1997) and 9–15 m/ka from the Caribbean (Adey 1978), although recent observations

show a marked decline in some regions (e.g., Perry et al. 2013). The FHPI molecular weight atolls and atoll reef islands observed today are geologically young features, having formed on older foundations since global sea level stabilized about 6,000 years ago (Bard et al. 1996). They have developed some degree of dynamic equilibrium with current climate and oceanographic environment, but are continually subject to readjustment, erosion and sedimentation, in response to varying sea levels, wind patterns, and storms. Reef islands (Fig. 5a) develop on atoll margins, typically surrounding a central lagoon (Richmond 1992; Kench et al. 2005; Woodroffe 2008). In places these form a complete ring, but often they occupy only part of the reef rim, leaving large gaps (Fig. 4). Reef islands are typically Go6983 order elongate quasi-linear ABT-737 cost features 100–1,000 m wide with crests <4 m above MSL and consist predominantly of unlithified or weakly cemented sediments derived from the reef, resting on a hard reef flat or cemented coral-rubble conglomerate. The dominant constituents of reef-island sediment vary from atoll to atoll, ranging from coral or crustose coralline algae to calcareous green algae (Halimeda) and foraminifera. Foraminifera tend to predominate on Pacific atolls, while

Halimeda is the dominant sediment source in the Caribbean (Yamano et al. 2005; Perry et al. 2011). On many atolls in the Pacific and eastern Indian Ocean, evidence of a higher Holocene sea level is preserved as fossil coral in growth position (Pirazzoli et al. 1988; Woodroffe et al. 1999; Woodroffe 2008). Exposures of slightly raised conglomerate in the shore zone provide some resistance to erosion and influence the planform shape of reef islands (Solomon 1997). Inter-island channels and passages interrupt the continuity of atoll rim islands and provide openings 3-oxoacyl-(acyl-carrier-protein) reductase for lagoon water exchange and for sediment from the reef to be swept past the islands into the lagoon (Fig. 5b). Fig. 5 a Southern reef rim of Manihiki, northern Cook Islands (1,200 km north

of Rarotonga), looking east toward the southeast corner of the atoll (photo courtesy SM Solomon 1996). b Northeast rim of Nonouti Atoll, Kiribati, 240 km south-southeast of Tarawa, looking onshore. Grooved forereef and reef crest in foreground with reef flat, complex reef islands and inter-island passages carrying sediment into the lagoon (background). Reef flat is approximately 250 m wide and main channel in middle of image is 500 m wide at near end (photo DLF 1995) High carbonate islands including raised atolls High carbonate-capped islands (Fig. 2) occur in forearc belts adjacent to subduction zones such as the Tonga Trench (Clift et al. 1998; Dickinson et al. 1999), the Cayman Trench (Perfit and Heezen 1978; Jones et al. 1997), and the Lesser Antilles arc-trench system (Bouysse et al. 1990).