Shoreline changes and high-energy wave impacts at the leeward coast of Bonaire (Netherlands Antilles)
© The Society of Geomagnetism and Earth, Planetary and Space Sciences (SGEPSS); The Seismological Society of Japan; The Volcanological Society of Japan; The Geodetic Society of Japan; The Japanese Society for Planetary Sciences; TERRAPUB. 2012
Received: 7 December 2010
Accepted: 9 August 2011
Published: 24 October 2012
Supralittoral coarse-clast deposits along the shores of Bonaire (Netherlands Antilles) as well as increased hurricane frequency during the past decade testify to the major hazard of high-energy wave impacts in the southern Caribbean. Since deducing certain events from the subaerial coarse-clast record involves major uncertainties and historical reports are restricted to the past 500 years, we use a new set of vibracore and push core data (i) to contribute to a more reliable Holocene history of regional extreme-wave events and (ii) to evaluate their impact on shoreline evolution. Multi-proxy palaeoenvironmental analyses (XRF, XRD, grain size distribution, carbonate, LOI, microfossils) were carried out using nearshore sedimentary archives from the sheltered western (leeward) side of Bonaire and its small neighbour Klein Bonaire. In combination with 14C-AMS age estimates the stratigraphy reflects a long-term coastal evolution controlled by relative sea level rise, longshore sediment transport, and short-term morphodynamic impulses by extreme wave action, all three of which may have significantly influenced the development of polyhaline lagoons and the demise of mangrove populations. Extreme wave events may be categorized into major episodic incidents (c. 3.6 ka [?] BP; 3.2–3.0 ka BP; 2.0–1.8 ka BP; post-1.3 ka [?] BP), which may correspond to tsunamis and periodic events recurring on the order of decades to centuries, which we interpret as severe tropical cyclones. Extreme wave events seem to control to a certain extent the formation of coastal ridges on Bonaire and, thus, to cause abrupt shifts in the long-term morphodynamic and ecological boundary conditions of the circumlittoral inland bays.
Key wordsWashover deposits tropical cyclones (hurricanes) tsunamis Holocene stratigraphy coastal hazards environmental change Caribbean
A broad spectrum of potential triggering mechanisms of tsunamis exists throughout the Caribbean region. These include (i) earthquake-triggering tectonic movement (strike-slip motion, oblique convergence) along the boundary of the Caribbean and North American Plates (Grindlay et al., 2005) or the Venezuelan coast (Audemard et al., 2005); (ii) the Lesser Antilles subduction zone with earthquakes and various sources of explosive and effusive volcanism (e.g. Zahibo and Pelinovsky, 2001; Mattioli et al., 2007); (iii) morphological signatures of large-scale submarine mass failure, e.g. north of Puerto Rico (Grindlay et al., 2005; ten Brink et al., 2006) or on Curaçao (Hornbach et al., 2010); (iv) submarine debris avalanches along the Lesser Antilles arc (Deplus et al., 2001); (v) teletsunamis from the open Atlantic Ocean as triggered by the 1755 Lisbon earthquake (O’Loughlin and Lander, 2003) or by a future volcanic edifice collapse at the Canary Islands (Ward and Day, 2001). In some places possible geologic evidence of such events has been found onshore such as marine sand sheets deposited inland, barrier breaches or supralittoral boulder deposits in elevated positions significantly exceeding the size of the largest boulders moved by recent severe hurricanes (Khan et al., 2010; Scheffers and Scheffers, 2006), e.g. on Aruba, Bonaire and Curaçao (ABC Islands), the An-tillean Arc, Anegada, Barbados, Jamaica, the Grand Caymans and the Bahamas (Jones and Hunter, 1992; Scheffers, 2004, 2005; Kelletat et al., 2005; Robinson et al., 2006; Atwater et al., 2010). The high tsunami risk is also confirmed by O’Loughlin and Lander (2003) who compile 53 reliable tsunami occurrences in the Caribbean region within the last 500 years of written history.
the designation of high-risk areas,
the creation of public awareness for a generally under-estimated coastal hazard, and
local disaster mitigation planning (cf. Rhodes et al., 2006).
2. Study Sites
The island of Bonaire (Fig. 1) comprises a volcanic core (Late Cretaceous, Washikemba Formation) and a series of surrounding palaeo-reef terraces (Neogene-Quaternary) forming steep cliffs along the coast as well as minor relics of Palaeogene deposition. Slow tectonic uplift (around 5 cm/ka), tilting and Quaternary sea-level fluctuations fostered the development of a sequence of reefal limestone terraces. The lowermost palaeo-reef stages, the Middle Terrace (MT) and the Lower Terrace (LT), relate to MIS 7 or earlier and 5e, respectively (Herweijer and Focke, 1978).
Bonaire has an arid climate and experiences persistent tradewinds from the east, with easterly storms and occasional hurricanes during the period between June and November. The coasts have a microtidal regime (c. 0.3 m). While the eastern shore is exposed constantly to high wave energy, the western, leeward shore—including the study sites of Saliña Tam and Klein Bonaire—is calmer and thus characterised by a vertically narrow notch and a flourishing fringing reef (Focke, 1978). Nevertheless, increased wave action triggered by tropical cyclones in the last decade, e.g. Hurricane Lenny in 1999, taking an unusual west-to-east track, had significant morphological effects on the coral rubble beaches (Scheffers, 2005) and destroyed large parts of the living reef (Bries et al., 2004). The southern part of the western (leeward) coastline from Lacre Punt to Punt Vierkant is covered by coral debris and boulders of up to 2 t, most of which were washed onshore in 1999. Several boulders of up to 20t lie on top of the lower marine terrace LT between Kralendijk and Goto Meer (Scheffers, 2005).
In search of subsurface extreme wave deposits along the leeward side of Bonaire, the former inland bay of Salina Tam and the shallow back-barrier lagoon of southern Klein Bonaire (Fig. 1) were chosen for stratigraphic investigations. The sites are characterised by background sedimentation from shallow standing water (brackish to hypersaline) and occasional fluvial input (Saliña Tam) behind a barrier of coral rubble. At some places thick beds of mangove peat are present. Event layers consist of shallow marine sands, shells, and coral fragments.
2.1 Salina Tam
Postglacial sea-level rise flooded Saliña Tam. The boka is separated from the open sea by a bar of sand, coral rubble and beachrock reaching a width of up to 70 m and a height of up to 3 m above present sea level (a.s.l) (Figs. 2 and 3). When this bar formed and whether it formed due to long-term morphodynamic processes (e.g. longshore drift) (Zonneveld et al., 1977) or due to extreme wave events (Scheffers, 2005; Morton et al., 2008) is a subject of this paper. Today, salinity of the bokas is high (up to 120‰ below the halocline of Goto Meer during summer (Kobluk and Crawford, 1990)) and the water table is low due to low permeability of the seaward barrier, low precipitation most time of the year, as well as to high evaporation (De Buisonjé, 1974).
Approximately 250 m west of Salina Tam, the coastal barrier of coral rubble is separated from the inactive cliff of the LT by a morphological depression filled with sediment (site SAT 10). At ground level the uppermost part of a bioerosive notch is visible. Numerous coral boulders (a-axes up to 2 m) are clustered at the landward avalanching face of the barrier (Fig. 2) (Scheffers, 2005; Morton et al., 2008).
2.2 Southern Klein Bonaire
In order to reconstruct sedimentation processes and palaeoenvironments at the two sites, we examined five sediment cores for their sedimentological, geochemical and fau-nal composition. Cores allow for sampling relatively great depths regardless of the groundwater table, though they only provide one-dimensional insights into the stratigraphy and may hamper the identification of certain sedimentological features indicative of tsunami or storm deposition. Four vibracores (d = 6.0 and 5.0 cm) were taken at Saliña Tam with an engine-driven Atlas Copco 248 coring device. The maximum coring depth was 11 m b.s. (below surface). Two of them were taken with open steel probes (SAT 7 and 10), and in these cases the cores were cleaned, photographed, documented and sampled in the field for multi-proxy analyses. Two vibracores were preserved in closed PVC tubes, which were split in the laboratory (SAT 8 and 9). The fifth core was a 1.28-m PVC push core (d = 7.5 cm) also split in the laboratory (KLB 1).
3.1 Non-destructive core analysis
The inorganic element composition of KLB 1 and SAT 8 was determined using an ITRAX X-ray fluorescence (XRF) core scanner (Cox Analytical Systems). The device was prepared with a 3 kW Mo X-ray tube set to 30 kV and 30 mA. It enabled analyses of semi-quantitative variations of elements from Al to U by scanning 1 mm steps for 20 s each. Element amounts are shown as count rates (cr) representing estimates of the relative concentrations in the sediment (Croudace et al., 2006).
3.2 Analyses using core samples
For a sufficient amount of sediment material each sample from the open cores (SAT 7 and 10) represents sections of 5-10 cm from significant stratigraphic units. The closed cores (SAT 8 and 9, KLB 1) were sampled selectively in 1–2 cm sections. Samples were air-dried and broken up by hand with a mortar and pestle. The carbonate content of the fine-grained fraction (<2 mm) of all vibracores was gas-volumetrically measured following the Scheibler method. Loss on ignition (LOI) was determined by oven-drying at 105°C for 12 h and ignition in a muffle furnace at 550°C for 4 h (Beck et al., 1993). The wet sieve-pipette technique (Kohn, 1928) was applied for analysing the grain size distribution after pre-treatment of the aliquots with Na4P2O7 (55.7 g/l) for aggregate dispersion. Shell material was not removed. Results were processed with GRADISTAT software (Blott and Pye, 2001). Mean grain size was calculated after Folk and Ward (1957) and grain sizes were classified after Arbeitsgemeinschaft Boden (2005).
In order to identify sediment provenance areas (marine, terrestrial-autochthonous, terrestrial-allochthonous), the mineralogical spectrum of selected powder samples was investigated by means of a Siemens 5000D X-ray diffractometer. XRD investigations were carried out using Cu Kα radiation (40 kV, 40 mA). Samples were run from 10° to 70° 2Θ. For semiquantitative interpretation X’Pert High-Score Plus software (PANalytical) was used, which is based on the Rietveld refinement technique fitting a calculated XRD profile to the measured pattern and assigning abundances of minerals.
14C-AMS dates for samples from Saliña Tam and Klein Bonaire were carried out at the radiocarbon laboratoriy of the University of Georgia at Athens (USA).
Depth (cm b.s.)
Lab ID UGAMS#
Age cal BP (2σ)
2740 ± 25
2280 ± 20
3110 ± 20
4030 ± 25
4160 ± 25
3360 ± 25
SAT 10/4 Ko
1890 ± 25
2080 ± 25
KLB 1/a 43
3240 ± 25
KLB 1/c 70
3570 ± 30
4. Sedimentary Record of Salina Tam
4.1 The back-barrier record—SAT 7/8
Sediment cores SAT 7 and SAT 8 represent the stratigraphy directly behind the broad ridge of coral rubble separating Saliña Tam from the open sea (Fig. 2). One open (SAT 7) and one closed (SAT 8) core were taken at the same site. The environmental interpretation of the cores is given on Figs. 6 and 7.
The lower 7.75 m (11.00–3.25 m b.s.) at site SAT 7/8 consist of a coquina of fine shell debris (light grey bivalves, mainly Ctena orbiculata, and gastropods, mainly Bulla striata, Caecum sp.), carbonate sand (on Bonaire predominantly fragments of Halimeda sp.) and bryozoan fragments showing a high degree of abrasion. Ca and Sr concentrations are high and slightly decrease in the uppermost part. At 3.35–3.25 m b.s., the coquina contains lagoonal ostracods (Cyprideis beaveni [partly noded], Cyprideis sp., Perissocytheridea cribrosa; Fig. 5), small benthic foraminifers (miliolinids), and remains of small fish and echinoderms.
The overlying deposit of very dark brown sandy silt (3.25–2.82 m b.s.) shows an abrupt decrease in CaCO3 and increasing LOI values. From 3.00–2.82 m b.s. the unit is stratified and contains thin layers of calcite, arag-onite and gypsum. Concentrations of K, Ti and Br increase. Cyprideis beaveni (partly noded), Cyprideis sp., Perissocytheridea cribrosa and miliolinid foraminifers are still present. Mollusc shells, bryozoan and echinoderm remains are absent.
The overlying unit (2.60–2.38 m b.s.) is pale white and almost entirely consists of CaCO3. Four sequences–three normally graded beds containing shells of Cerithium sp. and coarse sand at the bottom, and one inversely graded bed (Fig. 7)—were identified. A very thin mud drape covers the second graded sequence. The section contains reworked valves of brackish ostracods as well as miliolinid foraminifers, Amphistegina, Discorbis, Alcyonaria and fragments of Malacostraca, Scleractinia and several other marine forms. Planktonic foraminifers (Globigeri-noides cf. immaturus) were also located (Fig. 5). Aragonite is the dominating mineral. The amount of quartz is very low. From the lower part of this unit (in SAT 7) as well as from 2.43 m b.s. (in SAT 8) cerith shells were radiocarbon dated to 2607-2462 and 2021-1869 cal BP (Table 1, Figs. 6 and 7).
Between 2.38 and 2.30 m b.s. are three fining-up sequences, with distinct lower contacts consisting of a very thin basal layer of carbonate sand and a thicker muddy, organic-rich part. The spectrum of microfossils covers Cyprideis sp. and P. cribrosa, and some tests of miliolinid foraminifers and Amphistegina. The amount of marine biogenic particles is significantly reduced compared to the underlying graded beds.
The overlying units represent the background sedimentation: Ca and Sr are lower than previously, and LOI, Ti, Br and K values higher. The most abundant mineral is quartz. Several plant remains (leaf fragments, wood) and angular stones were found. A thin unit of alternating silt layers of carbonate and gypsum occurs between 2.30 and 2.26 m b.s. From 1.00–0.76 m b.s., CaCO3 values and mean grain size are higher than background and the sediment is more poorly sorted.
4.2 The landward alluvial plain—SAT 9
From the base, 5.00 m, to 3.49 m b.s. there is a unit of black peat with high LOI and low CaCO3 concentrations as well as a large number of juvenile smooth bivalves and several specimens of miliolinid foraminifers and Ammonia spp. (Fig. 5). Plant fragments from 3.60 and 3.55 m b.s. were dated by 14C to 4826–4584 and 4568–4424 cal BP.
The peat is overlain by half a meter of light olive brown carbonate mud with an erosive basal contact (3.49–2.94 m b.s.) and numerous gypsum crystals. Carbonate content reaches up to 60%. Angular stones and complete cerith shells are present in the matrix. C. beaveni (partly noded) and P. cribrosa as well as several miliolinid foraminifers compose the microfauna. Juvenile smooth bivalves are rare. No shell material indicating open marine or reefal origin was identified.
From 2.94 to 2.77 m b.s. the sediment consists of thin alternating beds of carbonate sand (light brown) and grey layers of silty clay, both containing gypsum and halite crystals. While sand layers are linked to small peaks in CaCO3, silty clay layers coincide with peaks in LOI. C. beaveni (partly noded), Cyprideis sp. as well as miliolinid foraminifers are abundant, whereas P. cribrosa is rare. Several ostracods show signs of reworking.
The overlying metre (2.77–1.74 m b.s.) consists of olive grey sandy silt showing an upward decrease in CaCO3. At 1.74–1.65 m b.s. there are three layers of coarse gypsum crystals. Above, the uppermost unit of SAT 9 consists of very dark grey clayey silt with several reddish dark brown sections. The ostracod fauna is brackish, noded C. beav-eni decrease. A minor peak in CaCO3 occurs at 0.90– 1.00 m b.s.
4.3 Between Saliña Tam and Punt’i Wekua—SAT 10
The coral rubble is overlain by a unit of very dark brown mangrove peat (2.17–0.52 m b.s.) dated to 2295–2004 cal BP at 2.10 m b.s. An erosional boundary separates the peat from a carbonate sand layer (0.52–0.40 m b.s., layer A in Fig. 9) containing reworked peat remains, shell debris and two 4 cm-fragments of Diploria sp. (1563–1395 cal BP). In a trench at the site (photo inset in Fig. 9), even coarser coral shingle and beachrock slabs containing branches of A. cervicornis were present in this layer. At 0.40–0.30 m b.s. (layer B in Fig. 9) the sediment consists of poorly sorted, grey silty sand with shell debris. The overlying strata consist of dark greyish brown (0.30–0.17 m b.s.) to dark yellowish brown (0.17–0.00 m b.s.) silty matrix with reduced carbonate sand components (layers C and D in Fig. 9).
4.4 The sedimentary record of southern Klein-Bonaire—KLB 1
The basal part (1.28–1.20 m b.s.) consists of light olive grey sandy silt containing several gastropod shells, a lens of root material, and a brackish-marine foraminifer assemblage dominated by miliolinid foraminifers and Ammonia spp. (both taxa highly abundant), marine mollusc shells, and only few ostracods. Between 1.20 and 0.70 m b.s. is a layer of pure mangrove peat void of Ca and Sr and exhibiting a high plateau in the Br curve. The peat is unconformably overlain by two thin graded beds (0.70–0.67 cm b.s.; 0.67– 0.66 cm b.s.), both characterized by basal carbonate sand with well-preserved gastropod shells and shell fragments, an upward decrease in Ca, a Br peak in the upper part corresponding to a mud cap (Chagué-Goff et al., 2002; Perez et al., 2010) and a large number of reworked brackish ostracods. The amount of aragonite is more than 60%. Radiocarbon dating of a cerith shell (0.70 m b.s.) yielded an age of 3614–3426 cal BP. The thin sand beds are overlain by a well sorted layer of light yellowish brown sandy silt (0.66– 0.64 m b.s.) rich in Ca and Sr. Aragonite is significantly reduced in favour of calcite. A thin layer of mangrove peatresembling the lower peat is present at 0.64–0.60 m b.s. A sharp upper boundary separates it from a massive layer of loamy carbonate sand (0.60–0.35 m b.s.), which is divided into three subunits: (i) a lowermost normally graded sequence with shells and shell fragments (0.60–0.50 m b.s.); (ii) a coarsening-up sequence (0.50–0.43 m b.s.) associated with increasing values of Ca and Sr, a large peatclast, most likely from the underlying peat, and shells of Cerithium sp. in the upper part; (iii) a normally graded bed (0.43–0.35 m b.s.) with basal shell material and another large peat clast.
The overlying stratum (0.35–0.15 m b.s.) also has a normally graded bed and contains Cerithium sp. shells. At 0.14–0.02 m b.s. is a pale yellow, silty fine sand consisting of calcite, dolomite, gypsum and halite with no larger components. The surface is composed of a very dark brown aragonite-rich crust.
Interpretation of the cores is based on the assumption that sedimentary patterns are predominantly determined by relative sea level evolution, intermittent river input, typical yearly wave action as well as hurricanes and tsunamis. The frequency of strong hurricanes is considered as periodic (in the order of 10–500 years), the one of major tsunamis as episodic (in the order of 500–5000 years). Both are summarised under the term extreme wave event (EWE). Even though long-term fluctuations in temperature and precipitation were considered to be very important in other palaeoenvironmental investigations along Caribbean shorelines (e.g. Bertran et al., 2004), they appear rather negligible in this study, at least concerning the prehistoric core sections. Evaporation rates throughout the time of deposition seem to have been cosistently high, often resulting in stressful ecological conditions, reflected by the low diversity of the in-situ ostracofauna (cf. Frenzel and Boomer, 2005). Increased sedimentation rates in the last millennium on Bonaire (Engel et al., 2010) may be the result of a combination of anthropogenic impact on the vegetation— e.g. livestock breeding since the 16th century AD (Hartog, 1978)—and a regional aridification impulse (Haug et al., 2003).
5.1 High energy wave impacts and shoreline change
5.1.1 Klein Bonaire (KLB)
In the south of Klein Bonaire, the lowermost calcareous deposit (pre-3.6 ka BP) may be associated with a calm lagoon connected to the open ocean according to the presence of a large number of shallow marine to brackish foraminifers (Quinqueloculina spp., Ammonia spp.) and ostracods (C. beaveni) (e.g. Culver, 1990). Several well-rounded shell fragments point to temporarily intensified energetic conditions. Thus, the mangrove peat overlying this carbonate mud may be interpreted as a regressive process where prograding mangroves colonised marginal marine sediments, similar to findings made by Woodroffe (1981) at North Sound, Grand Cayman.
At around 3.6 ka BP or later (cerith shell: 3614–3426 cal BP) a high-energy wave event (which we label EWE I) possibly destroyed the mangroves, as indicated by an erosional unconformity and two thin fining-up sequences, each capped by rafted plant fibres from the underlying peat. Ostracod valves from the beds indicate reworking. The event significantly contributed to the formation of a barrier of coral rubble fringing the entire coast of southern Klein Bonaire and which limited access to the open ocean. This is inferred from the subsequent layer of carbonate mud resembling recent deposition at KLB 1. High amounts of dolomite (>25%) within this lithofacies result from increasing Mg/Ca ratios due to evaporation of the supratidal sea water and withdrawal of Ca due to gypsum precipitation and secondary replacement of pre-existing CaCO3 (Deffeyes et al., 1965; Klosowska et al., 2004). Subsequently, mangroves began to recolonise the site.
The mangrove stands, which reestablished at KLB 1 after EWE I, were irreversibly destroyed by a major wave impact (EWE II) overtopping the barrier. EWE II left a deposit, which unconformably overlies the mangrove peat. It is divided into three beds of marine sediment and contains large reworked clasts of the underlying peat material causing excursions in the Br curve (Fig. 9). EWE II struck the coastline of Klein Bonaire 3.2–3.0 ka BP or later (cerith shell: 3236–3028 cal BP).
5.1.2 Saliña Tam (SAT)
The deepest and oldest sediment unit reached at Saliña Tam is between 11.00 and 3.25 m b.s. right behind the barrier of coral rubble (SAT 7/8). High amounts of Ca and Sr, well rounded carbonate particles and shell debris as well as its extraordinary thickness relate to a sublittoral environment or—regarding the upper part of the unit—to the beach ridge of a shoreline, which ran landward in a sheltered position right at the foot of the MIS 5e cliff (mid-Holocene transgression in Fig. 2). Since long-term littoral sedimentation is connected to the sea level, an age of c. 8 ka for the base of core SAT 8 may be inferred from the model of southern Caribbean sea level evolution by Milne et al. (2005). The early to mid-Holocene transgression is assumed to have flooded the near-shore parts of the island’s drainage network creating bokas with full sea access and a landward fringe of mangroves comparable with today’s inlet of Lagun, west Bonaire (cf. Engel et al., 2010). Mangroves established when relative sea level rise decelerated c. 7–6 ka ago (McKee et al., 2007) and compensation through subsurface accumulation of resistant roots and rhizomes was possible (Woodroffe, 1981; McKee et al., 2007). The mangrove populations at Saliña Tam were probably dominated by Rhizophora mangle according to mid-Holocene pollen spectra (Engel et al., 2009) and recent mangrove stands (De Freitas et al., 2005) along the west coast of Bonaire. Small but stable mangrove populations persisting at Saliña Tam until at least 4.5 ka BP are represented by thick fibrous peat accumulations in the landward core SAT 9 (5.00–3.49 m b.s.). Their microfaunal assemblage of brackish ostracods and foraminifers, both of which show relatively high abundance and diversity, as well as numerous juvenile bivalves reflect low-energy environmental conditions of a distal lagoon connected to the open sea.
Isolation of the boka some time before 3000 BP is reflected by thin alternating layers of organic rich sediment, platy aragonite and gypsum, which cover the littoral litho-facies in SAT 8 (Fig. 4). The evaporites relate to autochthonous sedimentation and a negative water balance due to limited water input either from the sea or inland in combination with high evaporation as also observed on Curacao (Klosowska et al., 2004). Mg, Na, Cl and Ca ions indicate high evaporation rates and isolation from the sea similar to recent conditions, but also continuous sea water supply through the permeable seaward barrier. Depending on fluctuating concentrations of soluble salts, different evaporite types precipitated forming the cyclic laminated depositional pattern. Surface runoff at that time was reduced since the amount of detrital material from the volcanic catchment area (quartz, plagioclase) is very low (SAT 8, 3.00-2.82 m b.s.). Euryhaline to polyhaline conditions are supported by the sole presence of Cyprideis sp. and Perissocytheridea cribrosa within the ostracofauna (Keyser, 1977).
No sedimentary evidence for an abrupt closure of the boka during an episodic wave event was found at SAT 8. It seems likely that the barrier was formed gradually due to the low rate of sea-level rise (Milne et al., 2005), a moderate longshore current from south to northwest (Zonneveld et al., 1977) and the effects of periodic tropical cyclones, which are capable of moving coral rubble onshore (Schubert and Valastro, 1976; Scheffers and Scheffers, 2006; Spiske and Jaffe, 2009). The stratigraphy of the lower part of the barrier (Fig. 5) also supports a gradual closure of Salina Tam due to the very well rounded particles in its entire lower part (pre-1300 BP according to Scheffers et al., 2009) resembling the degree of roundness of A. cervicornis fragments at the present beachface. They differ significantly from the angular coral rubble, which builds up the uppermost part of the barrier (Fig. 3) and was removed and transported onshore by a major hurricane (EWE XVI or later?) according to Scheffers (2005) and Scheffers et al. (2009). For the period when Salina Tam closed (c. 3.5–3.4 ka BP), a gradual barrier formation was also reconstructed for the St. Michiel Lagoon at leeward Curaçao, which shares similar morphodynamic boundary conditions (Klosowska et al., 2004). However, the isolation of Saliña Tam is in the same time window as EWE I (inferred from the core at Klein Bonaire) which may have accumulated coral material at the outlet of the boka.
Isolation of the small basin of Saliña Tam resulted in a demise of the mangrove population in the landward part of Salina Tam (SAT 9), which depends on the circulation of sea water. The deposition of autochthonous carbonate mud at SAT 9 started before 3359–3206 cal BP and correlates with the evaporite facies in SAT 8 (3.00–2.82 m b.s., pre-3039–2857 cal BP). The carbonate mud itself in SAT 9 is not related to an EWE since it is very homogeneous and marine sand, faunal remains or reworked material of the underlying peat are absent. However, the erosional unconformity might be induced by purely erosional processes during EWE I—the relevance of which has been demonstrated by MacInnes et al. (2009) on the Kurils, N Pacific. The abundant valves of noded C. beaveni (75%) and P. cribrosa as well as several miliolinid foraminifers within the carbonate mud indicate euryhaline to polyhaline still water conditions (Keyser, 1977) and show no signs of reworking.
We interpret the basal part of the coarse shelly sequence in SAT 8 (2.82–2.76) to be a deposit of EWE II (cf. KLB 1, chapter 5.1.1); the age control is from an overlying bed (2.72 m b.s.) of 3039–2857 cal BP. This basal unit is a fining-up sequence, which has a partly marine microfauna, an upward decrease in Ca and Sr, and is capped by organic-rich mud. The mud layer, marked by a small Br peak (Fig. 6), we interpret to have been deposited after flow attenuation.
We also interpret the following nine sequences (2.76– 2.60 m b.s. in Fig. 6) as deposits of overwash events (EWE III–XI) affecting the interior of Saliña Tam due to the partial destruction of the barrier during EWE II. Within the entire section EWE III–XI, increased marine influence is reflected by abraded sand-sized shell particles. Each of the nine de-positional cycles comprises basal sand with increasing phy-tomass and mud content upward. Accordingly, nine significant overwash events may be inferred between c. 3.0 ka BP and the overlying age 2.0–1.8 ka BP based on radiocarbon dates of cerith shells (Table 1, Fig. 5).
The depositional sequence containing a radiocarbon age of 2021–1869 cal BP unconformably overlies the EWE III– XI unit and consists of a wide variety of marine microfossils (benthic and planktonic) indicating that it was generated by a larger EWE (which we label XII) than EWE III–XI.
After EWE XII, three minor overwash deposits separated by relatively thick mud sections (EWE XIII–XV) indicate a lower frequency compared to the phase of EWE III–XI.
Above the EWE sequences associated with a partial destruction of the barrier and a higher susceptibility to over-wash deposition, still-water conditions very similar to the period before EWE II (pre-3.2–3.0 ka BP) indicate that the barrier closing the boka recovered. We assume that reshaping the barrier represents development towards an equilibrium defined as “stability of form” (Woodroffe, 2002: 32) during a relatively stable sea level after disturbances (EWE II–XII) manifested by cyclic carbonate sequences spanning a period of c. 1 ka. This is a long time given the fact that beaches of Sumatra and Thailand have reorganised only a few years after the Indian Ocean Tsunami of 2004 (IOT) (Choowong et al., 2009; Liew et al., 2010). Nevertheless, Kraus (2005): 171) describes barrier breachings, which did “not recover on the timescale of human lifetime” in case the event was so strong that the sediment was transported into deeper water—consider the narrow reef and steep offshore slope of Bonaire—where it was out of reach for long-term wave action. Temporary changes in external boundary conditions, e.g. an interruption of the longshore current, increased hurricane frequency, and limited sediment sources, also have to be taken into consideration. In addition to the coring results, the reestablishment of the barrier after 2.0 ka BP is corroborated by ESR ages from the Saliña Tam barrier, all of which are younger than 1.3 ka (Scheffers, 2005).
The period of increased susceptibility to overwash impact at Salina Tam (EWE III–XI) or EWE II both inferred from SAT 8, might correlate with layer 2.94–2.77 m b.s. in SAT 9 where reworked ostracods were identified; however, this is a tenuous assumption since age control is not available. Apart from that, SAT 9 has no clear event deposits.
West of Saliña Tam, at SAT 10, a mangrove population established around 2.0 ka BP. Below the mangrove peat, the coral rubble from the basal core unit is interpreted to derive from a major EWE (II or XII?). After the event, the area was sheltered by the coastal barrier but still had access to the sea providing a suitable habitat for mangroves. The demise of the mangroves is associated with the two overlying units of medium sand (layers A and B in Fig. 9), which most probably represent one or two EWE. The age of a coral boulder found at the landward foot of the broad ridge of coral rubble adjacent to SAT 10 was dated to 1300 ± 60 (Fig. 2; Scheffers, 2005). Since a Diploria. sp. fragment from the sand layer yielded a similar age (1563–1395 cal BP), boulder transport and deposition of the sand layers may be linked to one EWE (which we label XVI). The overlying silt-dominated alluvial lithofacies (C and D in Fig. 9) contains several carbonate sand components testifying to periodic small overwash processes.
The upper sediment column of SAT 8 (2.00–0.00 m b.s.) and SAT 9 (2.78–0.00 m b.s.) is dominated by detrital sedimentation as indicated by increased amounts of quartz, anorthite and albite (feldspar varieties) in the mineralogical spectrum. Mean grain size is small reflecting the interface between the fluctuating still water body and distal alluvial fans (inferred from changing LOI percentages). At SAT 8, two candidate overwash deposits occur at 1.96–1.87 m b.s., where several bryozoan fragments are preserved, and at 0.97–0.77 m b.s. (EWE XVI?). The upper one might correlate with a peak in CaCO3 at SAT 9 (1.00–0.90 m b.s.). However, both layers are heavily altered by capillary evap-orites from interstitial pore waters.
5.2 Extreme wave events (EWE): tsunamis or tropical cyclones?
Sediment layers from Salina Tam and Klein Bonaire interpreted as extreme wave deposits fulfill several criteria commonly associated with tsunami and/or storm wave impacts, such as a basal unconformity, reworked underlying material, graded bedding, increased mean grain size, peaks in marine indicator ions (Ca, Sr), increased CaCO3 content as well as marine microfossils showing signs of reworking (Switzer and Jones, 2008; Mamo et al., 2009; Peters and Jaffe, 2010). However, in the sedimentary record, differentiating between deposits of tsunamis and waves generated by extraordinary storms is challenging (Bridge, 2008) since most onshore sedimentary features attributed to either one may be generated by both hydrodynamic processes (Sugawara et al., 2008). Further problems in deducing a chronology of extreme wave events from the strati-graphic record include the possibility that events may not leave sedimentary traces, that sediments may be eroded or heavily disturbed, e.g. by bioturbation (Szczuciński, 2012), and that radiometric ages obtained from the deposit may not represent the age of the event (Sugawara et al., 2008) due to possible previous reworking or local reservoir ages. The sedimentary pattern a tsunami creates is hard to predict and site-specific. However, interpretations may be enhanced by identifying the presence of a high number of common tsunami signature types, by careful analyses of the local sedimentary environment and “the geologic potential for tsunamis” (triggering processes) at a site (Peters and Jaffe, 2010: 22), by comparing a candidate tsunami deposit with local modern analogues (either recent tsunami or storm deposits), and by also considering the coarse-clast record (e.g. Yu et al., 2009; Peters and Jaffe, 2010). On Bonaire, no historical tsunamis are documented, but category 5 hurricanes passed the island several times within close distance during the recent past (Meteorological Service of the Netherlands Antilles and Aruba, 2009) leaving very little to no sediment at coastal depressions such as alluvial plains and bokas (Engel et al., 2010).
5.2.1 EWE I (→ KLB 1)
Tsunami. EWE I was only found in KLB 1 where it is represented by two thin graded beds of 2 and 1 cm thickness. It may also be associated with an erosional unconformity above the peat in SAT 9. The graded beds are dated to c. 3.6 ka BP or later (Fig. 11). Both graded beds are characterized by plant remains and finer material covering basal marine sand. These findings indicate a long wave period of at least several minutes of flow attenuation. Similar observations were made following the tsunamis of Papua New Guinea 1998, Peru 2001 (Morton et al., 2007) and the IOT 2004 (Choowong et al., 2008; Naruse et al., 2010). Thus, storm wave origin after a long period of undisturbed mangrove growth seems unlikely though not impossible.
5.2.2 EWE II (→ SAT 8, KLB 1)
Tsunami. Barrier destruction or breaching by EWE II at Saliña Tam c. 3.2–3.0 ka BP is a phenomenon commonly associated with extraordinary storms or tsunamis (Andrade et al., 2004; Kortekaas and Dawson, 2007; Atwater et al., 2010). Even though it is difficult to deduce the exact origin of the EWE II deposit in SAT 8, the presence of open marine planktonic forman-ifera, which are absent in the overlying deposits from periodic events may point to tsunami (cf. Luque et al., 2002; Uchida et al., 2010). At Klein Bonaire, two normally and one inversely graded sequence are associated with EWE II. Large intraclasts of the underlying peat are a typical feature of tsunami deposits (Kortekaas and Dawson, 2007; Morton et al., 2007; Choowong et al., 2008; Switzer and Jones, 2008; Bourgeois, 2009; Mamo et al., 2009; Peters and Jaffe, 2010), even though they have also been observed within storm deposits (Wang and Horwitz, 2007). At Playa Grandi, northeast Bonaire, a coeval deposit was interpreted as tsunamigenic based on taphonomic characteristics and the comparison with the marginal sediment input during recent hurricanes (Engel et al., 2010). Scheffers et al. (2009) deduced a major tsunami around 3.1 ka BP based on 14C and ESR ages of onshore coral debris from eastern Bonaire even though this chronological interpretation has recently been challenged by Morton et al. (2008).
5.2.3 EWE III–XI (→ SAT 8)
Cyclones. Deposi-tional cycles of sand and organic-rich mud present in SAT 8 relate to periodically recurring inundation pulses during EWE III–XI in the order of decades to centuries. The lower sequences might also be associated with a tsunami wave train of EWE II creating several fining-up layers (cf. Morton et al., 2007; Switzer and Jones, 2008).
However, nine (EWE III–XI) thin graded sequences implying c. 1 ka of deposition correspond to the approximate recurrence rate of severe tropical cyclones on Bonaire, which is about 100 years (Meteorological Service of the Netherlands Antilles and Aruba, 2009). It is assumed that storm waves transported reworked particles from the surf zone and shallow marine ostracods into the partly opened southern section of Saliña Tam, each time followed by ponding conditions resulting in sedimentation of organic-rich mud and plant debris and growth of algae (cf. Morton, 1978). This interpretation is in accordance with that of sand layers in a hypersaline lagoon of southern Puerto Rico by Donnelly and Woodruff (2007). A series of thin normally graded sequences may only be attributed to one single storm event if the graded layers are not separated by mud layers due to the short periods of storm wave pulses (Morton et al., 2007). No planktonic or larger foraminifera were identified in these beds, also indicating a different, less extended source area of the sand than in the sediments of EWE II and XII.
5.2.4 EWE XII (→ SAT 8, SAT 10 [?])
Tsunami. Around 2.0–1.8 ka BP, EWE XII struck Bonaire’s coastline. For the same time, a tsunami impact was inferred from a massive shell debris layer on the eastern shore (Engel et al., 2010). The high diversity of marine particles including planktonic foraminifers and marine ostracods recorded in this bed at SAT 8 (Fig. 5) indicates a wider source area compared to the underlying beds interpreted as storm deposits and may support the tsunami hypothesis. Larger foraminifers such as Amphistegina sp., for instance, relating to a reefal sediment source were also found in deposits of the IOT 2004 on the Andaman Islands (Hussain et al., 2006). In a sediment sequence from Martinhal (Algarve, Portugal) containing deposits from the 1755 AD Lisbon tsunami and subsequent storm events, slightly increased mi-crofossil diversity within the tsunami sediments was one of the few features differentiating the layers (Kortekaas and Dawson, 2007). The bedding structure including shell debris at the bottom, two fining-up sequences followed by inverse grading and a relatively thick normally graded sublayer may correspond to tsunamigenic deposition rather than to cyclone-induced waves (Morton et al., 2007).
5.2.5 EWE XIII–XV (→ SAT 8)
Cyclones. Sediment layers of EWE XII–XV (SAT 8) show a similar structure to those of EWE III–XI, even though thicker subunits of organic-rich mud indicate lower frequency, which could be related to barrier regrowth. Cyclic hurricane impacts are assumed to be responsible for their deposition since diversity and abundance of marine microfossils decreases compared to EWE XII.
5.2.6 EWE XVI (→ SAT 10, SAT 8 [?])
Tsunami? A sand deposit unconformably overlying mangrove peat at SAT 10, containing shell debris and coral rubble (1563– 1395 cal BP), and an adjacent ESR-dated coral boulder (1300 ± 60 a according to Scheffers, 2005) indicate that around 1.3 ka BP or later, a major wave event (EWE XVI) impacted the leeward shore of Bonaire. EWE XVI is the youngest EWE that is well-preserved in the local stratigraphy. Major historical hurricanes, e.g. in 1877 and 1999, only modified the higher berm (Scheffers, 2005; Fig. 2), but did not leave distinct sand sheets within the back-barrier, what may indicate that EWE XVI was a tsunami.
The stratigraphy of Saliña Tam at the leeward coast of Bonaire reflects an interplay of long-term sea-level rise, gradual sediment dynamics as well as periodic (tropical cyclones) and episodic (tsunamis) wave impacts. Figure 11 provides a synopsis of the cores of this study focussing on the distribution of extreme wave deposits. Clear sedimentary evidence for EWE I (tsunami) is only provided on Klein Bonaire, though it may be associated with the ero-sional unconformity in SAT 9. The scale on the right on Fig. 11 shows that EWE II (around 3.2–3.0 ka BP) which we also interpret as tsunamigenic is well represented at several sites on the island including the windward coast. A third candidate tsunami deposit (EWE XII) from c. 2.0– 1.8 ka BP is preserved at Saliña Tam (SAT 8) and Lagun (Engel et al., 2010). EWE XVI (post-1.3 ka BP) had a major impact on barrier accumulation at Saliña Tam. It may also correspond to a tsunami since recent strong hurricanes (e.g. west-east-tracking Hurricane Lenny in 1999) caused no changes on the top and back of the barrier. However, sedimentary evidence of this event is limited at other sites. Today, i.e. in case of a stable barrier of coral rubble, marine sediment deposition at Salina Tam tends to zero during tropical cyclone conditions. Thus, the graded sequences of EWE III–XI and XIII–XV, which we interpret as storm wave deposits, are associated with a breach of the barrier.
The geographical distribution of event deposits was found to be very irregular and difficult to predict, even on a small spatial scale. The same applies to the impact of tsunamis and extraordinary storms on the coastal morphology. However, the outcome of this study is that high-energy wave events do have long-lasting effects on the coastal morphology and ecosystem of Bonaire. This influence includes century-scale destruction of coastal ridges and may even trigger or drive ridge formation (cf. Scheffers, 2005; Scheffers et al., 2009). This process has recently been observed during Hurricane Lenny, when a spit of coral rubble (c. 100 m long) was accumulated in the foreshore of north Bonaire (Scheffers and Scheffers, 2006; Morton et al., 2008). EWEs seem to control the formation of coastal sedimentary landforms to a certain extent, as already been emphasised by Scheffers (2004), 2005), Morton et al. (2008), Scheffers et al. (2009), and Watt et al. (2010), and thus, they shift ecological and morphodynamic boundary conditions of the circumlittoral bokas.
Funding by the Deutsche Forschungsge-meinschaft (German Research Foundation) is gratefully acknowledged (BR 877/26-1). Administrative and logistic support was kindly provided by DROB (Government of the Island Territory Bonaire/Department of Environment and Natural Resources) and STINAPA (Bonaire National Parks Foundation). We are thankful for fieldwork support by Frank Schabitz (Cologne), Timo Willershauser (Mainz) and Jan Brouwer (Hato, Bonaire). Andreas Ginau (Frankfurt/M.) helped with the interpretation of XRD spectra. Andreas Bolten (Cologne) calculated the bathymetric model. Armine Shahnazarian (Cologne) assisted the XRF analyses. We are grateful to Jody Bourgeois (Seattle) and Klaus Re-icherter (Aachen) for their thorough reviews and helpful remarks as well as Kirstin Jacobson (Marburg) for language editing.
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