on the IR and eight on the OR. At each site, three permanent transects were established by installing markers at 0, 10, and 20 m along each transect. In addition, three sediment stations were established adjacent to each transect at each site. To install permanent markers at each of the monitoring stations, a total of 12 holes were drilled into the reef surface with a hydraulic-powered rotary drill using a 2.5-cm-diameter coring bit (Supplementary Fig. S6). JHH and WFP collected a total of 204 core plugs that penetrated 5–10 cm into the reef surface. Of these, 96 cores were retrieved from the IR and 108 from the OR. Of the collected cores, 78 (72%) from the IR and 90 (94%) from the OR were composed of A. palmata. We haphazardly chose 10 cores from the IR and 16 cores from the OR for dating. WFP collected four additional surface samples by hand from other locations in south Miami: one A. palmata sample from the southern end of the IR and OR where the two reef-lines merge just south of Key Biscayne, but north of Fowey Rocks (25.64° N, 80.10°W), one A. palmata from the OR in the same area, and two Ma. areolata samples from the MR near Government Cut (25.75° N, 80.11°W).
We note that although we cannot definitively demonstrate that all of the surface samples of A. palmata we collected in this study were in their original growth positions, they were all collected from well-cemented reef framework, suggesting that they are likely in situ and not storm-ridge deposits. Furthermore, our observations of the exposed IR and OR in Miami (Government Cut; Fig. 1a) indicate that these reefs are primarily composed of in situ reef framework. Similarly, we cannot verify that the ages we used from previous studies were all from in situ corals49,82; however, those studies described sampling well-developed reef framework38,41,42,47 and the dated sequences generally had well-ordered chronologies49,50, suggesting that those samples were not allochthonous deposits.
Collection of reef-framework samples
On 8 May 2017, WFP, LTT, and MLR collected a total of 29 subfossil coral fragments by hand from the southern channel-wall of Government Cut, where the channel cuts through the in situ reef framework of Miami’s OR (Fig. 1a; Supplementary Fig. S2a,b; 25.76° N, − 80.09° W). Prior to sampling, divers laid out 50-m transects running east and west from a central point along the top surface of the channel wall. Sampling was conducted at the central point (0 m) and every 25 m along the transect lines. At each 25-m mark, divers haphazardly collected one or more coral samples near the top (− 12 m relative to MSL), middle (− 14 m MSL), and bottom (− 16 m MSL) of the channel wall. The water depth of each sample, as determined by dive computers, was recorded in the field. The in situ depth measurements were later tide-adjusted to depths relative to MSL using data from the NOAA tide station on Virginia Key, FL (Station ID: 8723214; https://tidesandcurrents.noaa.gov/), located 8 km SW of the site. For this study, 11 of the best-preserved samples of A. palmata and five samples of other coral species, representing a depth range of − 10.7 to − 17.1 m MSL, were selected for radiometric dating.
We determined the ages of 62 of the newly collected sub-fossil corals from throughout southeast Florida: eight from the surface of the OR off West Palm Beach, eight surface samples from the OR off Boynton Beach, four surface corals collected from south Miami, 26 of the surface cores collected from the IR and OR around Government Cut, and 16 of the corals collected from within the OR framework of Government Cut50.
Samples free from any visually observable diagenetic alteration were collected from the internal skeletons of those corals using tile saws dedicated to that purpose at the USGS Saint Petersburg Coastal Marine Science Center or at Florida Atlantic University. All samples were sonicated in a bath of warm (~ 25–35 °C), deionized water for 15 min to remove detrital material from the skeletal matrix and were acid-etched to remove surficial contaminants prior to radiocarbon analysis. The samples from Boynton Beach were also soaked in a diluted 8% sodium hypochlorite solution to remove organics and pre-screened for evidence of diagenetic alteration using a combination of X-ray diffraction and petrographic analysis of thin sections. Those samples contained no detectable calcite and only minimal secondary aragonite.
All of the surface samples from West Palm Beach, eight of the reef-surface samples collected around Government Cut, and two of the Boynton Beach samples were dated by accelerator mass spectrometry (AMS) at the Woods Hole Oceanographic Institution’s National Ocean Sciences AMS Center (NOSAMS). The remaining six corals from Boynton Beach were dated by AMS at the Center for Applied Isotope Studies at the University of Georgia. The samples from south Miami were processed at the USGS Radiocarbon Laboratory in Reston, Virginia and were AMS-dated at the Lawrence Livermore National Laboratory. The remaining surface samples from around Government Cut were AMS dated at the Keck Carbon Cycle AMS Laboratory at UC Irvine using the rapid dating methodology described by Bush et al.83. Although this method results in higher analytical uncertainties (i.e., lower precision) than for samples dated using the standard AMS procedure, it has been shown to produce ages with high accuracy84. Dating methods for the ages derived in previous studies38,41,42,47,48,51,85 can be found in those publications (see also Toth et al.58 and Stathakopoulos and Toth82). Conventional radiocarbon ages were corrected for the fractionation of δ13C based on measured δ13C, or δ13C = 0 ± 4‰ if δ13C was not measured. All radiocarbon ages were calibrated to years before present (where ‘present’ is 1950 C.E.) using the Marine13 calibration curve86 in Calib 7.0.2 software (http://www.calib.org). In order to account for the temporally variable, local radiocarbon reservoir-age offset (ΔR) in southern Florida67, each radiocarbon age was assigned a predicted ΔR (see Toth et al.50) from an empirical model of Holocene ΔR variability developed by Toth et al.67,87. Two U-series ages from Stathakopoulos and Riegl42 were excluded from our analysis because elevated 232Th indicated the possibility of contamination by detrital thorium, and an additional sample from that dataset was excluded because it was likely transported from its original depositional environment49,82. All radiometric age data, sample depths (and uncertainties), and sample metadata are provided in Toth et al.50 (https://doi.org/10.5066/P9Z21NMU).
Determining reef-accretion rates and termination
Where possible, we used the ages from vertical sequences to estimate vertical accretion rates during intervals in the history of the SFCRT (see Supplementary Discussion). Accretion rates were calculated by dividing the depth interval over which a sequence was deposited by its timespan (lower minus upper age of that interval). Accretion rates from the OR of Miami were derived from a vertical transect of samples from A. palmata framework collected from Government Cut. For the previously published records38,42,85, we used published core logs42,58 to identify which intervals in the cores were dominated by A. palmata, massive corals, or mixed assemblages. Although we did not find a significant difference in accretion by massive, A. palmata, or mixed facies (Supplementary Discussion and summarized in Supplementary Table S2), for consistency, we focus our discussion on trends in accretion of A. palmata facies as this was the only taxon present throughout the entire Holocene record.
The time at which reef development terminated at each site was determined based on the ages of A. palmata samples collected within 1 m of the reef surface50. The timing of termination of the OR and IR in each subregion was visualized using non-parametric Kernel Density Estimation (KDE) using the IsoplotR package v.3.388. KDE creates a smoothed probability density curve based on the weighted distances of data within a sliding probability distribution function (kernel) window. The shape of the kernel (width of the window) is defined by a bandwidth parameter within the KDE. The IsoplotR package uses an adaptive bandwidth modifier89 that increases the bandwidth where data are sparse and decreases the bandwidth where the data are dense88. In our KDE analysis, we used a starting bandwidth of 300 years, based on the mean total (positive plus negative) 2σ uncertainty in the radiometric ages of 287 years in the dataset. The peaks in the KDE represent clustering in the distribution of A. palmata ages near the reef surface, which we assume to represent the last period of reef development in any given location. Termination of reef accretion most likely would have occurred sometime between this peak and the youngest A. palmata age at that location. We used this range of ages as a conservative estimate of the timing of reef shutdown rather than simply relying on the youngest A. palmata ages at each location because minimum ages are subject to sampling biases.
OR-termination ages were compared among subregions using a Kruskal–Wallis test and Nemenyi post-hoc test because the data were not normally distributed even after natural-log or square-root transformation. For this analysis, we did not include three A. palmata ages from the OR of Miami that were significantly younger (by > 2.3 ky on average) than the rest of the ages in the dataset (Mann–Whitney U test: U = 48, p = 0.002). These ages represent a separate, later interval when A. palmata was present on the Miami OR that would have biased the comparison among subregions. Without additional sampling it is not possible to determine if these ages represent the resumption of reef development on the Miami OR or a short-lived, isolated population. The timing of IR-termination in Broward and Miami was compared using a Mann–Whitney U test because the data were not normally distributed even after natural-log and square-root transformation. Final termination ages (the OR in Palm Beach and the IR in, separately, Broward and Miami) were compared along a latitudinal gradient using a linear regression. The residuals of the model were normally distributed (Shapiro–Wilk test: W = 0.95, p = 0.83) with untransformed data. Accretion rates of A. palmata reefs were compared between the Early and Middle Holocene in the Broward subregion using an independent t-test. The data were normal (Shapiro–Wilk test: W = 0.96, p = 0.82) and homogeneous (Levene’s test: F1,11 = 1.86, p = 0.20) after natural-log transformations. We also compared the rates of reef accretion during the Late Holocene by massive corals on the IR to the single estimate of reef accretion on the MR, 0.8 m ky−1 (Supplementary Table S2), using a one-sample t-test. The IR data were normal without transformation (Shapiro–Wilk test: W = 0.85, p = 0.12). All statistical analyses were conducted using RStudio v.3.6.390.
Hughes, T. P. et al. Coral reefs in the Anthropocene. Nature 546, 82–90. https://doi.org/10.1038/nature22901 (2017).
Bruno, J. F., Côté, I. M. & Toth, L. T. Climate change, coral loss, and the curious case of the parrotfish paradigm: Why don’t marine protected areas improve reef resilience?. Ann. Rev. Mar. Sci. 11, 307–334. https://doi.org/10.1146/annurev-marine-010318-095300 (2019).
Aronson, R. B., Macintyre, I. G., Wapnick, C. M. & O’Neill, M. W. Phase shifts, alternative states, and the unprecedented convergence of two reef systems. Ecology 85, 1876–1891 (2004).
Stanley, G. D. The history of early Mesozoic reef communities: A three-step process. Palaios 3, 170–183 (1988).
Copper, P. Ancient reef ecosystem expansion and collapse. Coral Reefs 13, 3–11 (1994).
Flügel, E. Pangean shelf carbonates: Controls and paleoclimatic significance of Permian and Triassic reefs. In Pangea: Paleoclimate, Tectonics, and Sedimentation During Accretion, Zenith, and Breakup of a Supercontinent Vol. 288 (ed Klein, G.D.) 247–266 (Geological Society of America Special Paper, 1994).
Kiessling, W., Simpson, C., Beck, B., Mewis, H. & Pandolfi, J. M. Equatorial decline of reef corals during the last Pleistocene interglacial. Proc. Natl. Acad. Sci. 109, 21378–21383. https://doi.org/10.1073/pnas.1214037110 (2012).
Toth, L. T. et al. ENSO drove 2500-year collapse of eastern Pacific coral reefs. Science 337, 81–84 (2012).
Toth, L. T., Kuffner, I. B., Stathakopoulos, A. & Shinn, E. A. A 3,000-year lag between the geological and ecological shutdown of Florida’s coral reefs. Glob. Change Biol. 24, 5471–5483. https://doi.org/10.1111/gcb.14389 (2018).
Toth, L. T. & Aronson, R. B. The 4.2-ka event, ENSO, and coral reef development. Clim. Past. 15, 105–119. https://doi.org/10.5194/cp-15-105-2019 (2019).
Kleypas, J. A., McManus, J. W. & Meñez, L. A. B. Environmental limits to coral reef development: Where do we draw the line? Am. Zool. 39, 146–159 (1999).
Dullo, W.-C. Coral growth and reef growth: A brief review. Facies 51, 33–48 (2005).
Glynn, P. W., Druffel, E. M. & Dunbar, R. B. A dead central American coral reef tract: Possible link with the Little Ice Age. J. Mar. Res. 41, 605–637 (1983).
Toth, L. T. et al. Climatic and biotic thresholds of coral-reef shutdown. Nat. Clim. Change 41, 369–374 (2015).
Woodroffe, C. D. et al. Response of coral reefs to climate change: Expansion and demise of the southernmost Pacific coral reef. Geophys. Res. Lett. 37, https://doi.org/10.1029/2010GL044067 (2010).
Clark, T. R. et al. Episodic coral growth in China’s subtropical coral communities linked to broad-scale climatic change. Geology 47, 79–82. https://doi.org/10.1130/g45278.1 (2018).
Veron, J. E. N. Environmental control of Holocene changes to the world’s most northern hermatypic coral outcrop. Pac. Sci. 46, 405–425 (1992).
Boucek, R. E., Gaiser, E. E., Liu, H. & Rehage, J. S. A review of subtropical community resistance and resilience to extreme cold spells. Ecosphere 7, e01455. https://doi.org/10.1002/ecs2.1455 (2016).
Beger, M., Sommer, B., Harrison, P. L., Smith, S. D. A. & Pandolfi, J. M. Conserving potential coral reef refuges at high latitudes. Divers. Distrib. 20, 2455–3257. https://doi.org/10.1111/ddi.12140 (2014).
de O. Soares, M. et al. Marginal reefs in the anthropocene: They are not Noah’s ark. In Perspectives on the Marine Animal Forests of the World (eds Rossi, S., & Bramanti, L.) 875–128 (Springer, 2020).
Randall, C. J., Toth, L. T., Leichter, J. J., Maté, J. L. & Aronson, R. B. Upwelling buffers climate change impacts on coral reefs of the eastern tropical Pacific. Ecology 101, e02918. https://doi.org/10.1002/ecy.2918 (2020).
Sully, S. & van Woesik, R. Turbid reefs moderate coral bleaching under climate-related temperature stress. Glob. Change Biol. 26, 13675–21373. https://doi.org/10.1111/gcb.14948 (2020).
Wanner, H., Solomina, O., Grosjean, M., Ritz, S. P. & Jetel, M. Structure and origin of Holocene cold events. Quatern. Sci. Rev. 30, 31095–33123. https://doi.org/10.1016/j.quascirev.2011.07.010 (2011).
Marcott, S. A., Shakun, J. D., Clark, P. U. & Mix, A. C. A reconstruction of regional and global temperature for the past 11,300 years. Science 339, 1198–1201 (2013).
Haug, G. H., Hughen, K. A., Sigman, D. M., Peterson, L. C. & Rӧhl, U. Southward migration of the intertropical convergence zone through the Holocene. Science 293, 1304–1308 (2001).
Hardy, J. W. & Henderson, K. G. Cold front variability in the southern United States and the influence of atmospheric teleconnection patterns. Phys. Geogr. 24, 1205–2137. https://doi.org/10.2747/0272-36220.127.116.11 (2003).
Liu, Z. et al. Paired oxygen isotope records reveal modern North American atmospheric dynamics during the Holocene. Nat. Commun. 5, 3701. https://doi.org/10.1038/ncomms4701 (2014).
Flannery, J. A., Richey, J. N., Thirumalai, K., Poore, R. Z. & DeLong, K. L. Multi-species coral Sr/Ca-based sea-surface temperature reconstruction using Orbicella faveolata and Siderastrea siderea from the Florida Straits. Palaeogeogr. Palaeoclimatol. Palaeoecol. 466, 100–109 (2017).
Precht, W. F. & Aronson, R. B. Climate flickers and range shifts of reef corals. Front. Ecol. Environ. 2, 3075–3314 (2004).
Precht, W. F. et al. Back to the future: the history of acroporid corals at the Florida Garden Banks, Gulf of Mexico, USA. Mar. Geol. 349, 152–161 (2014).
Precht, W. F. & Miller, S. L. Ecological shifts along the Florida reef tract: the past as a key to the future. In Geological Approaches to Coral Reef Ecology (ed Aronson, R.B.) 237–312 (Springer, 2007).
Jones, N. P., Figueiredo, J. & Gilliam, D. S. Thermal stress-related spatiotemporal variations in high-latitude coral reef benthic communities. Coral Reefs 39, 1661–1673. https://doi.org/10.1007/s00338-020-01994-8 (2020).
Vaughan, T. W. Investigations of the geology and geologic processes of the reef tracts and adjacent areas of the Bahamas and Florida. Carnegie Inst. Washington Yearbook 12, 1–183 (1914).
Lirman, D. et al. Severe 2010 cold-water event caused unprecedented mortality to corals of the Florida reef tract and reversed previous survivorship patterns. PLoS ONE 6, e23047 (2011).
Roberts, H. H., Rouse, L. J., Walker, N. D. & Hudson, J. H. Cold-water stress in Florida Bay and northern Bahamas; A product of winter cold-air outbreaks. J. Sediment. Res. 52, 145–155. https://doi.org/10.1306/212f7efa-2b24-11d7-8648000102c1865d (1982).
Perry, C. T. et al. Loss of coral reef growth capacity to track future increases in sea level. Nature https://doi.org/10.1038/s41586-018-0194-z (2018).
Shinn, E. A. & Lidz, B. H. Geology of the Florida Keys (Florida University Press, 2018).
Banks, K. W., Riegl, B. M., Shinn, E. A., Piller, W. E. & Dodge, R. E. Geomorphology of the Southeast Florida continental reef tract (Miami-Dade, Broward, and Palm Beach Counties, USA. Coral Reefs 26, 617–633 (2007).
Banks, K. W. et al. The reef tract of continental southeast Florida (Miami-Dade, Broward and Palm Beach counties, USA). In Coral Reefs of the USA (eds Riegl, B.M. & Dodge, R.E.) 175–220 (Springer Netherlands, 2008).
Walker, B. K. Spatial analyses of benthic habitats to define coral reef ecosystem regions and potential biogeographic boundaries along a latitudinal gradient. PLoS ONE 7, e30466 (2012).
Lighty, R. G., Macintyre, I. G. & Stuckenrath, R. Submerged early Holocene barrier reef south-east Florida shelf. Nature 276, 59. https://doi.org/10.1038/276059a0 (1978).
Stathakopoulos, A. & Riegl, B. M. Accretion history of mid-Holocene reefs from the southeast Florida continental reef tract, USA. Coral Reefs 34, 173–187 (2015).
Kuffner, I. B. & Toth, L. T. A geological perspective on the degradation and conservation of western Atlantic coral reefs. Conserv. Biol. 30, 706–715. https://doi.org/10.1111/cobi.12725 (2016).
Toth, L. T. et al. The unprecedented loss of Florida’s reef-building corals and the emergence of a novel coral-reef assemblage. Ecology 100, e02781. https://doi.org/10.1002/ecy.2781 (2019).
Gischler, E. Quaternary reef response to sea-level and environmental change in the western Atlantic. Sedimentology 62, 429–465 (2015).
Hubbard, D. K. Holocene accretion rates and styles for Caribbean coral reefs: Lessons for the past and future. SEPM Spec. Publ. 105, 264–281 (2013).
Lighty, R. G., Macintyre, I. G. & Stuckenrath, R. Acropora palmata reef framework: A reliable indicator of sea level in the western Atlantic for the past 10,000 years. Coral Reefs 1, 125–130 (1982).
Toscano, M. A. & Macintyre, I. G. Corrected western Atlantic sea-level curve for the last 11,000 years based on calibrated 14C dates from Acropora palmata framework and intertidal mangrove peat. Coral Reefs 22, 257–270 (2003).
Stathakopoulos, A., Riegl, B. & Toth, L. T. A revised Holocene coral sea-level database from the Florida reef tract, USA. Peer J 8, e8350. https://doi.org/10.7717/peerj.8350 (2020).
Toth, L. T., Precht, W. F., Modys, A. B. & Stathakopoulos, A. Radiometric ages and descriptive data for Holocene corals from southeast Florida. In USGS Data Release, https://doi.org/10.5066/P9Z21NMU (2021).
Shinn, E. A., Hudson, J. H., Halley, R. B. & Lidz, B. H. Topographic control and accumulation rate of some Holocene coral reefs: South Florida and Dry Tortugas. In Proceedings of the 3rd International Coral Reef Symposium Vol. 1, 1–7 (1977).
Neumann, A. C. & Macintyre, I. Reef response to sea level rise: Keep-up, catch-up or give-up. Proc. Fifth Int. Coral Reef Congress 3, 105–110 (1985).
Khan, N. S. et al. Drivers of Holocene sea-level change in the Caribbean. Quatern. Sci. Rev. 155, 13–36. https://doi.org/10.1016/j.quascirev.2016.08.032 (2017).
Finkl, C. W., Benedet, L. & Andrews, J. Seabed classification based on interpretation of airborne laser bathymetry in class II waters off southeast Florida. In Proceedings of the International Coastal Symposium (Höfn, 2005).
Blanchon, P. Back-stepping. In Encyclopedia of Modern Coral Reefs (ed. Hopley, D.) 77–84 (Springer, 2011).
Blanchon, P., Jones, B. & Ford, D. C. Discovery of a submerged relic reef and shoreline off Grand Cayman: Further support for an early Holocene jump in sea level. Sed. Geol. 147, 253–270. https://doi.org/10.1016/S0037-0738(01)00143-9 (2002).
Milne, G. A. & Peros, M. Data–model comparison of Holocene sea-level change in the circum-Caribbean region. Global Planet. Change 107, 119–131. https://doi.org/10.1016/j.gloplacha.2013.04.014 (2013).
Toth, L. T., Kuffner, I. B. & Stathakopoulos, A. Descriptive core logs, core photographs, radiocarbon ages, and data on reef development for cores of holocene reef framework from the florida keys reef tract. USGS Data Release https://doi.org/10.5066/F7NV9HJX (2018).
Camoin, G. F. & Webster, J. M. Coral reef response to quaternary sea-level and environmental changes: State of the science. Sedimentology 62, 401–428. https://doi.org/10.1111/sed.12184 (2015).
Törnqvist, T. E. & Hijma, M. P. Links between early Holocene ice-sheet decay, sea-level rise and abrupt climate change. Nat. Geosci. 5, 601–606. https://doi.org/10.1038/ngeo1536 (2012).
Hallock, P. & Schlager, W. Nutrient excess and the demise of coral reefs and carbonate platforms. Palaios 1, 389–398 (1986).
Hubbard, D. K., Gill, I. P. & Burke, R. B. Holocene reef building on eastern St. Croix, US Virgin Islands: Lang Bank revisited. Coral Reefs 32, 653–669 (2013).
Precht, W. F. & Aronson, R. B. The stability of reef-coral assemblages in the quaternary. In Coral Reefs at the Crossroads. Coral Reefs of the World (eds Hubbard, D.K., Rogers, C.S., Lipps, J.H., Stanley Jr., G.D.) (Springer, 2016).
O’Brien, S. R. et al. Complexity of Holocene climate as reconstructed from a Greenland ice core. Science 270, 1962–1964. https://doi.org/10.1126/science.270.5244.1962 (1995).
Olsen, J., Anderson, N. J. & Knudsen, M. F. Variability of the North Atlantic Oscillation over the past 5,200 years. Nat. Geosci. 5, 808–812 (2012).
Kaufman, D. et al. A global database of Holocene paleotemperature records. Sci. Data 7, 115. https://doi.org/10.1038/s41597-020-0445-3 (2020).
Toth, L. T., Cheng, H., Edwards, R. L., Ashe, E. & Richey, J. N. Millennial-scale variability in the local radiocarbon reservoir age of south Florida during the Holocene. Quat. Geochronol. 42, 130–143. https://doi.org/10.1016/j.quageo.2017.07.005 (2017).
Burman, S. G., Aronson, R. B. & Van Woesik, R. Biotic homogenization of coral assemblages along the Florida reef tract. Mar. Ecol. Prog. Ser. 467, 89–96 (2012).
Leonard, N. D. et al. Re-evaluating mid-Holocene reef “turn-off” on the inshore Southern Great Barrier Reef. Quatern. Sci. Rev. 244, 106518. https://doi.org/10.1016/j.quascirev.2020.106518 (2020).
Sully, S., Burkepile, D. E., Donovan, M. K., Hodgson, G. & van Woesik, R. A global analysis of coral bleaching over the past two decades. Nat. Commun. 10, 1264. https://doi.org/10.1038/s41467-019-09238-2 (2019).
Wyatt, A. S. J. et al. Heat accumulation on coral reefs mitigated by internal waves. Nat. Geosci. 13, 28–34. https://doi.org/10.1038/s41561-019-0486-4 (2020).
Precht, W. F., Gintert, B. E., Robbart, M. L., Fura, R. & van Woesik, R. Unprecedented Disease-Related Coral Mortality in Southeastern Florida. Sci. Rep. 6, 31374. https://doi.org/10.1038/srep31374 (2016).
Kuffner, I. B. et al. Improving estimates of coral reef construction and erosion with in situ measurements. Limnol. Oceanogr. 64, 2283–2294. https://doi.org/10.1002/lno.11184 (2019).
Yates, K. K., Zawada, D. G., Smiley, N. A. & Tiling-Range, G. Divergence of seafloor elevation and sea level rise in coral reef ecosystems. Biogeosciences 14, 1739–1772 (2017).
Kodra, E., Steinhaeuser, K. & Ganguly, A. R. Persisting cold extremes under 21st-century warming scenarios. Geophys. Res. Lett. 38, https://doi.org/10.1029/2011GL047103 (2011).
Stott, P. A. et al. Attribution of extreme weather and climate-related events. WIREs Clim. Change 7, 23–41. https://doi.org/10.1002/wcc.380 (2016).
Cohen, J. et al. Recent Arctic amplification and extreme mid-latitude weather. Nat. Geosci. 7, 627–637. https://doi.org/10.1038/ngeo2234 (2014).
Francis, J. A. & Vavrus, S. J. Evidence linking Arctic amplification to extreme weather in mid-latitudes. Geophys. Res. Lett. 39, https://doi.org/10.1029/2012GL051000 (2012).
Banks, K., Dodge, R. E., Fisher, L., Stout, D. & Jaap, W. Florida coral reef damage from a nuclear submarine grounding and proposed restoration in Proceedings of the 1st International Coastal Science Symposium. 64–71 (Palm Beach, 1998).
Precht, W. F., Macintyre, I. G., Dodge, R. E., Banks, K. & Fisher, L. Backstepping of Holocene reefs along Florida’s east coast (abstract). In Proceedings of the 9th International Coral Reef Symposium. 321 (Bali, 2000).
Gintert, B. E. et al. Regional coral disease outbreak overwhelms impacts from a local dredge project. Environ. Monit. Assess. 191, 630. https://doi.org/10.1007/s10661-019-7767-7 (2019).
Stathakopoulos, A. & Toth, L. T. South Florida Holocene coral sea-level database. USGS Data Release https://doi.org/10.5066/P98QFBJ3 (2020).
Bush, S. L. et al. Simple, Rapid, and Cost Effective: A Screening Method for 14C Analysis of Small Carbonate Samples. Vol. 2013, 10 (2013).
Grothe, P. R. et al. A comparison of U/Th and rapid-screen 14C dates from Line Island fossil corals. Geochem. Geophys. Geosyst. 17, 833–845. https://doi.org/10.1002/2015GC005893 (2016).
Lidz, B. H., Reich, C. D. & Shinn, E. A. Regional Quaternary submarine geomorphology in the Florida Keys. Geol. Soc. Am. Bull. 115, 845–866 (2003).
Reimer, P. J. et al. IntCal13 and Marine13 radiocarbon age calibration curves 0–50,000 years cal BP. Radiocarbon 55, 1869–1887. https://doi.org/10.2458/azu_js_rc.55.16947 (2013).
Toth, L. T., Cheng, H., Edwards, R. L., Ashe, E. & Richey, J. N. Local radiocarbon reservoir age (ΔR) variability from the nearshore and open-ocean environments of the Florida Keys reef tract during the Holocene and associated U-series and radiocarbon data. USGS Data Release https://doi.org/10.5066/F7P8492Q (2017).
Vermeesch, P. IsoplotR: A free and open toolbox for geochronology. Geosci. Front. 9, 1479–1493. https://doi.org/10.1016/j.gsf.2018.04.001 (2018).
Abramson, I. S. On bandwidth variation in kernel estimates—A square root law. Ann. Stat. 1217–1223 (1982).
Team, R. RStudio: Integrated Development for R. RStudio. http://www.rstudio.com/. (PBC, 2020).
Fernandez-Partagas, J. & Mooers, C. N. K. A subsynoptic study of winter cold fronts in Florida. Mon. Weather Rev. 103, 742–744. https://doi.org/10.1175/1520-0493(1975)103%3c0742:Assowc%3e2.0.Co;2 (1975).
We are indebted to the late Ian G. Macintyre, whose kind spirit and foundational work in carbonate geology inspired us to probe the geological record to achieve a greater understanding of the controls on coral-reef development. New reef-matrix samples from south Miami and reef-surface samples from Palm Beach County were collected under Florida Fish and Wildlife Conservation Commission Special Activity Licenses (SAL-13-1436-SRP, SAL-16-1797-SRP, and SAL-18-1659A-SRP) provided to LTT, ABM, and AEO. Samples associated with establishment of the Port Miami monitoring program were collected under FDEP Permit No. 0305721-001-BI issued to the U.S. Army Corps of Engineers. We thank Jack McGeehin of the U.S. Geological Survey Radiocarbon Laboratory for facilitating radiocarbon analysis through the Lawrence Livermore National Laboratory, and Guaciara dos Santos from the Keck AMS laboratory for assistance with rapid radiocarbon dating. We thank Pam Hallock-Muller, Paul Blanchon, David Blakeway, Evan Edinger, and two anonymous reviewers for their thoughtful comments on an earlier version of this manuscript. Funding for the study was provided by the Coastal/Marine Hazards and Resources Program of the USGS. RBA and LTT’s research was partially supported by the U.S. National Science Foundation (grant OCE-1535007). Any use of trade, firm, or product names is for descriptive purposes only and does not imply endorsement by the U.S. Government. This is contribution no. 235 from the Institute for Global Ecology at the Florida Institute of Technology.
The authors declare no competing interests.
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Toth, L.T., Precht, W.F., Modys, A.B. et al. Climate and the latitudinal limits of subtropical reef development. Sci Rep 11, 13044 (2021). https://doi.org/10.1038/s41598-021-87883-8